| moata
: Ze < Ce

VEE 3

—

(<a EC Siete Ss
2 x \t — —

yh = = —_ 3
6 CO EK a< << <
x <@ 4 * QC

3 Sk SE

— = aS: = > Se ee oN

URE 4G, CC ECHR « aM ee «
SOS ee Kas <a << —
Ss <<

s Ce CC ars = ee Se, a a o EE SA
ECC a <a <a

far ae —
Af

Wy NNN y\ An Al

‘A A AN. a ;

EY,

OF

THE GIFT
WHITN

S

J

WHITNEY LIBRARY,
turgis Hooper Professor
IN THE
MUSEUM OF COMPARATIVE ZOOLOGY

a
=I
@)
ater
fo
2
7
2)
2
ae
<
ie
aie
=
pad
—

P va AN ie as A ‘s i 5 ry VA
f Ai\ AA AAA | eal JAR es N Alia! Ree! ME wal) i ANAnANa f Ey
AVN AN MA AAR BA | san) mg A
WAAAAAnaaA ARADA | Wn, , AaAWAnannnnrn : ana

i NARA ‘AA AAAS AAN IAT AN MARARA WAS ~

AA fp: jm A .
A AATAA al
AAA

|

the 2 23>

P\peN
\ wm aN [\IX" - PW ENA

' AP A ~\ ‘ i ! / AVA \ \ AP AAR , . A AA AA 7. | AN A \ 4 eel" y ’ Ap : AA wy Al ¥

HAR; ABA ARARA AAA AAAAAN“AAAL An SANA ‘aaa APS AN RAIA Nvarnan’ an AR ‘aary
| . : | Na =! NAN oN

. AW AAAVNAVAVAA al : |

Aan ag WAAR AAAAA Aa AA ne

lay:

AAA nanan

SERNAME Ane

GEOLOGICAL SCIENCES
LIBRARY

AA ; ANA MAAN naar an x -
| AAAAAARA,
Ann nny Biak
AIAN A.” ARARANS A Af
| Va ANA
DAAAN AAAAAA
An \nh\a AA AAA
A Anh
BWW Ww \nt\ ay AN aan xan
En Annrat | Ah AA iaae ates
pene One ; Nala MAINA ARS
ala An/\ AN NAAR
A! Y Wee val Ay atte!

THE

GHOLOGICAL MAGAZINE:

OR,

Monthly Journal of Geology :

WITH WHICH IS INCORPORATED

“THE GEOLOGIST.”

NOS. CCLIX. TO CCLXX.

EDITED BY

HENRY WOODWARD, LL.D., F.R.S., F.G.S., F.Z.8., F.R.M.S.,

OF THE BRITISH MUSEUM OF NATURAL HISTORY;

VICE-PRESIDENT OF THE PALAONTOGRAPHICAL SOCIETY,

MEMBER OF THE LYCEUM OF NATURAL HISTORY, NEW YORE; AND OF THE AMERICAN PHILOSOPHICAL
SOCIETY, PHILADELPHIA; HONORARY MEMBER OF THE YORKSHIRE PHILOSOPHICAL
SOCIETY; OF THE GEOLOGISTS’ ASSOCIATION, LONDON; OF THE GEOLOGICAL
SOCIETIES OF EDINBURGH, GLASGOW, AND NORWICH ; CORRESPOND-

ING MEMBER OF THE GEOLOGICAL SOCIETY OF BELGIUM; OF
THE IMPERIAL SOCIETY OF NATURAL HISTORY OF
MOSCOW; OF THE NATURAL HISTORY SOCIETY
OF MONTREAL; AND OF THE MALACO=-

LOGICAL SOCIETY OF
BELGIUM,

ASSISTED BY

ROBERT ETHERIDGE, F.BS. L. & E, F.GS., F.C8., &.,

OF THE BRITISH MUSEUM OF NATURAL HISTORY.

WILFRID H. HUDLESTON, M.A., F.R.S., F.G.S.
AND

GEORGE J. HINDE, Pu.D., F.G.8., &c.

NEW SERIES. DECADE III. VOL. III.
JANUARY—DECEMBER, 1886.

LONDON:

TRUBNER & Co., 57 anv 59, LUDGATE HILL.
F. SAVY, 77, BOULEVART ST.-GERMAIN, PARIS.
1886.

HERTFORD:

PRINTED BY STEPHEN AUSTIN AND SONS.

THE
GEOLOGICAL MAGAZINE
DECADE III, VOL. IIL.
JANUARY—DECEMBER 1886.

aie” any re (vie
HHITADAM 1 £01 nade

| ee |

a) <=rit SOF?

eet: SERMAD
id

tH AMAL

LIST OF WOODCUTS.

Part of spine of Edestus Heinrichsi: ?

Pectoral spine of Aspreds levis
a3 5, Doras, sp. -
” 3, Leecopterus, sp.

Dorsal spine of Hybodus

Didymograptus vacillans, Tullberg
Dicellograptus Forchhammeri, Geinitz «
Dicranograptus ramesus, Hall .

Pterograptus dilaceratus, sp. Dov.

Tetragraptus approzimatus, Nich.

Dichograptus Scdgwickii, Salter -
Pe octobrachiatus, Hall .
os Kjerulfi, Herrmann

Clonograptus multiples, Nich. -
Diagram, Talus of Cliff .

.

.

Palatal Teeth of Carboniferous Fishes

Fruiting organ of Williamsonia Morieri, Sap. -
Goniolina, after Sap. and Marion

33 33

Sections of Igneous Rocks of Stanner -

Pitchstone Vein at Chiaja di Luna, Island of Polen .

Tooth of Notidanus gigas, Sismonda

> 29
3, LMorosaurus

3, Schidosaurus .«

3, Lodrosaurus

3» Lgvanodon Prestwichi
3» Craspedodon lonzensis «
Section through North America

Section near Honiton, Devonshire -
Eophyton ? explanatum, Hicks, and Hyalonema mirabile, Gray
Azosmilia elongata, Duncan

Catopsalis polluz
Ptilodus medigvus
Esthonys Burmeistert
Hyopsodus vicarius

Ueneghinii, Lawley «

.

Vill List of Woodcuts.

Anaptomorphus homunculus . . « «© + + «6 «© «

39 EIMNULUS oat metic aetutts! Fife), (eer iatecunenins
Diagram of Troostocrinus Reinwardi . . .« « «
Diagram showing arrangement of Basals in Platycrinus

», to show the position of the ridges of Stephanocrinus angulatus

Skeleton of Iguanodon Bernissartensis, Boulanger
Periptychus rhabdodon . .. ». «© «© 6 « «© «© «¢
Brain of Phenacodus primevus

Skull of Coryphodon elephantopus

Loxolophodon cornutus . . Se Wee che)
Striated Pebble from the Salt nee 0

LEROMOPO UWE =o 0 6) 0, Oo Oo oO
Enhydrocyon stenocephalus Se catyrsl rey ame amoeartsy crs
Nimravus gomphodus Cit Liha ORAM ECCI D HMI. IO
Pogonodon platycopis Se Laie

Section at New Entrance to Cae Gwyn Cave

Section in Cae Gwyn Cave, near New Entrance

Section in Cae Gwyn Cave, about 16 ft. from New Entrance

LIST OF PLATES.

PAGE

Se IRMPECSTU SMD AUISTY EL WiOOU Wael) “ey isi Wes te et teks 1
vy II. Skeleton of Phenacodus primevus, Cope. « + »« « « « = 49
waeiienvecent and Kossil Hippopotami =: 5 << 5 . «= « « « 114
even Eosst Ostracoda irom: Colorado! ye) ee 5 cele te 145
© Wo MionetonbionGn anise 955 oo ino oo ac 193
Wav lemhossileNotidanidse Vays ks ke eS eee es ee, 208
Pale arboniierous: Ostracoda.) 6 «i ee 2 es 248
v VIII. Desmidopora alveolaris, Nicholson. . . . «© «© «© «© « « 289
_ IDS. Gilitinaks Tigi jing 6 GG GG Fo 6 5 6 6 4 342
ecm linterion Oolite Madreporaria, = 0. 9. <6 «| « i «| 885
7a len @acponiterous Ostracoda, (2 | ws ew 433
ellen Carboniferous: Ostracoda, i) sl | sea sue se ee 433
» XIII. Augen-Gabbro, Karakclews, Lizard, Cornwall . . . . - . 481

y XIV. Organisms in Carboniferous Shales, Forestof Dean. . - . . 529

vv

XV.

Ditto ditto ditto al ae hey coer 52S

ideeagapaanared € %, A (aon nth *v ; a na f t - b : :
P ld yaeade 4 : ’ } : " { a ce

wae bY
(Cm a@e ib cooptacienll Tania 4 bo ties eee
ahi. den UR AS oe Dad of Dent he peed “ ei
. Ne ee) eee si od danaala dame F Hi
Cian al Trea bi hon Oe arena ge or 4 , i;
Peay rat ail Penney od ; * fh Pk ke ys og “a, i.
ee eee cee Dcgaanl oats Sen eh Arka ae .
Bs) ee yas ree hie a ie yah
Eat neti eure mo, Tae
dee! Vl Ge sia i Rae) ye Ate
Papa ten ike i ’ ya ae hina e
;, si jae cf P, ee 8) ere whoo et Aiaien. ets
ih ees ethan oy <a le Pa ee ;
meld Wau te Prk Rive, Reais? Sop ahaa taal
pial at Cae MWaryer me OS LOVA,
ter. ie)

Geol.Ma§.1886. Decade lIL:Vol I. PL.I.

La

lh

E.C, Woodward delet lith. West, Newnan &Co.imp.

EHdestus Davisu,H.Woodw.
Carboniferous: Western Australia,

THE

GEOLOGICAL MAGAZINE.

NEW SERIES = DECADE, hia VOE, iil.
No. I—JANUARY, 1886.

Orem IN Atte) Ata Cae eee

—

I.—On A RemMarKABLE ICHTHYODORULITE FROM THE CARBONIFEROUS
SERIES, Gascoynr, WxESTERN AUSTRALIA.

By Henry Woopwarp, LL.D., F.R.S., F.G.S., ete.
(PALE Ie)

A years ago, Mr. Robert H. Scott, F.R.S., Secretary to the

Council of the Meteorological Office, kindly sent me a letter
from the Rev. J. G. Nicolay of Fremantle, Western Australia,
accompanied by a photograph of a fossil, the original of which had
been found by Mr. Davis ‘“‘in the valley of the Arthur River, an
affluent of the Gascoyne.” ?

I readily identified the fossil photographed as the impression of a
fish-spine, similar in form, but more highly curved than those
discovered in the Coal-measures of Arkansas, Indiana and Illinois,
originally described by Prof. Leidy as a fish-jaw, and named by him
Edestus vorax in 1855, and later as a fish-spine by MM. Newberry
and Worthen (Geological Survey of Illinois, 1870, vol. iv. pp. 550-
3638, pl. i.). Having expressed a wish to see the fossil itself, Mr.
Scott at once wrote to his sister, Lady Barker, wife of the Governor
of Western Australia, at Perth, who most kindly interested herself
to obtain the loan of it from Mr. Nicolay. After a protracted corre-
spondence, Mr. Edward T. Hardman, F.G.S., of the Government
Geological Survey of Ireland (who was at that time engaged upon a
Survey of the Kimberley District, Western Australia), was, upon his
return to England, entrusted with the charge of this unique specimen,
which is now in my hands.

The fossil (which is represented in our Plate I. of the natural size)
consists of the half of a heavy clay-ironstone nodule, having the
intaglio impression of a curved organism; the relievo half of the
nodule was not found. It was picked up by Mr. Davis “in
the valley of the Arthur River, an affluent of the Gascoyne from
the right, z.e. the north, above the confluence of the Lyons with the
Gascoyne, and about 130 miles in direct distance from the sea; both
rivers have, as I am informed, cut their channels through a flat-
topped range, which stretches beyond the Lyons to the north-west,
and on the top of which are found fossils very numerous, bedded in
limestone, among which a striated-winged Spirifer ” (probably
Spirifer vespertilio, G. Sby.?) “is prominent. It may be assumed
that the limestone bed is superior in position to that of the ferrugi-

1 Spelt, in some maps, ‘‘ Gascoigne.”
DECADE III.—yOL. I1.—NO. 1, 1

2 Dr. H. Woodward—Note on an Ichthyodorulite—

nous concretionary sandstone” (clay-ironstone) “in which the fossil
was bedded” (extract from Rev. J. G. Nicolay’s letter to Lady
Barker, Government House, Perth, W.A., 13th July, 1883.)

A carefully-prepared cast from the natural mould of the fossil
shows us in relief the curved outline of what may be estimated as
about three-fourths of the entire spine of a fish closely related
to Hdestus Heinrichsii, of Newberry and Worthen, from the Coal-
measures of Belleville, Illinois, but of much smaller dimensions, less
robust, and more highly curved than the American species.

We see in the Australian fossil 14 perfect flattened lancet-shaped
denticles, the cutting edges of which are crenulated along each
border (like the teeth of many of the Plagiostomous fishes) the
denticles being closely set along the outer curve of the spine, and
touching each other at their broadest expansion. They increase
gradually in size from one extremity of the fossil to the other. The
smallest denticle measures 3 lines in breadth, and 7 lines in length ;
the largest is 5 lines broad, and 11 linesin height. There is evidence
of the bases of one more denticle at the smallest end, and two more
at the largest end of the spine. The outer curve (which forms the
segment of a nearly true circle of 44in. diameter) measures around
the points of the denticles 6%in., and on the inner margin of the
spine (following the curve in each case) 34 in. The breadth of
the spine with its denticle at the broadest end is 16 lines; and at the
narrowest end 11 lines. The character of the American Hdestus is
that the shaft of the spine is segmented throughout, and breaks up
into curved portions, each bearing a denticle; these segments over-
lap to such a degree that the bases of the denticles are seen to curve
beneath each other, forming a series of raised imbricated ridges on
the sides of the spine, each curved ridge leading up to the base of
a denticle, as admirably shown by Prof. Leidy in his original paper.
The substance of the shaft of the spine of the Australian fossil must
have been much less massive than the American form, but was
evidently, like it, highly enamelled along its outer convex toothed
border, the hollows of the cast being all finely glazed.

In the Proceedings Acad. Nat. Sci. of Philadelphia, vol. vii. Oct. 30,
1855, p. 414, Dr. Joseph Leidy gives the name Hdestus vorax, to a
new genus of fishes, founded on a supposed fragment of a jaw with
portions of four teeth. In the Journal of the Acad. Sci. of
Philadelphia, Nov., 1856, 2nd ser. vol. iii. p. 159, Dr. Leidy
describes the specimen more fully, and figures it on plate xv.
“The fragment of jaw is six inches in length; and it measures
three inches in depth from the dental border. The sides are
symmetrical, and slope divergently from the latter position towards
the base, which is convex and moderately keeled in the median line.
At the dental border the jaw is about seven-eighths of an inch in
thickness, and at the thickest part of its base measures one inch
and four-fifths. Longitudinally the base of the jaw is slightly
concave and furrowed. The surface of the bone is covered with
fine vermicular, reticulating, broken ridges, assuming a striking
resemblance to Arabic writing. The most remarkable peculiarity

Strom the Carboniferous of Western Australia. 5)

of the jaw is its segmented character ; and of the segments the
fossil retains two very nearly perfect ones with portions of two
others. Each segment in outline forms an irregular pentahedron ;
and each possesses a single codssified tooth, whose broad surfaces
abruptly increase the acclivity of the sides of the jaw.”

This specimen is most probably from the Carboniferous series,
and was found at Frozen Rock, Arkansas River, 20 miles below
Fort Gibson, in the Indian Territory.

Prof. J. S. Newberry describes a much smaller specimen, under
the name of EHdestus minor, in the Geol. Surv. of Illinois, vol. ti. 1866,
p. 84, and gives a figure on plate iv. fig. 24. This figure repre-
sents one tooth only, 10 lines long, and 54 lines wide at base, and
3 lines thick, set saddle-like upon the edge of a flat, bony jaw. This
specimen was obtained from the Coal Measures, Posey County,
Indiana. In vol. iv. of the same work, at p. 350, Newberry and
Worthen describe and figure, pl. i. fig. la, 1b, another specimen
under the name of EHdestus Heinrichsii, from the Coal Measures of
Belleville, Illinois. The following is the description given by
Messrs. Newberry and Worthen of Hdestus Heinrichsii, N. & W., .
1870 :'—*‘Spine robust, one foot or more in length, by two and a half

YY

2 > car
Fic. 1.—Part of the spine of Edestus sp? (E. Heinrichsit?), Coal M., Indiana.

inches wide, and one and a quarter inch thick, composed of dense,
bony tissue, symmetrically flattened, with an ovoid section below ;
lenticular above; one margin nearly straight, the other gently
arched ; the basal end irregularly rounded off; the arched border
set with nine large, triangular, flattened, doubly crenulated,
enamelled denticles, each about an inch in height, the upper
half of the straight line forming a sharp cutting edge. ‘The
denticles of the arched border are broadly triangular in outline,
rising perpendicularly from the curved edge on which they
rest, each three-quarters of an inch in height, by one and a quarter
inch in breadth, compressed laterally, with crenulated cutting edges.
They are contiguously placed, and each is embraced by the acute

1 Geological Survey of Illinois, vol. iv. Geology and Paleontology, 4to, Illinois,
1870, pp. 350-353, pl. i. figs. 1aand 14. Some confusion exists in the references to the
figures here ; for of the two species drawn on the plate, the one named #. Heinrichs

agrees best with Leidy’s original figure ; whilst the one named L. vorax, which agrees
with our woodcut (supra), has much larger denticles.

4 Dr. H. Woodward—Note on an Ichthyodorulite—

prolongations of the enamelled base of the superior denticle, which
reaches back to its middle point. The spine is segmented throughout,
each segment bearing a denticle; the segments overlapping to such
a degree that the one bearing the superior denticle reaches two-
thirds of the distance from the summit to the base of the spine.”

A comparison of the Australian fossil spine with the American
species of Hdestus (excellent casts of both of which are in the
British Museum, Natural History) has convinced me that its true
place is in or near to Leidy’s genus. The denticles are placed
on the convex edge of the spine, a peculiar feature in the genus
Edestus, nearly all the spines of fossil plagiostomous fishes being
denticulated along the inner concave curved edge.’ The imbricated
curved lines passing from each denticle obliquely across the shaft of
the spine are also seen in both, and are quite peculiar to Hdestus.

Prof. Newberry has clearly pointed out the objections to the theory,
at first suggested by Prof. Leidy, that Hdestus was part of the
mandible of a plagiostomous fish. He mentions that “the jaws of
sharks are always cartilaginous, holding the bony and enamelled
teeth only by ligamentous attachments, so that in a fossil state the
jaws have usually disappeared, and the teeth are scattered, whereas
in Hdestus we have a dense bone to which the tooth-like denticles
are united by a firm bony anchylosis.” Again, “The form of the
fossil is wholly unlike that of any jaw of fish, reptile, or mammal
known, being rounded below, and terminating in an acute point,
smooth, even polished, and evidently never having been covered
by integument.”

In comparing the Australian fossil with various specimens in the
collection, Mr. William Davies drew my attention to the similarity
in arrangement of the teeth of Janassa bituminosa, from the Permian
of Durham; in one specimen of which six teeth with prolonged and
highly-curved bases may be seen united; but these teeth differ in
arrangement from the denticles of Edestus in being placed broad-
wise behind each other, not edge-to-edge in a row, as in Hdestus.

The only structure amongst fossil fishes strikingly analogous to
Edestus is to be found in the pectoral fins of the genus named by
Agassiz Ptychodus, from the Chalk of Sussex, and since described
by Prof. E. D. Cope from the Chalk of Kansas, under the name of
Pelecopterus.

Professor Cope writes :—‘ The entire pectoral fin, so far as is
known, is devoted to the construction of a powerful spine. This
follows from the fact that the spine is supported by all the
basilar bones. Six of the latter articulate in the fosse of the groove
of the scapula. They are flat, contracted at the middle, and ex-
panded at the extremities. In front of these are two others of a
short, thick, cylindric form, one applied to the superior, the other
to the inferior facets of the scapula above mentioned, while the
tuberosity rises pedestal-like between them. This structure gives a
slight hinge-movement like the opening of the blade of a knife, and

1 Tn Plewracanthus the spines are barbed on both edges, and so also are the spines
of the Sting-rays.

From the Carboniferous of Western Australia. 5)

entirely unlike the rotary hinge-movement characteristic of the
pectoral spines of Siluroid fishes.”

«The spine is composed of parallel rods in close apposition. The
anterior edge being oblique, the extremities of the rods terminate
successively at the border, which is trenchant, constituting the
offensive part of the spine. The edge is hardened, and the adjacent
parts of the spine thickened, and in some cases roughened by a
deposit of a hard substance resembling enamel. It is either straight
or regularly undulate or serrate, with recurved, acute, tooth-like
processes. The smaller species exhibit the serrate character, the
larger the regular border. In either case a most formidable weapon
is indicated, not less admirable than those already described from
Paleozoic rocks. There is a considerable resemblance between the
serrate type and the spines of the Carboniferous genus Edestus, in
which the teeth are more developed and denticulate.” (EH. D. Cope.
Report of the United States Geological Survey of the Territories.
F. VY. Hayden, U.S. Geologist-in-charge, vol. ii. p. 2448. Ato.
Washington, 1875.) (See Woodcut, infra, Fig. 4.)

Fig, 2. Fig. 3.

Fic. 2. Pectoral Spine of Aspredo levis ; (recent) Surinam.
95 Bi 3 % Doras, sp. S. America.

Pelecopterus, sp.. Chalk, Sussex.
55 : Dorsal Spine of Hybodus, Wealden, Sussex.

6 Dr. H. Woodward—Note on an Ichthyodorulite.

Amongst recent plagiostomous fishes I do not find any one species
with spines at all comparable in the least degree with the type of
Edestus. If it be permissible to interpret the Australian fossil to be
the impression of the spine of the pectoral fin of an Edestus-like
fish, there are numerous examples of living Siluroid fishes with
powerful pectoral fin-spines, some of which at least have denticles
upon the outer as well as the inner edge of the spine, although none
are so highly curved as the Gascoyne fossil. Arius rita, of the river
Ganges, has denticles on both edges of its pectoral spines; so also
has Aspredo levis (Woodcut, p. 5, Fig. 2), from Surinam ; Synodontis
omias, and Auchenaspis falcarius, from West Africa; Arius falcarius,
Formosa; and Silurus glanis, from Lake Derkos; Doras, sp., from
South America (Woodcut, p. 5, Fig. 3), and many others.

It is difficult to imagine any fish with a pectoral spine curved to
so great a degree as is this Australian ichthyodorulite, but on the
other hand it seems improbable that it was a median dorsal defence.

To quote again from Prof. Newberry :—‘‘The segmented structure
of the fossil is its most marked and anomalous feature, but one
equally so, whether it be considered spine or jaw, and for which no
parallel suggests itself. It is undoubtedly to this structure that we
must ascribe the absence of a large medullary cavity, as each
segment seems to have been nourished somewhat independently of
its fellows.

“Tt is also evident that this spine was implanted in the integu-
ment at a low angle, and that an investing skin or other nutrient
tissue covered fully half its surface, on the lower portion reaching
up to the enamelled bases of the denticles. This is the relative
position of the defensive spines of Rays, to which an analogy is
suggested by this character.

“In some plagiostomous fishes, a bone is found quite buried in the
integuments of the back, and which is a rudimentary representative
of a posterior dorsal fin; it is, therefore, not impossible that we
have in the fossil before us, a higher development and special
modification of that organ.” (Newberry and Worthen, op. cit. p. 852.)

Referring again to the valuable and suggestive memoir by Prof.
E. D. Cope on Pelecopterus quoted above (p. 4), I cannot but think
that it affords the most probable explanation of the anomalous
structure in Hdestus.

“The entire pectoral fin,” says Cope, “so far as it is known, is
devoted to the construction of a powerful spine.” ‘The spine is
composed of parallel rods in close apposition. The anterior edge,
being oblique, the extremities of the rods terminate successively at
the border, which is trenchant, constituting the offensive part of
the spine.”

It appears to me to be only necessary that the ‘ parallel rods’
composing the spine of Pelecopterus should be bent into curves,
corresponding to the segmentation seen in Hdestus, and we at once
have a solution of the peculiar structure in the latter.

If this interpretation be accepted, then Hdestus must be deemed to
be, like Pelecopterus, a modified pectoral fin-spine, composed of a

G. H. Kinahan—Irish Metamorphic Rocks. 7

number of parallel rods in close apposition, but highly curved in
the former ; the anterior edge in both being oblique, the extremities
of the rods terminate at the border, constituting with its dentated
edge the offensive part of the spine.

Without attempting more on the present occasion than to point
out the interesting analogy between the Australian fossil and the
American genus Hdestus, it seems, nevertheless, of the greatest
interest to call attention to the probable nature of this organism
and its geological age.

So lately as June 6th, 1883, Mr. W. H. Hudleston, F.R.S., F.G.S.,
communicated a paper to the Geological Society of London, “On a
Collection of Fossils and of Rock-Specimens from West Australia,
north of the Gascoyne River,” since published in the Quart. Journ.
Geol. Soc. vol. xxxix. pp. 582-595, pl. xxiii.

In this paper Mr. Hudleston mentions an earlier paper by Mr.
F. T. Gregory in 1861, and a map and sections presented to the
Society in 1847. ‘The paper and sections by Mr. Gregory must
be regarded (says Mr. Hudleston) as having laid the foundation of
Western Australian Geology south of the parallel of the Gascoyne
river.” ‘Mr. Forrest, the Colonial Surveyor, appears to have
discovered a range, or more properly a sort of continuous out-
crop trending N.N.W. for nearly 150 miles, which has yielded an
interesting suite of Carboniferous fossils.” A list of about 32 species
is given by Mr. Hudleston, namely, 5 Corals, 2 Kchinodermata, 4
Polyzoa, 8 Brachiopoda, and 2 Lamellibranchiata. It is not with-
out interest in connection with the present discovery of a Fish-spine
in this region closely related to the American Hdestus of Leidy, that
two species of Evactinopora are described, one of which is said to be
similar to Meek and Worthen’s Evactinopora grandis and is also,
like Hdestus, from the Carboniferous of Illinois (see Hudleston, op. cit.).

I have been requested to append the discoverer’s name to this
fossil, and as I am unwilling, in the present state of our knowledge,
to make a new genus for its reception, I propose to name it Hdestus
Davisii.

EXPLANATION OF PLATE I.

Fie. la. Pectoral fin ? spine of Edestus Davisii, H. Woodw. (nat. size), from the
Carboniferous Series of the Gascoyne District, Western Australia.
1d. Conjectural outline section of spine.

IJ.—IrisH Mreramorpuic Rocks.
By G. H. Kinauan, M.R.I.A,, etc.
Read at British Association, Aberdeen, 1885.

HE meeting of the British Association in Montreal gave different
Irish geologists facilities for examining the Archzean rocks of
Canada and the States, while since then they and also American
ceologists have had opportunities for studying the Irish Metamorphic
rocks; it may therefore be allowable to give an epitome of our
knowledge in regard to the latter.
In ten localities in Ireland are found metamorphic rocks more or
less similar to those of America; these localities may be classified as

8 G. H. Kinahan—LIvrish Metamorphic Rocks.

follows :—1st, Boylagh and Kilmacrenan, Co. Donegal ; 2nd, Tirhugh,
Co. Donegal; 3rd, Erris, Co. Mayo; 4th, Slievezamp and Ox
Mountain, Cos. Mayo, Sligo, and Leitrim; 5th, Charlestown district,
Co. Mayo; 6th, Slievegallion or Pomeroy district, Cos. Tyrone and
Derry; 7th, Cary or Ballycastle district, Co. Antrim; 8th, Yar-
Connaught or West Galway; 9th, Croaghankinshella, Cos. Wicklow
and Wexford; and 10th, Carnsore, Co. Wexford.

Boylagh and Kilmacrenan.—These are the northern baronies in the
county of Donegal, across which obliquely a tract of granitic rocks
extends, having outlying patches in Rossgull and Fanad, in the latter
barony. In connection with the gneiss there are some remarkable
peculiarities which as yet have not been explained ; but as the country
has still to be completely explored, it seems expedient only to say
that the Americans seem to consider the gneiss and associated schists
of Lackagh valley to be lithologically identical with the American
rocks of Mt. Alban series (Hitchcock) or Hudson River series (Dana),
as seen in the vale of the Schuyllkill river, Pennsylvania ; and these

American rocks they consider to be the equivalents of the English
Ordovician or Lower Silurian. Immediately south of the gneissoid
rocks supposed to be Laurentians, there is a long tract of rocks
which lithologically are identical with some of the Ontario
Laurentians, much more so than any of the gneissose rocks; they,
however, have been ignored. To the main tract of gneiss in the
barony of Kilmacreenan, in any place, either along the north-west
or south-east of its limits, there are no hard boundaries to indicate an
unconformability or fault boundary, as along these boundaries the
gneiss graduates into schists, and the latter into submetamorphic rocks ;
to the south-east, however, the graduation is, in general, more rapid
than to the north-west.

Tirhugh.—This tract is situated to the N.W. of Pettigo, in the
south portion of the Co. Donegal. The rocks partake very much of
the lithological characters of some of the Ontario Huronians and
Laurentians, but up to the present time they have not been claimed
as Irish Laurentians. In former writings I have suggested that they
are probably the representatives, either of the Passage beds between
the Ordovicians and the Cambrian, or of the Upper Cambrians.

Erris.—This is a portion of North-west Mayo. The gneissose
rocks have no well-defined boundaries ; neither has there been found
in connection with them an overlying unconformable conglomerate,
as has been believed by some, on account of the wording of their
published descriptions. _In former papers (Royal Geol. Soc. Ireland)
I have suggested that these rocks are metamorphosed Cambrians,
but no positive statement can be made as to their age; lithologically
they are similar to the metamorphosed Cambrians of the Co. Wexford,
but they are also very like some of the American Laurentians.

Slieve Gamp and Ox Mountains —These rocks occupy a long
narrow strip which extends from north-east Mayo, across Sligo into
the county of Leitrim. Some of the rocks are peculiar, as they occur,
similarly to the Norians of the Province of Quebec, as intrusive masses,
into which a coarse foliation has been subsequently introduced. The

G. H. Kinahan—TIrish Metamorphic Rocks. 2

assemblage appears to be the north-easterly extension of the rocks
of West Galway; elsewhere I have suggested that they are probably
either metamorphosed Ordovicians or Upper Cambrians.

Charlestown District.—This small exposure occurs near the north-
east boundary of Mayo; the rocks are more or less similar to those
in Tirhugh, but so few of them are exposed that it is difficult to
form an opinion as to their age; for the reasons given in a paper
read before the Royal Irish Academy, I have suggested that they may
be either of Upper Cambrian or Ordovician age, probably the latter.
As yet they have not been claimed as Laurentians.

Slieve Gallion or Pomeroy District.—This area is principally in
the Co. Tyrone, only a small portion extending into the Co. Derry.
The opinions in regard to the age of the rocks have undergone
sudden and extraordinary changes. First, they were mapped as
of Lower Silurian age, and when I showed that this classification
must be incorrect, it was again insisted on; but subsequently this
opinion was suddenly ignored, and they were stated to be of Laurentian
age. Lithologically many of these rocks are very similar to some of
the Canadian Huronians, and if there are any Archean rocks in
Treland, they probably occur here, as the rocks are evidently much
more ancient than the Ordovician to the south, while they appear
to be older than the submetamorphic rocks to the northward in the
Co. Derry; however, for reasons given elsewhere, I suspect that
they are metamorphosed Cambrians.

Cary or Ballycastle District.—These rocks occupy a tract at the
extreme north-east of Ireland, in the Co. Antrim. They seem to be
the north-east extension of the Slievegallion rocks, and to be of a
similar age, having been heaved northward by the great faults of
the Lough Neagh basin. As yet they appear to have escaped the
general confiscation.

Yar- Connaught or West Galway.—This tract lies immediately north
of Galway Bay. The age of these rocks is very apparent, they
rest on a great anticlinal curve, the axis of which dips westward,
thus bringing up the oldest rocks to the westward, in the hill group
called Bennabeola. Some of the older rocks are lithologically identical
with the Laurentians of the district of Chelsea, Province of Quebec.
Yet these older rocks of Bennabeola have not been claimed as
Laurentians, although the younger rocks to the southward have
been — although the latter, from their fossils in the unaltered
portions, appear to be the equivalents of the English Llandeilo and
Bala series.

Croaghankinshella.—Here the highly altered rocks occupy a small
tract at the meeting of the counties of Wicklow and Wexford, and
if lithological characters are conclusive, they ought to be included
among the Irish Laurentians, which up to the present has not been
done. Northward they have a hard boundary; southward their
margin is obscured by superficial accumulations, but eastward and
westward they graduate into the rocks belonging to the upper
divisions of the Irish Ordovicians.

Carnsore.—This is a small tract at the §.W. extremity of Ireland,

10 MM. Rutot § Van den Broeck—Age of the ‘ Tuffeau de Ciply.’

in the Co. Wexford. The rocks therein have not been claimed as
Taurentians by Dr. Hull, although some have been so classed by
Dr. Callaway. All the rocks are evidently portions of one group.
To me it would appear that unquestionably they belong to the
neighbouring rocks, which by their fossils are proved to be of
Cambrian age.

The sole evidence for the existence of Laurentian rocks in Ireland
is the lithological characters of the rocks; and if such characters
are of value, they ought to be of equal value in every case. ‘This,
however, is not the case, as in many places rocks lithologically
more or less similar to the American Laurentians are left out in the
cold; while in other places younger rocks, whose age is indicated
by their fossils, are included.

IiI.—Tue Turreau DE CIPLY SHOWN TO BE CHIEFLY OF TERTIARY AGE.
By MM. A. Ruror and E. Van pen Brock.

E wish briefly to state an important result, which the study of
certain Tertiary and Cretaceous beds in the neighbourhood of
Mons has enabled us to arrive at.

For a long time past, the beds, well known in the district just
mentioned, by the name of Zuffeau de Ciply, have been considered
by all geologists to be the equivalents of the Maestrichtien, that is
to say, as belonging to the highest subdivision of the Cretaceous
series of Belgium.

Now, our recent researches have convinced us that in the group
of beds called the Zuffean de Ciply, there have been confounded two
series quite distinct trom each other:

A. A lower fossiliferous series of slight thickness, extremely rich
in characteristic Cretaceous species, amongst which may be men-
tioned specially Thecidium pupillatum and Belemnitella mucronata.
We propose to give to this inferior tuffeau, which appears to cor-
respond to certain horizons of the Upper Cretaceous (Maestrichtien)
of Limbourg, the name of Tuffeau de St. Symphorien, from the locality
where it may, at present, be best observed.

ZB. An upper series, with fossiliferous zones, devoid of Cretaceous
species,’ but containing, on the contrary, a fauna with a Tertiary
facies, including numerous forms identical with those of the Calcaire
grossier de Mons. This series, which attains a thickness of nearly
twelve metres, constitutes the type of the deposit known by the
name of Tuffeau de Ciply. Its base is formed by a conglomerate
called the Poudingue de la Malogne, which, in certain localities, con-
tains numerous rolled Cretaceous forms derived from the underlying
formations.

The preceding data have been derived from stratigraphical and
paleontological observations, which show, furthermore, that there
exists an insensible passage between the Eocene formation known
as the Calcaire grossier de Mons and the Tuffeau de Ciply, by the

1 Nevertheless, two Maestrichtian forms, Thecidium longirostre, Bosq., and Aryiope
microscopica, Schloth., have passed up into the Hocene Zuffeaw de Ciply.

W. 8S. Gresley—A Modern Ferruginous Conglomerate. 11
intervention of a deposit called the Calcaire de Cuesmes a grands
Cerithes. On the other hand, a well-marked separation exists
between the Zuffeau de Ciply and the underlying Cretaceous tuffeau
with Thecidium papillatum.

Our paleontological proofs are founded on the presence of nearly
a hundred species, for the most part casts or impressions, collected
in the Zuffeau de Ciply, from its base upwards, among which species
there exist only a very few Cretaceous fossils, and these rolled,
evidently derived from the underlying beds, in contrast with a rich
fauna having a Tertiary facies, consisting of Gasteropods, Lamelli-
branchs, Corals, ete., amongst which may be distinguished species
either identical with those of the Calcaire de Mons, or nearly allied
to them, associated with numerous forms probably new.

A general examination of the smaller organisms, such as Fora-
minifera, Polyzoa, etc., leads us to believe that their comparison
with the microscopical fauna. of the Calcaire de Mons will lead
to conclusions similar to those which we have arrived at from a
comparison of their molluscan fauna.

We intend shortly to publish, in the Bulletin du Musée d’histoire
naturelle de Belgique, a Memoir setting forth in detail the results
that we have now briefly stated, and which modify in an unexpected
manner the stratigraphical position of the line of separation of the
Cretaceous and Tertiary formations of Belgium.

I1V.—On «a Moperrn Ferrrucinous ConGLoMERATE UPON ASHBY
Wotps, LreIcesTERSHIRE.

By W. S. Grestey, F.G.S.

URING the summer of 1885, in excavating for a small reservoir
for colliery purposes at Moira, three miles west of Ashby-de-la
Zouch, an interesting deposit of a kind of Limonite Iron-ore was
met with, the following description of which may interest some of
the readers of the GroLocicaL MaGazine.

The bed occurred about five feet below the surface soil, near a
small stream, at a place called ‘“‘ Hanging Hill” [see Geol. 1-inch
Map, Quarter-Sheet No. 63, N.W.]. In thickness it hardly reached
a foot, but its extent was not proved; it rested unconformably
upon stiff blue clay of the Coal-measures, and was overlaid by
yellowish clay, loam, sand, etc., unstratified, containing a few pebbles
and other drifted matter; it was principally composed of nodules
and fragments of nodules of earthy yellowish brown ironstone, of
similarly formed pieces of very hard and compact light grey siliceous
stone having a thin crust or shell of compact dark brown iron-ore,
(probably géthite), of sandy nodular masses largely composed of
limonite; of fragments and small nodules of fossiliferous bard red
hematite generally coated with a bright red skin which is often
powdery ; also specimens of compact brown iron ore having a yellow
ochre coating, sometimes the compact red and yellow hematites are
associated in the same sample, the latter variety appears to form

12. W.S. Gresley—A Modern Ferruginous Conglomerate.

a kind of shell to the red ore, though occasionally the two kinds
exist in thin alternating bands. These hard hematite fragments
are sometimes partially composed of quartz grains, and the concentric
zones of oxidation seen upon the surface of the specimen run through
the gritty parts just as they do through those devoid of the quartz
grains. Other specimens observed should, I think, be termed iron-
jasper rather than classed as hematite. The remainder of the in-
cluded pebbles, etc., are chiefly those of quartzite and fine-grained
hard sandstones and slaty rocks of yellow, brown, and green tiuts ;
also small fragments of coal. The size of the fragments in the
deposit range from mere specks to say eight inches in length, and
the whole mass is cemented together into a very hard and often
compact rock by brown iron ore of a semicrystalline siliceous
character. The bed is also fossiliferous, in that it contains bits
of decayed vegetable detritus, amongst which well-preserved nuts
(hazel-nuts) occur. These organic remains are not petrified, but
only browned and blackened, just as we sometimes find Lepidostrobi,
ferns, etc., occurring in a peculiar decayed and carbonised condition
in certain beds of the Coal-measures.

In regard to the derivation of this conglomerate and the way in
which it was probably formed, I may add that the nodular lumps
of earthy iron-ore, as well as the harder limonite-crusted masses,
were originally clay-ironstones, etc., of the neighbouring Coal-mea-
sures ; that the fragments of hard hematite (which are ‘ burnishers’)
have been derived from the outcrop of the Permian breccias by
which the western margin of the exposed Leicestershire Coal-field
is partly overlaid [see Gzoz. Mag. for 1885, p. 833], and that the
quartz and other pebbles, etc., have come from the Bunter series, also
found within a mile or so of the locality of this iron-ore gravel-
bed. The nuts, twigs, etc, were of course buried during the
deposition of the gravel, but the cementing iron-ore, which has acted
chemically so much upon the mass (as evidenced by the staining of
the pebbles and the alteration of the clay iron-stones and other frag-
ments), I consider has been thrown down during a quiet period
subsequent to the deposition of the stones, etc., and was most likely
produced from chalybeate waters issuing from the Coal-measures
close by the bed of gravel; the whole was subsequently covered over,
and thus consolidation resulted.

It need scarcely be added, that the presence of hazel-nuts in the
deposit proves it to be of quite recent date.

Posrscript.—The finding of a rusty iron nail of square section,
in lengh 2} inches, which is thickly, though irregularly, encrusted
with iron oxide and sandy matter, in this deposit, shows it to be of
quite recent date.

I am inclined to think, from the appearance of the locality, that
this iron-gravel occupies what was once the upper or shallow end of
the bed of a mill-pond ; at all events the character of the deposit is
such as we might perhaps expect to find in such a situation.

Dr. Herrmann—On Dichograptide—a Family of Graptolites. 13

V.—On tHe Graprouite Famity Dicnocraptipm, Larw.

By Dr. Orro Herrmann.?
[Translated and Abridged by W. 8. Dattas, F.L.S.]

Sub-order Ruappornora, Allm. Group Grapronitip#, Lapw.
Family Dicnoecrapripm, Lapw.

Hydrosoma bilaterally developed. Branches regular, always fur-
nished only with a single series of hydrothece (Monoprionidian).
Hydrothecee rectangular, touching one another, their inferior margin
slightly curved. Sicula generally persistent ; its free, pointed, down-
wardly directed end at the proximal extremity of the hydrosoma.

In 1851 M‘Coy (Brit. Pal. Foss. p. 9) proposed the generic name
Didymograptus for two-branched species with one row of cells
“sometimes on the inner, sometimes on the outer side of the
branches.” Nearly at the same time Geinitz established his genus
Cladograptus to include all two-armed or furcate Graptolites. These
two denominations have been employed in various senses by succeed-
ing authors, and considerable confusion has resulted. Hall? remarked
that these genera contained at least two distinct types, and proposed
to retain the name Didymograptus for such forms as D. Murchisout,
Beck, and to give that of Cladograptus to Didym. divaricatus, Hall,
and its allies. His genus Dicranograptus applied to forms like D.
ramosus, Hall, may be dropped.

In 1871 Hopkinson® separated such forms as Didymograptus
(Cladogr.) Forchhammeri under the generic name of Dicellograptus.
He adopted Hall’s view of the nature of Didymograptus, abolished the
name Cladograptus as a designation of two-branched Graptolites, and
accepted Hall’s name Dicranograptus. The two-branched Graptolites
were thus divided into three genera :—

Fic. 1. Didymograptus vacillans, Tullberg.
» 2. Dicellograptus Forchhammeri, Geinitz.
», 98 Dicranograptus ramosus, Hall.

1 Abridged from the third chapter of Dr. Herrmann’s paper in the Nyt Magazin
for Naturvidenskaberne, vol. xxix. pp. 124—214. (See also Grou. Maa. 1885, Dec.
IIf. Vol. Il. pp. 406 and 448.)

2 Introduction to the Study of the Graptolites, Albany, 1868, p. 234.

3 Grou, Maa. 1871, Vol. VIII. p. 20, Pl. I.

14 Dr. O. Herrmann—On the Dichograptide—

1. Didymograptus, M‘Coy (belonging to Lapworth’s family Dicho-
eraptide) with such forms as D. Murchison’, Beck and
D. vacillans, Tullb. (Woodeut, p. 15, Fig. 1).

2. Dicellograptus, Hopk. (of the family Dichograptidee, Lapw.)
with such forms as D. Forchhammeri, Gein. (Fig. 2).

3. Dicranograptus, Hall (of the family Dicranograptidee, Lapw.)
with such forms as D. ramosus, Hall (Fig. 3).

To these may be added the still somewhat problematical genus of

the family Dichograptida :—

4. Janograptus, Tullb., with such forms as Janograptus laxatus,
Tullb. (see p. 16).

The following genera are adopted by the author :—

Genus I. Dipymocraprus, M‘Coy.

Hydrosoma bilaterally symmetrically developed, consisting of two
simple branches diverging at an angle of 70°—180°. Sicula well
preserved and always visible. 'The two primordial buds originate in
the neighbourhood of the broad end of the sicula. Lower Silurian.

Species.
a. Type Didymograptus patulus, Hall.

1. Didymograptus patulus (Hall), Nich., Hopk. and Lapw., Brogger.
Graptolithus patulus, Hall, D. hirundo, Salt., Nich. _

Angle of divergence about 180°.

Horizons and Localities.— Quebec Group, Canada; Middle and Upper
Arenig, St. Davids; Skiddaw Slates, North of England; lower part
of the Phyllograptus-shales, Norway; Phyllograptus-shales, Skane
and West Gothland.

2. Didymograptus constrictus (Hall), Linnars., Lapw., Brogg.

Graptolithus constrictus, Hall.

Quebec Group, Canada; Lower Graptolite shales, Skane; Phyllo-
graptus-shales, Norway.

3. Didymograptus eatensus (Hall), Nich., Hopk., and Lapw., M‘Coy,
Brogg.

Graptolithus extensus, Hall.
Quebee Group, Canada; Lower Arenig (Wales) ; doubtfully in
the Lower Bala of Australia; Lower part of Phyllograptus-shales,
Norway.
4. Didymograptus euodus, Lapw. (and Hopk.).
D. eatensus, var. euodus, Lapw.

Hor. and Loc.—Lower Llandeilo, Wales.

5. Didymograptus arcuatus (Hall).
Graptolithus arcuatus, Hall.

Quebec Group, Canada.

6. Didymograptus extenuatus (Hall), Lapw.
Graptolithus extenuatus, Hall.

Quebec Group, Canada.

7. Didymograptus similis (Hall), Lapw.
Graptolithus similis, Hall.

Quebec Group, Canada.

a Family of Graptolites. 15

8. Didymograptus superstes, Lapw.
Lower Bala, Ireland; doubtfully near Albany, N.Y.
9. Didymograptus nitidus (Hall), Nich., Ether., Lapw.
Graptolithus nitidus, Hall. ;
Quebec Group, Canada; Skiddaw Slates; Arenig, Australia ;
doubtfully in Phyllograptus-shales, Norway.
10. Didymograptus suecicus, Tullb., Lapw., Brogger.
Tetragraptus-zone, Skane; Phyllograptus-shales, Norway ?

b. Type Didymograptus Murchisoni, Beck.

11. Didymograptus Murchisoni (Beck), Baily, Tornquist, Hopk.,

Nich., Trom. and Lebesce., Lapw., Tullb.
Graptolithas Murchisoni, Beck, Boeck.
Prionotus (?) geminus, His.

Graptolithus geminus, Scharenb., Kjerulf.
Didymoyraptus furcillatus, Hopk. and Lapw.

Angle of divergence about 40°.

Lower Llandeilo, Wales; Didymograptus-Murchisoni zone (Et. 4.)
Norway, Skane, France, Portugal.

12. Didymograptus indentus (Hall), Hopk. and Lapw., Broégger,
Tullb.

Quebec Group, Canada; Upper Arenig, Wales; Phyllograptus-
shales, Norway ; zone with Tetragraptus, Skane.

13. Didymograptus indentus, var. nanus, Lapw. and Hopk.

D. geminus, Nich.

Skiddaw slates, N. England; Upper Arenig, Wales; Lower and
Middle Llandeilo, Wales.

14. Didymograptus minutus, Tornquist, Lapw.

Phyllograptus-shales, Dalecarlia.

15. Didymograptus bifidus (Hall), Nich. Hopk., and Lapw.,
Brogger, Tuillb.

Angle of divergence 15°—20°.

Quebec Group, Canada; Skiddaw Slates, N. England ; Upper
Arenig, Wales. A somewhat divergent form in Phyllograptus-shales,
Norway; zone with Phyllograptus typus, Skane; Upper Arenig,
N. England.

ce. Type Didymograptus fasciculatus, Nich.
16. Didymograptus fasciculatus, Nich., Lapw.
Upper part of Skiddaw Slates.
17. Didymograptus arcuatus (Hall), Nich.
With a process opposite to the sicula. Quebec Group, Canada.

d. Type Didymograptus pennatulus (Hall).
18. Didymograptus pennatulus (Hall), Hopk. and Lapw.
Angle of divergence nearly 180° (Hall).
Quebec Group, Canada; Lower Arenig, Wales.
19. Didymograptus sparsus, Hopk., Lapw.
Lower Arenig, Wales.
20. Didymograptus gibberulus, Nich., Lapw.
Lower part of Skiddaw Slates, N. England.

16 Dr. O. Herrmann—On the Dichograptide—

e. Type Didymograptus affinis, Nich.

21. Didymograptus affinis, Nich., Hopk. and Lapw., Tornquist.

Angle of divergence 90°-150°.

Skiddaw Slates, N. England; Upper Arenig, Wales; doubtfully
in Phyllograptus-shales, Dalecarlia.

22. Didymograptus filiformis, Tullb., Lapw., Brogg.

Tetragraptus-zone, Skane; Phyllograptus-shales, Norway.

28. Didymograptus Nicholsoni, Lapw., Hopk. and Lapw.

D, serratulus, Nich.

Upper Arenig, Wales; upper part of Skiddaw Slates, N. England ;
doubtfully in Phyllograptus-shales, Norway.

24. Didymograptus pusillus, Tullb., Lapw., Brogger.

Angle of divergence 145°-165°.

Tetragraptus-zone, Skane; ? Phyllograptus-shales, Norway.

25. Didymograptus serratulus (Hall), ? Lapw.

Hudson’s River Group, New York; ? Utica Slates, New York.

26. Didymograptus striatulus, Linnarsson, Nich., Lapw.

Lower Graptolite shales, West Gothland.

f. Type Didymograptus V-fractus, Salter.

27. Didymograptus V-fractus, Salt., Nich., Lapw., Brogg., Tullb.

Skiddaw Slates, N. England; Tetragraptus-zone, Skane; Lower
part of Phyllograptus-shales, Norway.

28. Didymograptus balticus, Tullb., Lapw.

Resembles the preceding. —Angle of divergence 60°-105°.

Tetragraptus-zone, Skane ; Phyllograptus-shales, Norway.

29. Didymograptus Pantoni, M-Coy, Salt., Hther., Lapw.

Skiddaw Slates, N. England; Australia.

30. Didymograptus vacillans, Tullb., Lapw., Brégger.

Tetragraptus-zone, Skane ; Phyllograptus-shales, Norway.

31. Didymograptus, sp. (Hisingeri, Baily). Lower Bala, Ireland.
One of the latest species of Didymograptus.

Genus II. Janocraprvs, Tullberg (Geol. For. Forh. vol. v. p. 314).

From the usually indistinct sicula two branches issue in opposite
directions, or the whole hydrosoma is formed only of one branch.
The sicula is probably pressed into one branch. The angle of diver-
gence is very various. Hydrothece as in Didymograptus.

The genus, which is somewhat problematical, is one of the latest
of the Dichograptide. Its structure shows a remarkable agreement
with that of an irregularly developed Monograptid (M. /obiferus,
M‘Coy), in which a second branch may sometimes be produced.

1. Janograptus laxatus, Tullberg.

Gymnograptus Linnarssoni-zone, Skane. A Janograptus is also
mentioned in other Glossograptus-zones.

Other forms may be regarded as proceeding from a Didymograptus.
The two branches may divide dichotomously, producing a four-
branched form (Tetragraptus) ; or branchlets may issue from the two

a Family of Graptolites. 17

branches (Trichograptus, etc.). The following genera come under
the latter category :—
Genus III. Trrcnocraptus, Nicholson.

Hydrosoma bilaterally subsymmetrically developed. Two prin-
cipal branches on the celluliferous side, with a series of branchlets
which remain undivided. Hydrothec of the type of Monograptus
Nilssoni, Barr.

1. Trichograptus fragilis, Nich., Lapw.

Upper part of Skiddaw Slates, N. England.

2. Trichograptus retroflexus (Brogger).

Bryograptus retrofiexus, Broge.
Upper part of Dictyograptus-shales, Norway.
Genus IV. Bryograptus, Lapworth.

Hydrosoma bilaterally subsymmetrical, consisting of two com-
posite branches, diverging at a small angle from a distinct sicula.
From the two principal branches composite branchlets issue at small
but irregular intervals.

1. Bryograptus Kjerulfi, Lapw., Brogger.

Graptolithus tenuis, Kjerultf.

Dictyograptus-shales, Norway.

2. Bryograptus Callavei, Lapw. Upper Cambrian, Shropshire.

3. Bryograptus ramosus, Brogger.

Lower part of the Ceratopyge-shales, Norway. A very similar
species in abundance in shales below the Phyllograptus-shales at
Christiania.

Genus VY. Prerograprus, Holm (Ofv. Kongl. Vet. Akad. Forh.
1881, p. 74).

The hydrosoma issues from the wide end of the sicula. On the
two primary branches simple secondary branches arise from a number
of the hydrothece towards the apex, and these are bent alternately
to right and left of a plane passing through the primary branch, and
turn their cell-bearing side towards this plane.

Fig. 60. Fig. 6a. Fig. 5. Fig. 4.

Fic. 4. Pterograptus dilaceratus, sp. Nov. 7; et
Phyllograptus-shales, Galgenberg, Christiania.
», 5. Tetragraptus approximatus, Nich.
Phyllograptus-shales, Fure, Ringerike, Norway. A can
,, 6a. Dichograptus Sedgwickii, Salter (formation and locality as in Fig. 4.)

,, 6b. Part of a branch of Fig. 6a, enlarged twice nat. size to show the form of the
hydrotheca.

DECADE III—VOL. IlI.—NO. I. 2

18 Dr. O. Herrmann—On the Dichograptide—

1. Pterograptus elegans, Holm, Tullberg.
Graptolithus Murchisonii, Boeck ; G. gracilis, Kjerulf.
Primary branches diverging in curves at an angle of 50°-60°.
Didymograptus Murchisoni-zone (Kt. 4), Norway; zone with D.
Murchisoni' geminus, Skane.
2. Pterogaptus acutus (Hopk.), Holm.
Ptilograptus acutus, Hopk.
Primary branches diverging at an angle of 380°-40°.
Lower Llandeilo, Wales.
3. Pterograptus (?) dilaceratus, spn. (Woodcut, p. 17, Fig. 4.)
Hydrothece as in P. elegans, Holm. Secondary branches narrow
and thin, never so rigid as in that species. Angle of divergence of
the two primary branches probably about 180°. The hydrosoma
is always fragmentary (sicula not seen attached). Not unfrequently
a primary branch is met with, from the hydrothece of which closely
approximated branchlets project. It is sometimes rolled up circularly,
often only gently curved, or bent and broken into a zigzagged form.

Genus VI. Pievrocraptus, Nicholson.

Secondary branches proceed from both sides of the primary branches,
and themselves again give off branches ; primary branches diverging
at an angle of about 180°.

Referred by Lapworth to the Nemagraptide.?

1. Pleurograptus vagans, Nich.

Skiddaw Slates, N. England ; Phyllograptus-shales, Norway.

2. Pleurograptus lineuris (Carr.), Nich., Lapw.

Cladograpsus linearis, Carruthers.

Upper Llandeilo, England ; Hartfell Shales, Scotland.

3. Pleurograptus radiatus, Lapw. Hartfell Shales, Scotland.

The four-branched forms resulting from the dichotomous division
of a Didymograptus constitute

Genus VII. Trerracrartus, Salter.

Hydrosoma bilaterally symmetrically developed, consisting of four
simple equivalent branches. A central disc may or may not be
present.

The four-branched forms may be brought into two natural groups :

a. The two short branches issuing from the broad end of the
sicula diverge at an angle of about 180°, eg. Z. quadribrachiatus
(Hall). Thus is formed a funiculus uniting the two halves of the
hydrosoma, but this may be reduced until it nearly disappears (e.g.
T. Hicksii, Hopk., and T. Halli, Hopk.).

f. The two branches which originate from the sicula diverge at
an angle of 7180° (T. fructicosus (Hall)).

Group a.

1. Tetragraptus quadribrachiatus (Hall), Nich., Hther., Hopk.

and Lapw., Linnars., Torng., Broge., Herrm., Tullb.
Graptolithus quadribrachiatus, Hall, M‘Coy.
Tetragraptus crucialis, Salt.

1 Phyllograptus-shales, Norway.

2 See Notes on British Graptolithes, by C. Lapworth, F.G.S., Gzox. Maa. 1878,
Vol. X. p. 558, and Table I.

a Family of Graptolites. 19

Quebec Group, Canada; Skiddaw Slates, N. England ; Arenig,
Australia; Middle Arenig, Wales; Phyllograptus-shales, Norway,
Dalecarlia; Tetragraptus-zone, Skane.

2. Tetragraptus Halli, Hopk. and Lapw.

Middle Arenig, Wales.

3. Tetragraptus Hicksii, Hopk. and Lapw.

Middle Arenig, Wales.

4. Tetragraptus serra (Brongn.), (Gein.), Hopk. and Lapw., Tornq.

Fucoides serra, Brongn.

Cladograptus serra, Gein,

Graptolithus bryonoides, Hall.
Tetragraptus bryonoides, Salt., Nich.
Didymograptus bryonides, Carr., M‘Coy.

Arenig and equivalents in Wales, N. England, Canada, Norway,
Skane, Westgothland, and Dalecarlia; Newfoundland.

5. Tetragraptus denticulatus (Hall), Lapw.

Quebec Group, Canada; Silurian, Victoria ?

6. Tetragraptus crucifer (Hall), Nich., and Lapw.

With a central disc.

Quebec Group, Canada; Skiddaw Slates, N. England.

7. Tetragraptus alatus (Hall), Lapw.

With a central disc.

Quebec Group, Canada.

8. Tetragraptus Headi (Hall), Nich., Lapw:

With a central disc.

Quebec Group, Canada; Newfoundland; Lower part of Skiddaw
Slates, N. England.

9. Tetragraptus caduceus (Salt.).

Didymograptus caduceus, Salt., Nich., M‘Coy.
Phyllograptus similis, Hall.

Graptolithus Bigsbyi, Hall.

Tetragraptus Bigsbyi, Linnars., Lapw.

Skiddaw Slates, N. England ; Quebec Group, Canada; Phyllograptus-
shales, Norway, Skane; Australia (Hther., Ann. Mag. N. H. ser. 4,
vol. xiv. pl. ili. figs. 3, 4).

10. Tetragraptus approximatus, Nich., Lapw. (Woodcut, p. 17,
Fig. 5.)

Quebec Group, Canada; Phyllograptus-shales, Norway. Norwegian
Specimens differ in not having the branches so close together as in
Nicholson’s figure; the curvature on both sides of the branches is
sharper, and the branches do not so soon become parallel, and do not
continue so exactly parallel as Nicholson indicates. One specimen
from near Fure, in Ringerike, showed traces of a central disc.

Group P.

11. Tetragraptus fructicosus (Hall), Lapw., Broge., Herrm., Tullb.
Graptolithus fructicosus, Hall.
Didymograptus fructicosus, Ether., M‘Coy.
Quebec Group, Canada; Llandeilo Flags, Australia; Phyllograptus-
shales, Norway; Zetragraptus-zone, Skane; Arenig, Australia
(according to Lapworth).

20 Dr. O. Herrmann—On the Dichograptide—

From Zetragraptus two different groups of forms may be derived.
The four branches may divide dichotomously, producing hydrosomata
with eight or more branches (Dichograptus, Salt.) ; or secondary
branches may shoot forth from the four primary branches upon one
or both sides. The latter is the case in the following five genera.

Genus VIII. Scurzocraprus, Nicholson.

Hydrosoma bilaterally subsymmetrical, composed of four primary
branches, which issue in the form of a cross from the starting-point.
Each of these branches developes a series of rigid branchlets which
originate on each primary branch from the same side, and apparently
do not again divide. Hydrothece as in Monograptus sagittarius, His.
No central disc.

1. Schizograptus reticulatus, Nich., Lapw.

Dichograptus reticulatus, Nich.
Lower part of Skiddaw Slates, N. England.

Genus IX. Trocnocraprus, Holm (Ofv. Kongl. Vet. Akad. Férh.
1881).
Constructed exactly like the preceding genus, except that the
secondary branches give off branchlets always upon the same side.
1. Trochograptus diffusus, Holm, Brogger.
Phyllograptus-shales (Kt. 3, b), Norway.

Genus X. Crmnocrartus, Nicholson.

This genus, provisionally established by Nicholson, probably
belongs to this group. The fragment figured by Nicholson resembles
a portion of Trochograptus diffusus, figured by Holm, except that the
hydrothecz appear to be essentially different.

1. Ctenograptus annulatus, Nich.

Dichograpsus 2? annulatus, Nich.

Lower part of Skiddaw Slates, N. England.
Genus XI. Provisional.

1. Graptolithus Richardsoni, Hall, from the Quebec Group. The
mode of division of the branches as shown by the fragment figured
resembles that of Ctenograptus. But the commencement of the
hydrosoma is unknown, and we have no knowledge of the number
of primary branches.

Genus XII. Honocrartus, Holm (loc. cit.).

Hydrosoma bilaterally subsymmetrical. From the four primary
branches branchlets are given off on both sides at irregular intervals.
Hydrothecee as in Didymograptus.

1. Holograptus expansus, Holm.

Phyllograptus-shales, West Gothland.

Genus XIII. Gontocraptus, M‘Coy (Prodr. Pal. Vict. dec. v.)

1. Goniograptus Thureawi, M‘Coy, Lapw.

Arenig, Australia.

These smaller genera scarcely contain more than a single species
each, and probably in their case the establishment of genera has been

a Family of Graptolites. Zi

carried too far. This opinion also seems to be held by Tullberg
(Skane’s Graptoliter ii.). It would be better to regard them as sub-
genera of the two great genera Didymograptus and Tetragraptus.

All the many-branched Dichograptide may be conceived as origi-
nating from a Zetragraptus by repeated furcation. A division,
repeated in all branches, produces eight-branched forms; further
complete fureations give 16-branched forms and so on. Hitherto
the 8-branched forms constituted the genus Dichograptus, Salt., and
those with 16-32 branches the genus Loganograptus, Hall. But in
considering the various forms with 8 and more branches, we are at
once struck with an important contrast to those with 2 and 4 branches.
The latter, when perfectly preserved, invariably possess only 2 and
4 branches; but in the many-branched forms a remarkable variation
occurs in the number of branches; more and more frequently the
full number is either not developed or exceeded, imperfectly or
abnormally developed individuals become more and more numerous,
so that the number of branches becomes of less and less value as a
distinctive character. Thus in the multiramose species of the genus
Clonograptus, Hall, the number of branches oscillates between 40
and 60 for the same species. The number of branches becomes finally
so complicated as to be quite unimportant (e.g. Clematograptus mul-
tifasciaius, Hall). Thus the genus Loganograptus, Hall, with 16-32
branches appears to be quite arbitrary and artificial, and must be
suppressed, unless we are prepared to establish a genus for every
many-branched species. It has been proposed to refer all species
with more than four branches to Dichograptus, Salt., which has
hitherto included only 8-branched forms. But upon this the author
would put a limitation, as there is in the many-branched forms a
striking difference. ‘Thus either all the points of furcation are
situated in the immediate vicinity of the sicula (e.g. Dichograptus
Kjerulfi, Herrm., Fig. 8), while the more distant parts of the branches
remain undivided; or there are greater distances between the indi-
vidual points of furcation, so that the branches may divide through-
out their whole length, and the points of furcation may depart far
from the centre of the hydrosoma (eg. Fig. 9).” For the latter
forms Hall has proposed the name of Clonograptus, which may
stand, and thus we get two homologous series forming the genera
Dichograptus, Salt., and Clonograptus, Hall, each including forms
with 8, 12, 16, and more branches.

Genus XIV. Dicuocrartus, Salt. (modified).

Hydrosoma bilaterally symmetrical. From the broad end of the
sicula, which is directed upwards, issue two short oppositely diverging
branches, which fork. Of the four branches thus produced, all or a
part may again divide dichotomously once or several times at very
short distances, so that more than four equivalent, simple branches
are produced. The proximal parts of the hydrosoma are frequently
enclosed in acentral disc. Hydrothece as in Didymograptus, M‘Coy.

22 Dr. O. Herrmann—On the Dichograptide—

1. Dichograptus octobrachiatus (Hall), Nich., (M‘Coy), Lapw.,
Brogg. (Fig. 7.)

Sy y

g i YH

S
S
S

SALAEE
|

\\

Fie. 7. Dichograptus octobrachiatus, Hall, from the Phyllograptus-shales,
Galgenberg, Christiania (natural size).

Graptolithus octobrachiatus, Hall.
Graptolites (Didymograptus) octobrachiatus, M‘Coy.
Loganograpius Kjerulfi, Herrm. ex parte.

The central disc may or may not be present. In the typical con-
dition the species has eight branches, but specimens are frequent
with more or fewer branches.

Quebec Group, Canada ; lower part of Skiddaw Slates, N. England ;
Phyllograptus-shales, Norway ; Arenig, Australia. —

2. Dichograptus octonarius (Hall), Lapw.

Graptolithus octonarius, Hall.

Central dise unknown. Quebec Group, Canada.

3. Dichograptus Sedgqwickit, Salt. (Figs. 6a, 60.)

Figured but not described by Salter (Q.J.G.S. vol. xix. p. 138).

The author describes the species :—

In the typical condition the hydrosoma consists of eight simple,
curved branches, which are arranged as in D. octobrachiatus, Hall.
There is in this species the same variation in the number of branches
as in D. octobrachiatus, which is its nearest ally, the differences be-
tween them consisting in the curvature of the branches, and the
habit of the hydrothece. Of the latter there are eight in a length
of ten millim. Their lower border is curved and forms with the
axis an angle of 10°—12° at the proximal end, of about 30° at the
distal end. The apertural angle is about 90°, and the hydrothece,
which are about one-half longer than broad, are half free, appearing
as pointed, nearly perpendicular teeth (Fig. 6b). No central disc has
been observed either in English or Norwegian specimens.

Skiddaw Slate (lower part), N. England; lower part of Phyllo-
graptus-shales, Norway.

4, Dichograptus Kjerulfi (Herrm.) (Woodcut, p. 23, Fig. 8).

Loganograptus Kjerulfi, Herrm. ex parte.

In 1882 (Nyt Mag. for Naturv. xxvii. pp. 341-362) the author
described and figured, under the name of Loganograptus Kjerulfi, a
number of forms which subsequent study showed him must be

a Family of Graptoltes. 23

separated. The eight-branched forms, with some abnormally deve-
loped examples, are referred to D. octobrachiatus, Hall. The forms
furnished in the typical state with twelve branches are to be regarded
as a distinct species, and that these examples cannot be referred
either to D. octobrachiatus (Fig. 7) or to D. Logani, Hall, seems to the
author to follow from the facts that in some localities only eight- and
many-branched forms (D. Logani, Hall) have been found (e.g.
Australia and Canada), in others only those with numerous branches
(e.g. the Australian localities examined by R. Etheridge, jun.), and
in other localities again only eight-branched forms. In the locality
investigated by the author (Galgenberg, Christiania) the forms with
8 and 12 branches occur together, and he considers that here two
different species are associated. Further, the twelve-branched forms
constitute a bilaterally symmetrical species, and the number of
normally developed examples as compared with abnormal ones seems
to indicate their distinctness.

Ss
NZ

))}

Din

Fic. 8. Dichograptus Kjerulfi, Herrmann, Phyllograptus-shales, Galgenberg,
Christiania (natural size).

Description.—Hydrosoma bilaterally symmetrical, consisting of 12
branches when typically developed. From a sicula, which usually
persists as a rounded knob, issue 2 short branches, which bifurcate
first into 4 and then into 8 branches. Of these 8 branches, 4 again
divide, and these four are almost always those situated furthest from
the plane of symmetry, #.e. the inner branches of each half of the
hydrosoma of an octobrachiate form (Fie. 7i). The branches are
slender, thinnest in the neighbourhood of the sicula. The full
number of branches is frequently not attained, and rarely exceeded.
The central part of the hydrosoma is almost always enclosed in a
chitinous dise. The hydrothece are rarely to be seen within the
disc. There are 9 of them in a length of 10 millim. At the proxi-
mal end they form with the axis an angle of 13°—15°, at the distal
end one of about 35°. They are three times as long as broad, and
about one-third free. The lower border is curved. Aperture-angle
55°.

24 Dr. O. Herrmann—On the Dichograptide—

It has been thought that the forms described by the author (loc.
cit.), constituting a continuous series of examples with from 5 to 14
branches, were to be regarded as individuals of different ages, the
highest number of branches indicating the greatest age. The author
regards this view as untenable. No difference is to be detected in
the thickness and length of all the branches, such as would occur if
any of them were formed subsequently to the rest, whereas it might
be expected that the supposed younger branches would be observable
when they had just sprouted, and before they reached the margin of
the disc. It is also difficult to imagine how any such subsequent
increase could be brought about, as the branches originate by bifurca-
tion, which usually occurs only at the top of a branch. But the
notion is disposed of by the fact that young individuals occur with
8, 9, and 12 branches, just as in full-grown examples.

Dichograptus Kjerulfi is found in the lower part of the Phyllograptus-
shale (Kjerulf’s Lower Graptolite-shales, Brogger’s Etage 5b), and
occurs in great abundance in a thin bed in the Galgenberg, near
Christiania, associated with D. octobrachiatus (Hall), Didymograptus
constrictus (Hall), ete.

5. Dichograptus Logant (Hall) , Nich.

Graptolithus (Loganograptus) Logani, Hall.
Graptolites (Didymograptus) Logani, M‘Coy.
Loganograptus Logani, Lapw.

Quebec Group, Canada; Skiddaw Slates (lower part), N. England ;
Australia. D. Logani, Etheridge, Ann. Mag. N. H. ser. 4, vol. xiv.
pl. 1. fig. 12, is doubtful.

5b. Dichograptus Logani (Hall.), var. australis (M‘Coy).

Grapt. (Didymogr.) Logani, var. australis, M‘Coy.

Arenig, Australia.

From Dichograptus new forms may proceed by the development
of branchlets upon the primary branches. ‘These form—

Genus XV. Cxiematocraptus, Hopkinson.
Hydrosoma much ramified, bilaterally subsymmetrical. From a
short funiculus issue a great number of primary branches, from
which numerous branchlets spring on one or both sides, at irregular
distances, often closely packed together. Hydrothece as in Dicho-
graptus. No central disc.
1. Clematograptus implicatus, Hopk., Lapw.
Loganograptus? implicatus, Hopk.

Middle Arenig, Wales.

2. Clematograptus multifasciatus (Hall), Hopk. and Lapw.
Graptolithus multifasciatus, Hall.

Hudson River Group, New York.

D. (L.) Logani, Etheridge (Ann. Mag. N. H. ser. 4, vol. xiv. pl. ili.
fig. 11), from Australia, probably belongs to this genus.

Genus XVI. Citonocraptus, Hall.

Hydrosoma bilaterally subsymmetrical, consisting of more than
four simple branches produced by dichotomous division. ‘he spaces

a Family of Graptolites. 25

between the furcation-points are larger than in Dichograptus. Cen-
tral disc never present.

There is some uncertainty about the species of this genus. Hall
discovered in a loose block in Americaa form with 16 branches, which
certainly belongs to this genus (CZ. Milesi, Hall) ; this is figured, but
not described, by Hall. Nicholson found in the Skiddaw Slates two
specimens of a form which must also be referred to this position.
They possess a great number of branches (C. multiplex, Nich.). In
the Norwegian Phyllograptus-shale the author has found a consider-
able number of specimens agreeing in character with the above, and
especially with Nicholson’s species, six of which have 8, and four
16 branches, while many others vary between 8 and 16 branches

Fig. 9.

Fig. 9. Clonograptus muiltipler, Nicholson, Skiddaw slates, Peel-Wyke, Bassen-
thwaite, Cumberland.
(Fig. 9). These were formerly identified by the author with C.
Milesi (Hall), but he now regards this identification as doubtful.
Nicholson’s genus Zemnograptus is not sufficiently distinct from
Clonograptus.
1. Clonograptus Milesi, Hall.
Graptolithus Miles, Hall.
Temnograptus Milesi, Nich.
2. Clonograptus multiplex (Nich.). (Fig. 9.)
Dichograptus multiplex, Nich.
Temnograptus multiplex, Nich., Lapw.
Skiddaw Slates, N. England.
3. Clonoyraptus flexilis (Hall), Nich., Lapw.
Graptolithus flewilis, Hall.
Quebec Group, Canada.
4, Clonograptus rigidus (Hall), Nich., Lapw.
Graptolithus rigidus, Hall.
Graptolithus abnormis, Hall.
Quebec Group, Canada; Phyllograptus-shale, Norway.
0. Clonograptus ramulus (Hall), Lapw.
Graptolithus ramulus, Hall, Tornq.
Quebee Group, Canada; Phyllograptus-shale, Dalecarlia.
Graptolithus Richardsoni, Hall, does not belong to this genus.
6. Clonograptus tenellus (Linnars.)
Dichograptus ? tenellus, Linnars., Lapw.
Trichograptus tenellus, Nich.

Olenus-shale, West Gothland.

26 MM. De Rance and Topley—Rate of Erosion of Sea- Coasts.

The most ancient of known Graptolites, described by Linnarsson
in 1871, as Dichograptus ? tenellus. Tullberg regards it as a
Bryograptus ; Nicholson refers it to his genus Trichograptus. The
discoverer of the species noticed that its ramification agreed with
that of Clonograptus flexilis; and until more perfect specimens are
obtained, it may take its place here.

VI.—AN tnquiRyY INTO THE Rate oF HRoston oF THE SEA-COASTS
or ENGLAND AND WALES, AND THE INFLUENCE OF THE ARTIFICIAL
ABSTRACTION OF SHINGLE OR OTHER MartreriaL IN THAT ACTION.

By C. E. Dz Rance, F.G.S., and W. Torrey, F.G.S., Secretaries."

The Committee has during the past year received several Returns
relating to the south and east coasts of England. Most of those
relating to the coast south of the Thames are printed.

The thanks of the Committee are especially due to Major-General
Sir A. Clarke, who has instructed the Officers of the Royal Engineers
stationed around the coast to supply the Committee with such infor-
mation as they may possess or-be able to obtain. Further returns
are expected from the same department and from other official
sources; the Committee therefore think it best to defer any general
report until more complete information is obtained. _

The Memorandum drawn up by Mr. J. B. Redman so fully sets
forth the work of the Committee, and the importance of the inquiry
referred to it, that this is now printed.

The Memorandum by Mr. G. Dowker on Hast Kent gives a
sufficiently complete account of the changes of the coast in this
district ; changes which are of especial historical importance and
interest.

Mr. Whitaker has drawn up a list of works relating to the coast-
changes of England and Wales, which will be of great service to
the Committee and to those who may assist in the work.

The Committee would again ask for the assistance of any who by
long residence or other means have special knowledge of changes on
any part of the English and Welsh coast. Printed forms of ques-
tions can be obtained from any member of the Committee.

Extracts from the Mumoranpum By Mr. J. B. Repmay, M.Inst.C.E.

That the erosion of our south-eastern coasts by the action of wind
and waves has been assisted and increased by artificial agency, by
removal of material and by the treatment of works of defence in a
selfish spirit, unaccompanied by concerted action, resulting in injury
to adjoining frontages for the benefit of those operated on, can be
copiously illustrated by the records of our public departments, such
as the Admiralty, Woods and Forests or Works, the Board of Trade,
the War Office, and the Trinity Corporation, as well as by those of
nearly every harbour board, river conservancy, or local drainage and
sewage authority. And this fact is portrayed in a special literature

1 Being the substance of a Report laid before the British Association at Aberdeen,
and read in Section C. Geology, 1885.

MM. De Rance and Topley—Rate of Erosion of Sea-Coasts. 27

of its own, the Blue Books of the House of Commons, for the
various tidal harbours’ reports, inaugurated by the persistent agitation
of the late Joseph Hume, M.P., as well as those on harbours of
refuge, lighthouses, and shipping, give incidentally numerous isolated
cases showing how much this really imperial question has been over-
looked or confused by a division of authority, and the struggles with
lords of the manor, illustrated by a number of well-known cases,
adds additional exemplification.

The legal aspect of this question has been recently ably treated on
by a republication of “ Hall’s Essay on the Rights of the Crown in
the Sea-shore,” by Richard Loveland Loveland, of the Inner Temple,
in 1875, and this work shows well the imperial character of the
inquiry deputed to the British Association Committee on the Erosion
of the Sea Coasts of England and Wales.

As regards the wholesale removal of shingle and boulders from
marine spits and moles, it is only necessary to refer to such cases as
the quarrying of cement stones from the foreshores on either side of
Harwich, from the Beacon cliff to the southward, and from the
Felixstow cliffs to the northward, only stopped by the persistent
efforts made by Captain Hewett’s successor in the North Sea Survey,
the late Admiral Washington, and others. For illustration of this
pernicious practice and the deplorable results frequently entailed this
case suffices. Again, on the northern side, the indiscriminate
removal of shingle from the northern breakwater of Harwich har-
bour (Landguard Point) for ballastage by the lord of the manor has
been the fruitful source of litigation. Similar results from similar
practices at Spurn Point, at the mouth of the Humber, have been
entailed. In effect, this natural shingle mole, defending the entrance
to the most important harbour on our eastern coast, was nearly
breached in consequence.

Next to the removal for ballastage, the most fertile cause is
removal of material for road-making and for building purposes, and
when in the neighbourhood of a large town this becomes, from the
enormous quantity removed in the aggregate, sufficient to tell eventu-
ally on the oscillating natural foreshore protection. Take the case
of Hastings: for the last half-century there has beena constant draw
on the material for such purposes. The quantity used must be
enormous, and in effect the new portion of the town may almost,
without figure of speech, be described as in a large measure built out
of the sea. About 1836 Hastings was separated from St. Leonards
by a small marshy bottom, with a rill of water running through it,
called the “ Priory Marsh,” and during that year the sea was excluded
by the erection of a vertical stone wall joining the esplanade terraces,
and the two towns became what it is now, one big town. Since that
wall was erected the shingle in front of it has, from various causes,
become much attenuated, the groynes destroyed, and the sea has, it
is said, in places got under the sea walls. So great has been the loss
in the bay to the eastward, where is situate the old portion of the
town, the fishermen’s quarter, that a general exodus of that industry
to Rye, or elsewhere, has been threatened.

28 MM. De Rance and Topley—Rate of Erosion of Sea-Coasts.

A second groyne is being constructed from the base of the cliff
below the castle (where a similar work formerly existed) at a very
great cost, in order to promote accumulation of shingle along the
Hastings frontage, and to bring about again the old state of things.

The argument made use of by many owners of property here, as
elsewhere, to the effect that removal of shingle for building purposes
must be inappreciable (as however great the abstraction for such
purposes, millions of tons renew the shore after a change of wind)
is made in evident forgetfulness or ignorance of the fact that these
abstractions from and renewals to the natural “fulls” of beach,
alternately reduce and increase what is a circulating medium of
defence, moving in opposite directions up and down channel, with a
preponderating movement up-channel due to prevalence of south-
west winds, and that such a constant drain on a natural defence,
however recuperative, must tell in the long run.

The removal of boulders from the foreshore seaward of the summit
shingle neap and spring ‘“fulls,” either for road-making or for
manufacturing purposes, not only loosens the foreshore, and renders
it, thus disintegrated, less able to resist the stroke of the wave, but
in many cases, such as the ‘“‘Chenies” rock off Sheerness, and the
“Septaria ” blocks off Harwich, the material formed natural groynes
and breakwaters, and their removal, in reference to shore conservaucy,
was most suicidal. )

Another fertile source of accelerated erosion of a special locality
is the erection of a close pier for a harbour entrance, and of large
and lofty groynes for accumulating shingle, looking only to the pro-
tection of an isolated frontage, and without reference to the attendant
abstraction of material to the leeward of such works, from the
absolute stoppage of the material on its way to the less favoured
locality. The case is parallel to the last, as the oscillating medium is
laid under heavier contribution for a favoured locality, and is
gradually starved for the neglected neighbour to leeward.

Folkestone may be cited as a principal delinquent of this class, due
to the elongation of the close pier to the windward or westward of
its harbour, which half a century back was a trap for shingle, and a
fisherman’s first task in the early morning, prior to that, was to
excavate a channel through the newly-arrived shingle to get his boat
through and out to sea. The resultant accumulation of shingle to
windward forms the tongue of land on which stands the “ Pavilion,”
etc.

Now, in “ Hast Wear ” Bay there is an almost entire absence of
shingle, and the resultant falls of the chalk undercliff take place at
so alarming a rate that the very existence of the South-Eastern Rail-
way is jeopardized. That this action is not due to the Admiralty Pier
at Dover is shown by the entire absence of shingle to windward of
that work, but in its place a remarkable extension of the silty fore-
shore has taken place, gradually diminishing towards Folkestone.
Eastward of Dover we have similar results from the same cause ;
from the Castle Jetty to St. Margaret’s the base of the lofty chalk
cliff is now washed and abraded by the waves, and the lower débris

Notices of Memoirs—W. Watson—Black Rock of Kiltearn. 29
and shingle, forming an undercliff carriage-way into Dover some
thirty years back, has now entirely disappeared.

We may be asked to suggest a remedy, but this, perhaps, is beyond
the province of this Memorandum; but as regards the old stereo-
typed plan of building a solid pier out from the shore, for communi-
cation therewith from vessels, or for protection of the outfall of a
tidal river, it has been suggested that there are numerous cases,
where a moving beach has to be crossed, that it would be better to
commence the solid work altogether seaward of the shingle “fulls,”
and connect it with open piling to the shore, and so as to leave the
littoral movement of beach uninterfered with.

As respects groynes, there is hardly a watering-place on our
southern coast where they have not become a burning vexata questio
of the day, and at most of them illustrate the suggestion made more
than thirty years back, that groynes cut up a shore into a multitude
of bays, with a repletion of material on one side and deep water on
the other, and would have had a better substitute in a sea-wall that
allowed the shingle to pass freely backwards and forwards along its
face. Such was the experience with the frontage of Romney Marsh,
defended by Dymchurch sea-wall, 34 miles in length, where the old
system of groynes, which cut up the frontage into an interminable
number of bays, was abandoned about forty years back in favour of
the present stone slope.

The system of groynes at Brighton, for some isolated points,
appeared to have answered well when the supply arriving at that
town of shingle from the westward was uninterfered with, but a
change occurs when the system was continued to Hove, or West
Brighton, in thickening quantities. The material arriving was a
constantly diminishing one, from the fact that the Shoreham Gas
Works, erected under an Act of Parliament on the “live” beach
between the harbour and the sea, were found to stand upon a some-
what unstable base, with a fickle sea defence, unless supplemented by
artificial works. Groynes on an extended scale were erected, which
treated West Brighton in the same ungenerous spirit entertained in
former days for Rottingdean, for the sake of and advantage of Kemp
Town. The encroachment of the sea to the leeward side of the
groynes, on the esplanade lawns, has necessitated the erection of an
esplanade wall.

IN @ aise Sec Se Ore Vira sae So

Brief Notices of Papers Read before Section C. Geology, British Association
Meeting, Aberdeen, 1885.
I.—Tuu Cuasm cattep THE Brack Rock oF Kirmarn.
By Witi1am Watson.
HIS is a narrow ravine in conglomerate: its length is about 14
mile; its depth varies from 100 to 180 feet; its breadth at the
top varies from 12 to 15 to about 30 feet. The river which flows
through the ravine is the Altl-Granda; it drains Glen Glass (above
the ravine) ; the water flows into Cromarty Firth.

80 Notices of Memoirs—Dr. Hull—Geological Map of Egypt.

The author refers to popular views held to explain the formation
of the ravine—earthquakes and fracture—and shows that these are
inadequate. The ravine has clearly been produced by erosion, of
which the marks are still visible on the sides; the difficulty is to
explain how erosion could have produced a gorge of this kind with-
out weathering action and floods having denuded the sides.

Above the gorge in Glen Glass was once a lake. This had been
silted up to the height of about 80 feet with sand, washed out of the
Glacial débris of the glen. When the barrier that confined the lake
gave way, the river flowed over the surface of the conglomerate,
carrying with it much sand from the lake silt, and using this as
a means of rapidly eroding the rock. When the chasm was deep
enough to prevent the floods from overflowing the banks, the sides
could not be widened to any great extent. The disproportion
between the deepening and widening process has been maintained,
thus causing the steep-sided narrow glen. The excavation now
going on is small, whilst the weather has some effect on the sides ;
so that ultimately there will be produced an ordinary valley.

IJ.—Nortice oF AN Ourtins GeoLtogicaL Map or Lower Heypt,
ARABIA PETRHA, AND PALESTINE.

By Prof. Epwarp Hutt, LL.D., F.R.S., F.G.S.

HE map exhibited was enlarged from that which accompanies the
author’s book “‘Mount Seir, Sinai, and Western Palestine,”
giving a narrative of the expedition sent out into these countries by
the Palestine Exploration Society in 1883-84. It embraces a region
extending from the valley of the Nile on the west to the table-land
of Edom (Mount Seir) and Moab, including the Jordan, Arabah
Valley, and the mountains of Sinai. Its northern limit is the Lebanon.
The following formations and divisions are represented :—

‘ ( 1. Sandhills of Lower Egypt, the coast of Palestine,
and Arabah Valley.
RECENT. 1 2. Alluvial Deposits of the Nile, the Ghor, and Jordan
Valley.
Wise Gri st the Wady el Arabah.
(1. Raised Beaches bordering the Gulfs of Suez and
REcEackaaarn | Akabah, the Isthmus of Suez, and borders of
Post-PLIocENE TO Q Be Teen.
Pp 1 2. Ancient Deposits of the Salt Sea (Dead Sea).
or geod | 3. Old Lake-beds of the Sinaitic Peninsula and Arabah
L Valley.
Upper Eocene. Calcareous Sandstone of Philistia.
EocrneE TO Middle and Lower Eocene. Nummulite Limestone.
CRETACEOUS. Upper Cretaceous. Cretaceous Limestone.

Town CAMPON ER OUR. Limestone of Wady Nasb.
oy Desert Sandstone and Conglomerate.
Meramorpuic Rocks

(Archeean ?).

iL,

Me

3.

4. Cenomanian. Nubian Sandstone.
1.

{23.

} Gr

MopEEN Voreante \ Basalt, Dolerite, etc.

anite, Gneiss, and various kinds of Schist.

Rocks.

Granite, Porphyry, Felstone, Diorite, etc.

Beds of Tuft and Agelomerate of Wady Haroun and
Jebel esh Shomrah.

ANCIENT VOLCANIC OR
Priutonic Rocks.

Notices of Memoirs—John Gunn—Rocks of Caithness. 31

The main lines of fault and dip of the strata are also indicated.

As an outline of the scientific results which were arrived at by the
members of the expedition, and which are represented on the map,
had already been communicated to the Association,’ it was not con-
sidered necessary to repeat them here, but the author wished to add
that a topographical and geological map of the Arabah Valley on a
scale of about six miles to one inch was in preparation, and would
accompany the Geological Report now in the press for the Palestine
Exploration Society. The topographical survey had been made by
Major Kitchener, R.E., and Mr. John Armstrong (formerly sergeant-
major, R.E.), and the geological details had been inserted by the
author. In addition to these, several longitudinal geological sections
illustrating the structure of various parts of this region, and nume-
rous drawings would accompany the memoir.

I1J.—On THE Occurrence oF Lower Oitp Rep ConGLomMERATE IN
THE Promontory oF THE Fanap, Nortu Donegat.
By Professor Epwarp Hutt, LL.D., F.R.S., F.G.S.,
Director of the Geological Survey of Ireland.

HE district in which the Old Red Conglomerate occurs is formed
of ridges and valleys of metamorphic rocks, consisting of beds
of quartzite, schist, crystalline limestone, and trap, chiefly diorite.
It lies between Lough Swilly and Mulroy Bay, and is washed on
the north by the waters of the Atlantic. ‘The remarkable tract of
the Old Red Conglomerate, recently discovered by the officers of the
Geological Survey, is far remote from any mass of the same formation,

and it is unrepresented on any geological map hitherto published.

The beds consist of red and purple sandstones and conglomerates,
made up chiefly of quartzite pebbles and blocks, but also containing
others of limestone and trap; all derived from the surrounding
metamorphic series. They occupy an area of over two miles in
length and half a mile across, extending along the northern base of
Knock Alla, a ridge of quartzite which traverses the promontory
from side to side. The beds dip against the base of the mountain,
against which they are let down by a large fault, and they terminate
along their northern edge by an unconformable superposition on
beds of quartzite and limestone. They reach a total thickness of
about 800 feet.

From the position of these beds it becomes evident that they are
unconnected with any of the recognized basins of Lower Old Red
Sandstone, either in Scotland or Ireland, and may, therefore, be re-
garded as having been formed in an isolated basin, which, following
the example of Dr. Geikie, I may be allowed to name “‘ Lake Fanad.”
The tract will be a new feature on geological maps of Ireland.

TV.—On Rocks or Cenrrau CarrHness.
By Joun Gunn.
HE term “Central Caithness” is intended to embrace most of the
parish of Halkirk and part of the parish of Watten. The
1 Rep. Brit. Assoc. (Montreal Meeting, 1884), Transactions of Sections C and E.

32 Notices of Memoirs—W. Whitaker—Brighton Waterworks.

upper part of the parish .of Halkirk is covered by drift-gravel,
underlying peat. At Loch More flagstones are presented. Below
the lake may be traced the banks of what was once a great river.
At Dirlot the rocks are sandstone, granite, gneiss, gneissic con-
glomerate, and limestone. At Dalmore the right bank of the Thurso
is composed of Boulder-clay, the left of gravel. Here is seen a
chain of moraines, composed of granitic gravel and sand. At
Tormsdale a vein of some cinder-like material occurs. The flag-
stones at Poll a’ Chreagan are covered with freestone, as also at
Dale Bridge on the right bank of the river. On the left the flags
lie exposed in great tabular masses, overlying limestone. At the
top of the Mill Pool are the remains of a natural dam. Below this
pool a band of freestone once crossed the bed of the river. At Dale
are shifting beds of gravel, and here the river is continually changing
it course. Below Polihour flags again appear, and opposite Scots
Calder are banks of Boulder-clay, the boulders therein being very
distinctly striated. Great masses of flagstone block up the bed of
the stream at Gerston. At Halkirk the cliffs are coated with red ochre.

Granite is not visible at Dorrery, as has been stated by at least one
writer, but it does not appear to lie at any great depth below the flags.

At Achanarras a curious fossil fish, Coccosteus, is found in a small
slate quarry.

East from Spittal the angle at which the rocks dip gradually
diminishes, and at Lanergill reaches its nearest approach to a dead
level.

Drift gravel prevails in the neighbourhood of Halsary, and also
down part of Strathberg, where the banks of the ancient river may
again be traced. Here the Dalmore moraines are continued.

No evidence of volcanic action can be gathered from an examina-
tion of the rocks of Central Caithness, but the district presents a
fair field for the study of erosion by ice, air, and water.

V.—On THE WATERWORKS AT GoLpSTONE Roap, BRIGHTON.
By W. Wuiraxer, B.A., F.G.S., Assoc Inst.C.E.

OTES of a visit underground in December 1884, when the water

was pumped down for extending the galleries. These works

are perhaps the best example of the right way of getting a very

large supply of water from the Chalk, galleries being driven (in one

case to the length of 800 feet) at about low-water level, so as to
cut the fissures and intercept the water on its way to the sea.

The whole of the works (shafts and galleries) are in the White
Chalk, with but few flints in the bedding-planes, but with many
oblique layers along joint-planes. The supply comes chiefly from a
few powerful springs, and, though small contributions issue between
these, it is noteworthy how far a tunnel has sometimes been driven
before reaching a fissure of large yield. Under these circumstances
borings, or even shafts, might have failed to yield a large supply.

The roof of the north-eastern gallery is throughout of one bed,
rarely needing support, a thin brittle layer of flint at its base being
cleared away.

Reviews—Dr. Lindstrom’s Silurian Crustacea of Gotland. 33

VI.—Own some Rock SrrecIMENS FROM THE ISLANDS OF THE FERNANDO
Noronua GRovpr.

By Professor A. Renarv, LL.D.

HE rock specimens described in this communication were col-
lected by J. G. Buchanan, Esq., during the voyage of the
“Challenger.” The islands have been described by Darwin in his
“Geological Observations on Volcanic Islands” (2nd edition, p. 27).
The author, after having explained the geological structure, gives
lithological descriptions of the chief types of the rocks, which may
be referred to the phonolites (St. Michael’s Mount). These phono-
lites are composed of sanidine, augite, nepheline, hornblende, magne-
tite, nosean, and titanite.

The rocks of Rat Island are basalts with nepheline. The con-
stituent minerals are augite and olivine. The ground-mass is almost
entirely composed of nepheline; biotite and apatite occur as acces-
sory constituents. The little island known as Platform Island is
also basaltic, with a doleritic texture. It is composed of labradorite,
augite, olivine, magnetite, and biotite. The rock has undergone
alterations.

VII.—Traces or Harty Human Haprrations on Dexsipe & VIctniry.
By the Rev. J. G. Micuiz, A.M.

IRCULAR CAIRNS:—Their structure. Their probable uses—
human dwellings; sepulchral purposes. Urns, chests (cists)
found in connection (Migvie).

YeErD Hovsres:—General structure—examples in Cromer, Glen-
kindy, and Kildrummy. Probable uses. Generally found in the
vicinity of round cairns and circular foundations.

Laxe Dwetiines (Crannogs):—Island in Lock Kinnord, Loch
of Leys. Similar to those found in Wigtonshire and Ayrshire. Dr.
Stuart’s “Scottish Crannogs,” and Dr. Munroe’s “ Ancient Scottish
Lake Dwellings.” Relics found in connection—canoes, arrow-heads,
celts, stone knives, and stone cups.

Moatep Forts :—Lumphanan, Invernochty, Rothiemurchus, and
ruder form at Loch Davan.

Ancient Piortse Towns :—Character and situation. Davan—
Short description of ; probably the Devana of the Romans.

Sy 2st Ws 2 aS WWE IS
; SoS
I.—Forteckninc pA Gotitanps Situriska Crustacirr. Af G.
Linpstrom. Tafl. xii—xvi. (Ofversigt af Kong]. Vetenskaps-
Akademiens Forhandlingar, 1885, No. 6. Stockholm.)
A CaTaLoguE oF THE Siturran Crustacea oF Gotnanp. By G.
Linpstrém. 8vo. pp. 68, 5 Plates.
{Ey the thirty years which have elapsed since the issue of Angelin’s
great work ‘“ Paleontologica Scandinavica,” there.has been a
great accumulation of fresh fossil material from Swedish strata,
partly through the labours of Angelin himself, and partly through
DECADE II.—VOL. III.—NO. I. 3

o4 Reviews—Richthofen’s Atlas of China.

the work of succeeding paleontologists; and Prof. Lindstrém has
undertaken the desirable task of investigating its character. This
memoir contains the results of his studies of the Silurian Crustacea
of Gotland, from which locality 70 species of Trilobites, and two of
Merostomata, are enumerated and described. New species belonging
to the following genera are introduced, viz. Phacops (1); Cheirurus
(1); Spherexochus (2); Lichas (6); Harpes (1); Calymene (5) ;
Phaétonides (2); Cyphasphis (1); Proetus (6); Illenus (2); and
Bronteus (3). A new genus, Youngia, based on the characters of
Cheirurus trispinosus, Young, is formed, and includes two new species.
Most of the forms are fragmentary, but the portions preserved retain
their surface characters so perfectly, and these have been so clearly
and exactly described and figured in the plates and woodcuts, that
there should be no difficulty in identifying them. Prof. Lindstrém
gives a table showing the distribution of the species in the four
divisions of the Gotland strata, which correspond respectively to our
Upper Llandovery, Wenlock Shale, Wenlock Limestone, and Ludlow
beds; and from this it appears that in Gotland the Wenlock Lime-
stone is the richest in species; that there are three species peculiar
to the Upper Llandovery, ten to the Wenlock Shale, eleven to the
Wenlock Limestone, and four to the Ludlow beds. Some species,
as Spherexochus scabridus, Encrinurus punctatus, and Illenus barriensis,
appear in all the divisions, whilst all the species of Zichas are
limited to the two upper divisions. Prof. Lindstrom further states
the noteworthy fact that not one of these species is found in the
strata below the marly shales, which are the equivalents of the
Upper Llandovery, in Sweden. Calymene Blumenbachii has been
reported to occur in underlying beds, but according to Lindstrém,
the head-shields attributed to this species, found in West Gotland
and in Dalecarlia, are too badly preserved to admit of satisfactory
recognition. G. J. H.

IJ.—Arzias von Cuina. Orographische und Geologische Karten ;
vou FERDINAND FREIHERR voN RICHTHOFEN, zu des Verfassers
Werk: China, ergebnisse eigener Reisen und darauf gegrtindeter
Studien. Erste Abtheilung: Das Nordliche China. Berlin,
Dietrich Reimer, 1885.

Attias or Curva. Orographic and Geological Maps, by Frrpinanp
Fretgerr von Ricutruoren, for the Author’s work on China.
First part, Northern China.

HE construction of a series of geological maps of such a vast and
comparatively unknown country as China, must be a difficult

and arduous task, even in the hands of such a competent geologist
as Prof. von Richthofen. And yet in this Atlas we have, in addition
to the orographical maps, thirteen large maps, each representing an
area of 78,000 square kilométres, on which the boundaries of the
principal geological divisions of Northern China are delineated with
great apparent precision! The basis of the work rests on the
author’s observations during his travels in the country, but these of
course were limited to the comparatively narrow strip of territory

Reviews—Roemer’s Erratic Blocks of N. Germany. 30

bounding his route; he has further combined the information ob-
tained from other travellers and from the natives; but even so the
mapping of the geological features of no small proportion of the
country must have depended upon bold generalizations. Whatever
may be the result of subsequent actual investigation by future
Chinese or European geologists, this preliminary attempt to lay
down the geological boundaries of this vast area cannot fail to be of
great advantage and assistance to later workers, and deserves the
warmest recognition. The maps are on the scale of 1: 750,000; the
colouring employed for the different geological divisions is partly
similar to that adopted by the Geological Congress. This first part
of the Atlas is intended to accompany the second volume of the
author’s great work on China, which has been already noticed in
the GronocicaL Magazine.’ G. J. H.

T1.—Letama Ereratica, oper AUFZAHLUNG UND BESCHREIBUNG DER
IN DER NorDDEUTSCHEN EBENE VORKOMMENDEN Dinuviat GE-
SCHIEBE NORDISCHER SEDIMENTAR-GESTEINE. Von FERDINAND
Reamer. Mit 11 Tafeln und 5 Holzschnitten. Paleontologische
Abhandlungen herausgegeben von W. Dames und EH. Kayser.
Zweiter Band. Heft 5. (Berlin: G. Reimer, 1885.)

LutH#A ERRATICA, OR AN HNUMERATION AND DescRIPTION OF THE
DituviaL Erratics or NortHern SepimenTary Rocks occur-
RING IN THE Puains or Norta Germany. By Ferpinanp Ramer.
Ato. pp. 178. With 11 lithographed plates and 3 woodcuts.

N the Boulder-clay which is so extensively distributed over the
plains of North Germany and Russian Poland, besides the frag-
ments of gneiss, granite, and other crystalline rocks, there are numer-
ous broken-up portions of sedimentary strata, many of which abound
in fossils. These fossiliferous erratics have long been studied by
German paleontologists, more particularly by the veteran author of
this work, and the present memoir, with its 11 lithographed plates
of the principal fossils occurring in the Boulder-clay, is intended as
a more complete description of them than that published by him in
1862.?

The author first gives a list of the principal memoirs which have
appeared on the subject since 1828, and then refers briefly to the
geological position of the Boulder-clay ; the state of preservation of
the boulders and fossils ; the geographical extension of the deposit ;
the different formations to which the erratics belong; the original
localities from whence they come; and the manner in which ‘they
have been transported to their present positions. Following this, is
a detailed description of the different species of fossils, of “the pre-
sent distribution of each in the Boulder-clay, and of the beds in
which the fossils now occur in other European areas.

The fossiliferous erratics belong to the Cambrian, Silurian,
Devonian, Jurassic, Cretaceous, and Tertiary formations. The most

1 Decade II. Vol. IX. p. 429.
* Zeitschrift der deutschen geologischen Gesellschaft, bd. 4, pp. 678.

386 Reports and Proceedings—Linnean Society of London.

abundant and widely distributed are boulders of limestone of Silurian
age, belonging to what is known as the Orthoceren-Kalk, the
Korallen-Kalk, and the Beyrichien-Kalk. The Silurian and Cam-
brian erratics have been brought partly from Sweden and partly
from the Russian Baltic provinces. Boulders of Devonian age are
_rare, and limited to the eastern provinces of Prussia; they have un-
doubtedly been derived from Livonia and Courland. Only a few
scattered fragments of Carboniferous and Permian rocks have been
met with, and their original localities are unknown; whilst Triassic
boulders appear to be entirely absent. Jurassic boulders are only
‘met with in the Hastern half of the Boulder-clay area, as far as the
Elbe. Their source is unknown, but they are most nearly related
to Jurassic strata in Courland. Cretaceous boulders extend over the
entire area; they belong both to the Cenomanian, Turonian, and
Senonian divisions; the most abundant are flints, probably derived
from the Chalk of Denmark and the South of Sweden. No erratics
are known from the Gault and the Neocomian ; but calcareous frag-
ments of Wealden age are met with in Brandenburg. These, how-
ever, do not correspond with the Wealden strata of N.W. Germany,
and their origin is unknown. ‘Tertiary erratics are rare and of
limited distribution, but fossil wood and amber are widely scattered
in the Boulder-clay. j

The direction in which the erratics have travelled is partly from
North to South, and partly from North-east to South-west. There
is no indication of any movement from N.W. to §.E., and no erratics
from Norway are met with in the Boulder-clay of Germany. The
author believes that the Boulder-clay has been distributed by floating
ice, a view which is opposed to that held by the large majority of
recent investigators of the subject, who maintain that it is due to the
direct action of glacial or inland ice. G. J. H.

REPORTS AND PROCHHDIN GS.
er er
I.—Linnean Society or Lonpon.
November 5, 1885.—Sir John Lubbock, Bart., M.P., F.R.S.,

President, in the chair.

The first part of an exhaustive Monograph “On Recent
Brachiopoda,” accompanied by illustrations, by the late Dr. Thomas
Davidson, F.R.S., etc., was read by the Secretary. In this the
author reviews the labours of his predecessors in the same field,
with regard to the shell, the anatomy of the adult animal, and
its embryology. As regards the perplexing question of affinities,
he remarks :—“ Now, although I do not admit the Brachiopoda
to be Worms, they, as well as the Mollusca and some other
groups of Invertebrates, may have originally diverged from an
ancestral vermiform stem, such as the remarkable worm-like
mollusc, Neomenia, would denote.” He lays stress on the Brachi-
opodous individual being the product of a single ovum, and not
giving rise to others by gemmation. He considers that the shell,

Reports and Proceedings—Scientific Society, Reading. ov

the pallial lobes, the intestine, the nerves, and the atrial system
afford characters amply sufficient to define the class. The greatest
depth at which a living species has been found alive has been 2990
fathoms. As to classification, he groups the recent species into two
great divisions: I. Anthropomata (Owen)= Clistenterata (King); II.
Lypomata (Owen) = Tretenterata (King). The Anthropomata he
divides into three families :—(1), Terebratulacea, with seven sub-
families and thirteen genera and subgenera, seventy species, and
twenty-one uncertain species; (2), Thecideide, with one genus and
two species ; (3), Rhynchonellide, one genus, one subgenus, and eight
species. The Zypomata he also divides into three families, five
genera and subgenera, twenty-three species, and seven uncertain
species:—(1), Craniide, with one genus and four species; (2),
Discimde, with one genus, one subgenus, and eight species; (3),
Lingulide, with one genus, one subgenus, and eleven species. He
does not accept M. Deslongchamps’ scheme (1884) of classifying
the Zerebratulina, bringing forward Mr. Dall’s observations on
Waldheimia floridana of delicate spicule in the floor of the great
sinuses as telling evidence against the arrangement. The various
genera and species are then dealt with, followed by remarks on the
Terebratulacee, with copious descriptions and observations.

T].—Reapine Lirrrary anp ScrentiFic Society, Oct. 13, 1885.

“On THE CoaL-FIELDS or THE Unitep Kinepom.” Inaugural
Address from the President, J. H. Buaxer, F.G.S., Associate
Mining Institute C.E., of H. M. Geological Survey of England.

The President remarked that the question as to the rapid exhaustion
or otherwise of our coal-fields was of national interest and importance.

Coal consists of indurated or mineralized vegetable matter, and

occurs in seams, interstratified in beds of sandstone, grit, shale, clay,

and ironstone, and more rarely of limestone. These together are
called the Coal-measures, which in some Coal-fields attain a thick-
ness of some thousand feet. Of the amount of vegetation required
to form not only one seam but forty or fifty or more, varying from
one inch to several feet in thickness, which often succeed each other
in Coal-fields, we can form no adequate conception, any more than
we can calculate the time required for their growth and consolidation.
Passing more or less through the stage of peat, each bed or mass of
vegetation got buried under successive sediments, and through the
influence of time, water, chemical changes and pressure eventually
became converted into coal. In Britain and elsewhere the Carbon-
iferous rocks, which were originally more or less horizontal, were
disturbed and thrown into a series of wave-like curves or contortions
together with other formations of older date. After this disturbance,
combined with faults or dislocations of the beds, denudation or waste
ensued, and the upper part of the curves being most exposed were in
many instances removed or worn away, the portion so removed
supplying material for newer strata. The lower part of the curves,
or basin-shaped portions, were preserved from destruction by their

38 Reports and Proceedings—Address by J. H. Blake.

position. During and after this waste of Carboniferous rocks the
Permian and other newer strata were deposited on the eroded edges
of the Carboniferous and other older strata, and these in their turn
also underwent disturbances in Britain in a minor degree followed by
denudation. Thus the Permian and other newer strata lie uncon-
formably on the Carboniferous and other older rocks. It is some-
times possible to estimate approximately and sometimes with cer-
tainty the area occupied by Coal-measures under the overlying
Permian and Secondary formations, by giving attention to the
“strike” and “dip” or inclination of the beds and by other means ;
and even to infer the basin-shaped form of a Coal-field, part of which
is concealed. It was by paying careful attention to physical pheno-
mena such as these and to details of stratification, the thickening and
thinning of the formations, their conformity and unconformity, the
occurrence of faults or dislocations and other disturbances, that the
Committee appointed by the Royal Commission were enabled to
estimate the amount of coal, namely, 56,273 millions of tons, which
probably exists at workable depths under the Permian, New Red
Sandstone and other superincumbent strata in the United Kingdom.
Of these 56,273 millions of tons, upwards of 23,000 millions were
estimated to occur under Yorkshire, and the remainder in varying
proportions from 85 millions in one locality to upwards of 5000
millions in another, under Warwickshire, Leicestershire, Staffordshire,
Denbighshire, Cheshire, Lancashire and a few other places in
England, and 27 millions in Ireland. In estimating the quantity of
available coal in the Coal-fields of the United Kingdom, the depth of
4000 feet was adopted by the Royal Commission as the limit of
practical working, and all seams or beds of less than one foot in
thickness were excluded from the returns. Having alluded at length
to the description of the Coal-fields of the United Kingdom, showing
approximately the probable quantity of available or workable coal
they contain, the lecturer summed up the calculations as follows :—
Wales 34,466 millions of tons, England 45,741 millions of tons,
Scotland 9845 millions of tons, and Ireland 155 millions of tons, a
grand total of 90,207 millions of tons. To this must be added the
56,273 millions of tons estimated to exist at workable depths under
the Permian, New Red Sandstone and other superincumbent strata,
making an aggregate of 146,480 millions of tons. From 1870 to
1884— fifteen years—nearly 2052 millions of tons have been pro-
duced in this kingdom. Mr. Godwin-Austen had shown that Coal-
measures, which thin out under the Chalk near Therouanne, probably
set in again near Calais, and are prolonged in the line of the Thames
Valley, parallel with the North Downs, and, continuing thence under
the valley of the Kennet, extend to the Bath and Bristol Coal area.
He showed upon theoretical grounds that the Coal-measures of a
large portion of England, France, and Belgium were once continuous,
and that the present Coal-fields were merely fragments of the great
original deposit preserved in hollows. These views, the lecturer
continued, are supported by many eminent geologists who gave
evidence before the Commission, but they did not receive the support

Reports and Proceedings—Geological Society of London. 39

of Sir Roderick Murchison. The question of coal being deposited in
the South of England is still a theory. Turning to the question of
the duration of the total available quantity, the lecturer said that
chiefly depended upon the statistics of consumption. In the year
1660 the coal produce of the United Kingdom was apparently only
about 24 millions of tons; in 1700 a little more than 23 millions;
in 1750 nearly 5 millions; in 1800 upwards of 10 millions of tons.
About this period the system of canal navigation was rapidly extended,
and the result was that coals were gradually finding their way into .
new districts, by which means the consumption of coal was greatly
increased. In 1816 the production reached probably 27 millions.
Advancing to a later period when coal statistics were more carefully
collected, it appears that in 1854 the production of coal was upwards
of 64 millions. From that period up to and including 1883, when
the production of coal in the United Kingdom reached the largest
quantity yet recorded, namely, nearly 1632 millions of tons, there
has been a progressive increase; except in the years 1857, 1858,
1874 and 1878, on which occasions there was a decrease varying
from about one to two millions as compared with the quantity raised
in the year immediately preceding these dates. Again last year
(1884) there was a decrease of nearly three millions of tons. What-
ever view may be taken of the question of the duration of coal, the
results will be subject to contingencies. On the one hand, the rate
of consumption may be thrown back to any extent by adverse causes
affecting our national prosperity, and on the other hand, new dis-
coveries and developments in new directions may arise to produce
a contrary effect upon the consumption of coal. Every hypothesis
must be speculative, but it is certain that if the present rate of
increase in the consumption of coal be indefinitely continued even in
an approximate degree, the progress towards the exhaustion of our
coal will be very rapid.tFrom the Reading Observer, Oct. 17, 1885.

IJ].—Geronoetcan Soctery oF Lonpon.
(1.)—Nov. 18, 1885.—Prof. T. G. Bonney, D.Sc., LL.D., F.R.S.,

President, in the Chair.—The following communications were read :

1. “ Results of Recent Researches in some Bone-caves in North
Wales (Ffynnon Beuno and Cae Gwyn). By Henry Hicks, M.D,
F.R.S., F.G.S., with Notes on the Animal Remains, by W. Davies,
Hsq., F.G.S., of the British Museum (Natural History).

This paper contained the results of researches carried on in these
caverns in the summers of 1885, 1884, and 1885 by Mr. E. Bouverie
Luxmore, of St. Asaph, and the author. The enormous collection
of bones belonging to the now extinct animals of Pleistocene age
obtained had been submitted for examination to Mr. W. Davies, and
afterwards distributed to various museums. Several well-worked
flint implements were also discovered in association with the bones.

The following are the conclusions arrived at by the author, from the
facts obtained during the explorations :—That abundant evidence has
been furnished to show that the caverns had been occupied by
hyenas, and possibly by other beasts of prey, as dens, into which

40 Reports and Proceedings—

portions of carcasses of various animals had been conveyed in Pleis-
tocene times. The very great abundance of some animals, such as
the rhinoceros, horse and reindeer, and the frequent presence of
bones belonging to young animals, proved that the plain of the Vale
of Clwyd, with that extending northward under the Irish Sea, must
have formed a favourite feeding-ground even at that time. The
flint implements and worked bones showed also that man was
contemporary with these animals. The facts perhaps, however, of
greatest importance, made out during these researches, are those
which bear on some questions of physical geology in regard to this
area, which hitherto have been shrouded more or less in doubt. The
views on the physical conditions in Pleistocene times of the areas in
North Wales in which these and the other bone-caverns occur, so
ably put forward by Sir A. C. Ramsay, appeared to the author to be
strongly supported by the results obtained in these explorations.
The ravine in which the caverns occur must have been scooped out
previous to the deposition in it of the glacial sands and Boulder-clays.
This sand and clay, there seems good evidence to show, must have
filled up the ravine to a height above the entrances to the caverns,
and such sands and clays are now found at some points to completely
fill up the caverns. How, then, did these sands and clays get into
the caverns? Were they forced in through the entrances by marine
action or by a glacier filling the valley? Or were they conveyed in
subsequent to the deposition of the Boulder-clay in the valley and
surrounding area? ‘The position of the caverns in an escarpment
of limestone, at the end of a ridge of these rocks, with a sharp fall
on either side, prohibits the idea that the material could have been
washed in from the higher ground, as has been suggested by some
in the case of other caverns, if it had anything like its present con-
figuration. Moreover, there is scarcely any deposit now visible upon
the limestone ridge, and there is no certainty that there ever was
deposited there any great thickness of such a clay as that now found
in the caverns. The general position also of the bones in some of
the tunnels seems to indicate clearly that the force which broke up
the stalagmite floor, in some places 10-12 inches thick, and stalac-
tites 6 to 8 inches across, which thrust many of the large and heavy
bones into fissures high up in the caverns and placed them at all
angles in the deposit, and must have acted from the entrance inwards,
and the only force which seems to meets these conditions is marine
action. The following seem to the author to be the changes indicated
by the deposits. The lowest in the caverns, consisting almost entirely
of local materials, must have been introduced by a river which flowed
in the valley at a very much higher level than does the little stream
at present. Gradually, as the valley was being excavated, and the
caverns were above the reach of floods, hyenas and other beasts of
prey occupied them, and conveyed the remains of other animals into
them. Man also must have been present at some part of this period.
Gradually the land became depressed, the animals disappeared, sta-
lagmite was formed, and the sea at last entered the caverns, filling
them up with sand and pebbles, and burying also the remains not

Geological Society of London. 41

washed out. Floating ice deposited in this sea the fragments of
rocks derived from northern sources, and these became mixed with
local rocks and clays brought down from surrounding areas. The
greater part of the Boulder-clay in the Vale of Clwyd was probably
deposited as the land was being raised out of this Mid-Glacial sea.
During the process of elevation the caverns became again disturbed
by marine action and the upper fine reddish loam and the la:ninated
clays were deposited. It seemed to the author impossible to avoid
the conclusion that these caverns must have been submerged, and
afterwards elevated to their present height of about 400 feet above
the level of the sea, since they were occupied by Paleolithic man
and the Pleistocene animals.

2. “On the Occurrence of the Crocodilian Genus Tomistoma in the
Miocene of the Maltese Islands.” By R. Lydekker, Esq., F.G-S.

The author described the anterior portion of the cranial rostrum
of a Crocodilian from the Miocene of Malta, to which Prof. Sir R.
Owen has given the MS. name of Melitosaurus champsoides. The
author considered that there were no characters by which the spe-
cimen could be generically distinguished from Tomistoma. Mention
was made of a second crocodilian skull from the Miocene of the
Maltese Islands, and of a third from Lower Austria, both of which
the author thought might be included in the same genus.

3. “Description of the Cranium of a new Species of Erinaceus
from the Upper Miocene of @iningen.” By R. Lydekker, Esq., F.G-S.

The author described the palatal half of the cranium of a large
species of Hrinaceus from the Upper Miocene of Giningen, which he
regarded as closely allied to the existing H. ewropeus, and proposed
to name H. ceningensis.

(2.)\—Dec. 2, 1885.—Prof. T. G. Bonney, D.Sc., LL.D., F.R.S.,
President, in the Chair.—The following communications were read:

1. “On some Borings in Kent.—A Contribution to the Deep-
seated Geology of the London Basin.” By W. Whitaker, B.A.,
F.G.S., Assoc. Inst. O.E. (Communicated by permission of the
Director-General of the Geological Survey.)

Seven deep borings in the eastern part of Kent were described, all
of them reaching to the Gault. The chief one is at Chatham Dock-
yard, where after passing through the whole thickness of the Chalk,
the Gault was found to be 193 feet thick; whilst the Lower Green-
sand was only 41 feet, and was underlain by Oxford Clay, a forma-
tion not before known in Kent.

These facts involve the thinning of the Lower Greensand from
200 feet at the outcrop a few miles to the south, and the entire loss
of the whole of the Wealden Series, which further south exists in
great force, the Weald Clay being 600 feet thick, or perhaps more,
and the Hastings Beds 700 feet or more.

Still further south, in the central part of the Wealden district,
there are outcrops of the Purbeck Beds, whilst the Subwealden
boring continues the series downwards. We have thus an addition

42 Reports and Proceedings—Geological Society of London.

to the beds wanting at Chatham of some 400 feet of Purbeck and
Portlandian, of over 1100 feet of Kimmeridgian, and of nearly 500 ft.
of Corallian, ete. In a section of 32 miles, therefore (the distance
between the Subwealden and the Chatham borings), we have a
thinning of beds to the extent of over 3400 feet, or at the average
rate of about 100 feet in a mile.

This northerly thinning agrees with the facts that have been
brought before us from other deep borings in and near London; but
the Chatham boring is the first in the London Basin in which a
Middle Jurassic formation has been found. The teaching of the
deep borings, as a whole, is that north of the Thames older rocks
rise up beneath the Cretaceous beds, whilst on the south newer rocks
come in between the two.

The question of the finding of the Coal-measures beneath parts of
the London Basin seems to admit of a hopeful answer, whilst the
lesson of the deep borings as regards water-supply is that there is
small chance of getting water from the Lower Greensand at great
depths underground.

It would be well if underground exploration could be conducted
on a systematic plan, with proper regard to both topographical and
geological considerations, and not left any longer to the chance work
of people in search of water.

2. “Note on some recent openings in the Liassic and Oolitic
Rocks of Fawler in Oxfordshire, and on the arrangement of those
rocks near Charlbury.” By F. A. Bather, Esq. (Communicated by
Prof. J. Prestwich, M.A., F.R.S., F.G.S.)

The river Evenlode rises in the Lower Lias of the Vale of Moreton,
traverses the range of Oolites, and joins the Isis opposite Wytham
Mill. lias is exposed to about three-quarters of a mile below
Fawler, where Great Oolite is brought down by a fault; and in the
Geological Survey map Lower Lias is brought down the valley to
within half a mile of Charlbury Railway Station.

In this paper the author gives reasons for believing that the dis-
tribution of the different beds constituting the Lias in the Evenlode
Valley do not agree with the Geological Survey map, nor with Prof.
Hull’s description, recent sections and borings made for clay, used in
brick- and pottery-making, having exposed Lower-Lias clay in a
brick-yard at Fawler, marlstone and Upper-Lias clay in a neigh-
bouring coombe, and in a long section 100 yards north of the
brick-yard Inferior Oolite comes in upon the Upper-Lias clay. On
examining the banks of the Evenlode north of Charlbury, it was
found that clays referred to in the Survey map to Lower Lias are
really Upper Liassic, being above the Marlstone, sections of which
are exposed near Culsham Bridge.

It was shown how these corrections in the mapping of the ground
are explained by the section along the line of the Evenlode and by
the dips of the beds.

Correspondence—Mr. H. B. Woodward-- Mr. Lydekker. 48

CORRESPONDENCE.

OLD RED SANDSTONE UNDER LONDON.

Srr,—In his paper “On the Nature and Relations of the Jurassic
Deposits which Underlie London” (Quart. Journ. Geol. Soc. vol. xl.)
Prof. Judd discusses the age of certain red rocks met with deep
down at Richmond, Crossness, and at Kentish Town. One question
that arose was whether rocks of the barren Old Red Sandstone type
and of the Devonian (Hifelian) type were likely to be met with in
close proximity. While admitting that, as in the Ardennes, so under
London, the lowest member of the Devonian (the Gédinnien of Belgian
geologists) may underlie strata of the Hifelian type; yet Prof. Judd
attaches much weight to the suggestion made by Mr. Whitaker that
rocks of Old Red Sandstone and Devonian type are not likely to
occur near together.

This suggestion is, however, opposed to what is well known in
Devonshire. There we have the Red Sandstones of Cockington near
Torquay, and the grits of Picklecombe and Staddon near Plymouth,
as well as the Pickwell Down Sandstones of North Devon, which,
as Mr. Champernowne remarks (Proc. Geol. Assoc. vol. vill. p. 469),
probably represent (both stratigraphically and lithologically) parts
of the Upper Old Red Sandstone. These strata are nowhere far
removed, geographically, from rocks of the Hifelian type.

Then, too, we have the Lower Devonian grits of Lincombe, War-
berry and Meadfoot in South Devon, possibly equivalent in part to
the Hangman grits of North Devon; but they are of a different
character from the rocks resembling the Upper Old Red Sandstone.
Prof. Prestwich has insisted on the resemblance of the Kentish Town
red beds to the (Upper) Old Red Sandstone of the Mendip Hills
(Judd, op. cit. p. 753).

Hence, without committing myself to any definite opinion on the
subject, there appears to me no reason why rocks of Old Red Sand-
stone type (whether Upper or Lower) should not occur, as well as
Devonian strata, under the London Basin. Recent researches, more-
over, tend to show that the Devonian (Hifelian) strata may bridge
over the interval between the Upper and Lower Old Red Sandstone.

Of course it is still open to question whether these red rocks under
London are Upper or Lower Old Red Sandstone, or New Red Sand-
stone (Poikilitic). Horace B. Woopwarp.

BRADFORD-oN-Avon, Nov. 1885.

THE “FAUNA ANTIQUA SIVALENSIS.”

Srr,—As your readers are doubtless aware, the atlas of Falconer
and Cautley’s “Fauna Antiqua Sivalensis”” was originally published
in separate parts, with paper covers bearing the date of publication of
each part; but as the work was never completed, no general title-
page ever appeared. In all copies in public libraries that I have
seen the atlas has been bound, and the original paper covers
destroyed, so that there is no means of knowing the date of publica-

44 Correspondence—Dr. Anton Fritsch.

tion of particular plates in which specific names make their first
appearance, and I have noticed in several instances that writers have
consequently been unable to give the exact date of publication
to such names. As I am fortunate enough to possess a copy in
which the original covers are preserved, I have thought it well to
record the dates of publication of the different parts, and the num-
bers of the plates contained in each, viz.—
1846. Part I. Plates 1—12.
» II. ,, 138—22 and 13a (double).

>)
NCEE TN IES waa TINS WIG TS 1 Cy AD ALIN mah TR. | TUS NS GI) AN,
ADIN DB. SLs BIN,
Me Nie 9 Sp BS} punish DI Ns SIN
” mg le oa) See
a De a iWila wate Md Geeen Ge

5 5 WIS 35 (BY @B:
y VUE 5, Oo GOS

99
1g4900 Mhoxe sie fois) oo)
Tue Lover, HarpenpEen, Herts. R. LypEKKeER.

FAUNA OF THE GAS-COAL OF BOHEMIA.

Sir,—In the Grotoercan Magazine for November, 1885, p. 527,
Prof. E. D. Cope, in a very kind mention of my work, “ Fauna der
Gaskohle in d. Kalksteinen d. Permformation Bohmens,” Prag, 1885,
asks why Ido not agree with him that Oricotus had the thoracic vertebrae
embolomerous. Having only had the opportunity of comparing the
figure of Oricotus, which I have reproduced on p. 4, band ii. heft i.,
J saw only the neural arches and the ribs, and on the lumbar
vertebrae some bodies which I was inclined to consider elements of -
rachitomous structure. I feel sure that in the rich material in Prof.
Cope’s hands he has evidence in support of his opinion that all the
vertebrae in Cricotus are embolomerous in structure.

Pracug, 3 Nov., 1885. Dr. Anton Frirscu.

ON SOME CRETACEOUS MADREPORARIA, BY MR. R. F.
TOMES, F.G.S.

Srr,—As Referee of the paper by Mr. R. F. Tomes ‘On some im-
perfectly known Madreporaria from the Cretaceous Formation of
England,’ which was withdrawn by the Author from the Geological
Society, and is printed in the Grotoetcan Macazine for December,
1885, p. 541, Pl. XIV. I take exception to the statement in brackets
in the concluding paragraph of the paper on p. 552, ‘‘It is now
printed verbatim with figures by Mr. C. Berjeau of the specimens
exhibited at that meeting,” as calculated to mislead. It is true that
the originals of some of the figures on the Plate accompanying the
paper were exhibited at the Meeting, but the original specimens of
Figs. 1, 2, 8, 4, 5, 6, were not shown on that occasion. Further, in
the Explanation of the Plate on p. 552, it is stated: “Fig. 7. Rhiz-
angia mamilliformis. Three corallites united by the stolon.” Fig. 8.
Ib. Two corallites similarly united.” In the originals, however,

The “ Ooming-of-Age”’ of the Geological Magazine. 45

which were exhibited at the Meeting, the corallites were not united
by the stolon, and they are not figured as united (in Plate XIV.
Figs. 7,8) in the Gronogrcan Magazine, though they were so
in the original drawing submitted to the Geological Society by
Mr. Tomes.

As these statements relate to matters of fact, I should feel obliged
if you would allow me this opportunity of rectifiying them in the
MaGazine.

“THE REFEREE.”

MISCHIOUAN HOUS.

THE ‘“COMING-OF-AGE” OF THE GEOLOGICAL MAGAZINE.

TESTIMONIAL TO THE Eprror, Dr. H. Woovwarp, F.R.S., F.G.S.

A meeting of the Subscribers to the Testimonial to Dr. H. Woodward,
F.R.S., for twenty-one years Editor of the GroLroercaL Macazing,
was held on the 15th December, 1885, at the Apartments of the
Geological Society, Burlington House, when Prof. T. G. Bonney,
F.R.S. (President Geol. Soc.), presented to that gentleman, on behalf
of the subscribers, a silver salver with a tea and coffee service and
a cheque for £255. On making the presentation, Prof. Bonney
addressed Dr. Woodward as follows :—

“Dr. WoopwarpD—

It is now rather more than twenty-one years since the GroLoGIcaL
MaGazine arose upon the foundation—I had almost said the ruins—
of an earlier publication. For the whole of that time you have been
one of its editors, for almost the whole its principal editor. On you,
though supported by the aid and counsel of most able coadjutors,
has fallen the chief burden of the work, the chief responsibility of
the undertaking. ‘

It would be difficult to appreciate too highly the aid which the
Grontocicat MaGazine has rendered to the progress of our Science.
It has supplied a want which had long been felt, which would at
once recur if it ceased to make its welcome monthly appearance.
There are many Geological notes and papers written, which, from
their brevity, from their interest being of a somewhat ephemeral
character, from their treatment being more historical or their aim
more controversial, are not exactly suited to the pages of the
Quarterly Journal of the Society in whose rooms we are assembled ;
yet the appearance of these in print is a boon to students and a
benefit to science. The GronocicAL Macazine thus occupies a
position, which, on one hand, has common ground with our
Quarterly Journal; on another, with the Proceedings of Local
Scientific Societies ; on a third with such a publication as “ Nature,”
but which is not exactly covered by any one of these. During all

ese years it has been an important aid to British Geologists, and

46 The “ Coming-of-Age”’ of the Geological Magazine.

I do but echo their sentiments when I wish it and its editor a long
and prosperous life.

But this, Dr. Woodward, is not the only service that you have
rendered to science. It is possible for an editor to nip early aspirations
in the bud and to petrify the neophyte in science by a cold breath
of disapproval or sarcasm, All, however, who, like myself, have
made in the pages of the Grorogican MaGazine their first venture
in scientific authorship, will be ready to testify to the kind welcome
and friendly encouragement which we received from you. Many,
I feel sure, have thus been animated to further efforts; so that you
may with just pride assert that under your auspices the GronogicaL
Magazine has enlisted many recruits for the great army of scientific
workers. Yet more, not only in its pages, but also at your place
in the British Museum, you have been ever ready to help the student,
and to place at his disposal, with unvarying kindness and courtesy,
the full stores of your ripe knowledge. This work, so far as the
GrEoLoGicaL Magazine is concerned, you have done, in reality, if
not in name, at your own cost. The small sum assigned to you as
Editor—inadequate at the best as a return for your labours, has
frequently been consumed by expenses which you have incurred to
increase—I had almost said to maintain—its efficiency. In this
wealthy country those who labour on behalf of science, especially
in regard to its literature, must generally be content to do it at
their own cost. You have done this ungrudgingly for so long a
time, though, as the chief bread-winner of a family, you might justly
have excused yourself from so unremunerative a task.

The sum of money which, on behalf of the Subscribers, I have the
pleasure of placing in your hands is no discharge of the debt which
is due to you from Geologists, but it may suffice to prevent you
from feeling that the members of your household have been serious
losers by your zeal for the progress of Science; and in asking you
to accept this small present of plate, your friends, for whom I
speak, wish to leave with you a more visible memorial of their
respect and regard. They trust it will remind yourself and the
helpmate who has shared your labours—remind you both, we trust,
for many years to come—that we were not wholly ungrateful.
But, even when the call to cease from work has sounded for those
chiefly interested in the friendly gathering of to-day, this little
memorial may avail to show your children how much their father
was esteemed, and may nerve them to emulate the example of their
parents.”

Dr. Woodward in reply said :—

‘‘Pror. Bonney anpD GunTLEMEN—

Words are but feeble vehicles in which to convey the warm feelings that rise in
my mind to-day, and strive for utterance in response to the eloquent eulogium you
have just delivered; and when I look at the munificent testimonial you have
presented to me, I am at a loss to conceive how my poor exertions as Editor of the
GzoLocicaL Magazine can have been deemed worthy of so high a recognition,

Of one thing I feel assured that I owe very much to the kind words which you,

The “ Ooming-of- Age” of the Geological Magazine. 47

Sir, expressed from this chair in reference to myself in your Presidential address in
February last, and I am grateful to learn how large a number of my friends have
inscribed their names to this very handsome gift, which will be to me a lasting token
of their regard and friendship, and for my children after me.

The Gzotocrcan Macaztne is not by any means the earliest periodical specially
devoted to geology, although it may very justly claim to have survived for a longer
period than either of its predecessors.

The first attempt was made by Mr. Edward Charlesworth, F.G.S., who commenced
“The London Geological Journal” in September, 1846. Three very excellent and
richly illustrated Numbers appeared in September, 1846, and February and May, 1847,
when it expired—probably from want of funds. The veteran Editor still survives,
and so also do three of his contributors, Prof. Morris, Mr. James Carter of Cam-
bridge, and Mr. William Cunnington, F.G.S., formerly of Devizes, Wilts.

The “ Geologist,”’ edited by Mr. S. J. Mackie, was commenced in 1858, and after
five years and a half was merged (by purchase) in the GEotocican MaGazine in
July, 1864.

It is pleasant to observe amongst the contributors to the first volume of the
“< Geologist’ in 1858, the names of the Rey. P. B. Brodie, Prof. J. Morris, Prot.
Rupert Jones, Prof. (Sir) A. C. Ramsay, and Prof. Prestwich, names still prominent
on the ‘‘roll-call ” of eminent /iving geologists.

It is gratifying to know that for the past 21 years I have carried with me so large
and influential a body of supporters, beth at home and abroad.

But of the friends who stood beside us at the outset of our enterprise, many have,
alas! left us and “ gone with the great departed into the Silent Land.”

I rejoice, however, that Sir Richard Owen, Sir A. C. Ramsay, Dr. A. Geikie,
Professors Huxley, Prestwich, Rupert Jones, Morris, Boyd Dawkins, Ruskin,
Edward Hull, H. G. Seeley, Bonney, Nicholson, Dr. John Evans, Mr. Etheridge,
Mr. Topley, Mr. H. M. Jenkins, Mr. Kinahan, Mr. Meyer and many others amongst
my first contributors, are still with us; nor have we lacked very many new and able
friends who have helped us through what may be termed the “ renaissance period,’’ or
middle-age of our existence, and have continued to stand by us manfully until the
present day.

Glancing for a moment at the period embraced by the joint volumes of the
**Geologist’’ and the Grotocican Macazine combined (i.e. 28 years), we have
witnessed in that quarter of a century some of the greatest advances which have ever
been made in our science.

The dissemination of the Darwinian theory of Evolution has made the long-buried
past of Geological history only an early chapter in the life of our earth, and Paleon-
tology and Zoology have clasped hands never to be again disassociated.

The past quarter-century has also revealed to us that wonderful chapter in the
History of Early Man as displayed in the Old River Valley Gravels, Brickearths, and
Peat Deposits, in the Bone-caves, Rock-shelters, Kitchen-middens, Lake-dwellings,
and other Quaternary records of our Race, bringing into prominence the latest
chapter of Geology which ‘ dovetails’ the ‘ prehistoric’ with the ‘ historic’ periods.

The time would fail to tell of the progress of our science in a better knowledge of
Physiography, of ‘* Climate and Time,” the ‘‘ Great Ice-Age,” the Study of Karth-
quakes and Volcanoes; the Depths of the Sea; the Formation of Mountain Chains;
of Metamorphism; Atmospheric Denudation ; of the Continuity of Matter. Lastly,
but most important, both for organic and inorganic studies, has been the grand
development of Microscopic research as applied both to Palseontological and Minera-
logical studies, with which the names of our past President H. C. Sorby, and our

48 The “ Coming-of-Age’’ of the Geological Magazine.

present President Prof. Bonney, will always be associated, and for which the Royal
Microscopical Society and Mr. Frank Crisp have laboured energetically and long.

Probably no better sign of the utility of the Gzrorogican Macazine could be
given than the fact of the abundant supply of materials to fill its pages which the
Editor receives.

Having started the present serial in 1864, it is very agreeable to be able to state
that after the first year, during which my friend Prof. Rupert Jones undertook (at
Messrs. Longmans’ request) the task of Chief Editor—I have had the sole charge of
the GronrocicaL Macazine and have passed each number through the press myself,
nor have I relegated the duty to other hands on a single occasion.

Like other ephemerides, the GEoLocrcan Magazine has had its periods of financial
depression. At 18 months it was given over for dead by its first publishers (Messrs.
Longmans & Co.), and again at 10 years old it hardly seemed likely to pull through,
and Messrs. Triibner & Co. were rather doubtful as to the advisability of letting it go
on; but thanks to the generous support of friends, it recovered from both crises and
has still, I trust, the promise of many years of usefulness before it.

Having arranged its contents month by month for so many years, with my own
hands, I have sometimes imagined it to be all my own; but it would indeed be a
miserable failure were it not for the long list of distinguished contributors whose
papers give value to its pages, and without whom the Gronoeican Macazine would
years ago have ceased to exist.

As regards its financial position, the Gzotocrcan Macazine has the disadvantage
of beimg a Class-periodical — appealing only to Geologists, Palsontologists, and
Mineralogists.

The ‘‘ Annals and Magazine” and ‘ Silliman’s Journal ’ have much broader bases,
taking cognizance of all branches of Natural History, and, in the case of Silliman, of
Chemistry and Astronomy also.

But notwithstanding our limited sphere, we have been able to sustain life for
21 years, and a few degrees of warmth on the part of our geological friends, in adding
to our list of subscribers, would produce a marvellous effect in an increased circulation,
gratifying alike to Publishers, Printers, Artists and Editor, who have done their best
to keep the production of the Gzotocican MaGazine up to the standard of the
present time.

If any stimulus were needed by myself as Editor, my friends have this day applied
it in the form of a very substantial recognition of my services, for which I am bound
to reiterate my warmest and most sincere thanks. I trust, Sir, that you will long
continue, with my other friends, to give me that kindly aid and support which is so
essential to the future success of the GroLtogican Macazinz.

Work on British Purrograrny.—Messrs. Watson Bros. and
Douglas, of Birmingham, announce the publication of a work on British Petro-
graphy, being a Description of the Ordinary Rocks of the|British Isles, by J. J.
Harris Teall, M.A., F.G.S., etc., illustrated by 50 Chromo-Lithographic plates
from original drawings of typical microscopic slides. ‘To be completed in 25 Imperial
Octavo Monthly parts, including 100 figures and about 350 pages of text. ‘The first
part is announced to be published in February next. From a previous acquaintance
with Mr. Teall’s able and careful labours in petrography, we anticipate that this
work will be a most valuable Book of Reference for the use of Professors and
Lecturers in Geology and Petrography, and for all who are interested in the study of
British Rocks.

“DIMIUE “AT'S (QQ ‘Buruoty udayp4ony ‘Ursvg UAOZ]-S1G ‘2uaI0q yIvsv4JY
‘adoy ‘suanusg snposmuayg fo uojajayS

“ SS

= SS

te wer ON

\
~ \ | a

LLL,

YY}

Yl
fv Uf

ee

YY

\\ j io
MQ & WA
\w \\_\yy_\T

Td To Si avon ‘O88I “SVIN “10x

THE

GEOLOGICAL MAGAZINE.

NEW SERIES. \DECADE, Tile VOEs- Itt.
No. II.—FEBRUARY, 1886.

Ore aeaNPASE, PASE ae CGrbeEn Ss

I.—Pror. H. D. Cors, on A New Tyre oF PerissopactyLe Uneou-
LATE FROM THE WasatcH Hocene or Wyomine TERRITORY,
Unitep States oF NortH AMERICA.

(PLATE II.)

N his last published volume on the Vertebrata of the Territories,’
Prof. Edward D. Cope has figured and described many new
and remarkable forms of the Order Uneutata from the Eocene of
Wyoming. The most important and interesting among the numerous
species described being the genus Phenacodus, of which the nearly
entire skeletons of two species have been discovered, namely P. pri-
meevus, represented in our plate (Plate II.) and P. Vortmani. So
far as the present evidence goes, Phenacodus appears to have been the
most generalized form of a Perissodactyle Ungulate hitherto described,
though other contemporary genera may ultimately show characters
as generalized, when the relation of those species founded upon the
dentition to those founded on the detached bones of the extremities
is better known. The teeth of Phenacodus are tuberculated, with
intervening valleys, resembling the dentition of some of the bunodont
Artiodactyla, whilst the femur has a third trochanter, and the fore and
hind feet have each five well-developed digits, showing it to be a
Perissodactyle or odd-toed ungulate.

Again, the scapula is widened anteriorly, as in the Ursine Carnivora,
the Amblypoda and Proboscidea. With the last group the form of
the ulna also coincides, being large and broad relatively to the radius,
and also in that the bones of the carpus do not interlock.

From these coincidences of structure Prof. Cope says, ‘‘ This genus
must be placed in a special group of an order which includes the
Proboscidea”’ (p. 383). On the other hand, in a lecture on the Horse,
recently delivered at the City of London Institute, Prof. W. H.
Flower, LL.D., F.R.S., infers, from certain structural characters, that
it was an early ancestor of the Hquide. However, the following
general description of the genus (extracted chiefly from the “ Ameri-
can Naturalist,”* and reproduced again in Prof. H. D. Cope’s later
and grander work) will better serve to convey, in the author’s own

* “Report United States Geological Survey of the Territories,’ F. V. Hayden.
vol. iii. ‘* The Vertebrata of the Tertiary Formation of the West,’’? Edward D.
Cope. Washington, 1884 (inner title 1883) ; 4to. pp. xxxiv. and 1009; plates 75,
several folding.

* The American Naturalist, vol. xv. 1881, p. 1017.

DECADE III.—vVOL. IUI.—NO. II. 4

50 Prof. E. D. Cope—A New Perissodactyle Ungulate.

words, the leading facts in reference to this remarkable Eocene
Mammal.

“A New Types or PERISssODACTYLE UNGULATE.

In a paper on the ‘Homologies and Origin of the Molar Teeth of
the Mammalia Educabilia,’ published in March, 1874, I ventured
the generalization that the primitive types of the Ungulata would be
discovered to be characterized by the possession of five-toed planti-
grade feet, and tubercular teeth. No Perissodactyle or Artiodactyle
mammal was known at that time to possess such feet, nor was any
Perissodactyle known to possess tubercular teeth. Shortly after
advancing the above hypothesis, I discovered the foot structure of
Coryphodon, which is five-toed and plantigrade, but the teeth are
not of the tubercular type. For this and allied genera, I defined
a new order, the Amblypoda, and I have published the confident
anticipation that genera would be discovered which should possess
tubercular (bunodont) teeth. This prediction has not yet been
realized. I now, however, record a discovery, which goes far to-
wards satisfying the generalization first mentioned, and indicates
that the realization of the prophecy respecting the Amblypoda is
only a question of time.

In 1873 I described, from teeth alone, a genus under the name of
Phenacodus, and although a good many specimens of the dentition
have come into my possession since that date, I have never been
able to assign the genus its true position in the mammalian class.
The teeth resemble those of suilline Ungulates, but I have never had
sufficient evidence to permit its reference to that group. Allied
genera recently discovered by me have been stated to have a hog-
like dentition, but that their position could not be determined until
the structure of the feet shall have been ascertained.

In his recent explorations in the Wasatch Eocene of Wyoming,
Mr. J. L. Wortman was fortunate enough to discover a nearly entire
skeleton of a Phenacodus very near the typical P. primevus, which
presents all the characters essential to a full determination of its
place in the system. The unexpected result is, that this genus must
be referred to the order Perissodactyla and the Proboscidea, and
that, with its allies, it must form a special division of that order
corresponding in the tubercular characters of its teeth with the
bunodont or suilline division of the Artiodactyla. In this character,
however, there is a closer gradation than in the case of the
Artiodactyla, and it would scarcely be necessary to create such a
group on that character alone. But the genus differs further from
the Perissodactyla and approaches the Proboscidea, in the fact. that
the astragalus articulates with the navicular only, and by a
universally convex surface, as in the Carnivora.

The astragalus resembles that of the latter order very closely, and
differs from that of Hyracotherium and the nearest forms among the
Perissodactyla. Phenacodus has, moreover, five well-developed toes
on all the feet, and was probably not entirely plantigrade. ‘The cast
of the brain-case shows that the cerebral hemispheres were quite
small and nearly smooth, and that the very large cerebellum and

Prof. HE. D. Cope—A New Perissodactyle Ungulate. 51

olfactory lobes were entirely uncovered by them. The bones of the
two carpal rows alternate with each other, and there is a third
trochanter on the femur. The cervical vertebra are opisthoccelous.
The systematic position of the genus may be schematically represented
as follows:

Order Prrissopactyza. Ungulate; digits of unequal lengths ;
carpal bones alternating; a postglenoid process. Astragalus with
proximal trochlea, and without distal double ginglymus.

Suborder Diplarthra. Astragalus distally plane or concave in one
direction, and uniting with both navicular and cuboid bones; a
third trochanter on the femur. The known families belonging here.

Suborder Condylarthra. Astragalus convex in all directions
distally ; only uniting with navicular bone; a third trochanter on
the femur.

Family Phenacodontide. Molar teeth tubercular; the premolar
teeth different from the molars; five digits on all the feet.

Genera: Phenacodus, Cope, and very probably Catathleus,!
Mioclenus, and Protogonia,? Cope; and perhaps also Anisonchas,
Cope. These genera include fifteen species, all from the Lower
Hocene beds. The Condylarthra are then the ancestral type of the
known Perissodactyla, that is, of the Horses, Tapirs, and Rhinoceroses,
and of the numerous extinct forms.”

Prof. Cope arrives at the following conclusions as to the measure-
ments of the entire animal as figured (see Plate II.). ‘The measure-
ments of Phenacodus primevus show that this species was as large as
a ‘Big-horn’ ;* that its body was rather longer than in that animal,
and its legs shorter and more robust. It was in fact proportioned
more as in the common American Tapir, but was of smaller size.
The middle three toes of both feet reached the ground, whilst the
first and fifth projected laterally and posteriorly, like the dew-claws
of the Hogs. The tail was longer and heavier than that of any of
the living hoofed mammals, resembling in its proportions that of the
Wolf. The eyes were small and the muzzle long, but was singularly
soft above and near the extremity. Whether this soft part was
pierced by valvular muscles, as in the Hippopotamus, or was produced
into a short proboscis, as in the Saiga (Antelope) or in the Tapir,
cannot be certainly ascertained, but there are indications of the
insertion of important cartilages, if not muscles, on the superior
faces of the premaxillary bones.

The animal was probably omnivorous in its diet. It was not
furnished with any weapons of offence or defence pertaining to the
osseous system, so that it must have sought refuge in flight. The
well-developed muscular insertion of its limbs, and the digitigrade
character of its step, indicate that it may have had considerable
speed.”

“« Distribution.—The bones of this species have been found wher-
ever the beds of the Wasatch Epoch occur, but most abundantly in

1 American Naturalist, October, 1880.
* Proceedings American Philosophical Society, September, 1881.
3 Ovis Canadensis, ‘‘The Rocky Mountain Sheep.”

52 Prof. P. Martin Duncan—On Cretaceous Madreporaria.

Northern Wyoming. From the Wind River Valley Mr. Wortman
brought two specimens, and ten from the Big-Horn Basin.” (op. cit.
pp. 462-463).

Nore.—We are indebted to the kindness of Prof. E. D. Cope for

permission to reproduce the figure of Phenacodus given in our Pl. II.
—Eprr. Gron. Maa.

I].—Aw Answer To “OxsserRvATIONS ON SomE ImpeRFectty Known
MapREPORARIA FROM THE Cretaceous Formation oF ENGLAND,
By R. F. Tomess, Esa., F.G.S.”

By Prof. P. Martin Duncan, F.R.S.

HEARD this communication read at the Geological Society in
June last, and I made some remarks upon it which are noticed
in the Proceedings of the Society. A considerable portion of the
paper consisted of criticisms of some of my work which appeared
in the British Fossil Corals (2 ser. Pal. Soc. part ii. Nos. 1 and 2,
1869-70). Some specimens were exhibited, in the author’s absence,
which were presumed to afford evidence of a satisfactory kind. But
it was observed that the very imperfect and bad condition of the
fossils did not substantiate the author’s statements. Many specimens
which ought to have been exhibited were not before the Society, and
yet the classificatory position of some very rare corals could then
and there have been settled. As this paper was not published by
the Geological Society, as the author ignores the remarks I made on
the paper, and as it appears in the Gronocrcan Magazine for
December, 1885, p. 541, I ask a small space for a reply.

In answer to Mr. Tomes, I assert that Micrabacia Fittoni, nobis
(Pal. Soc. loc. cit. p. 37, pl. xiv. figs. 6, 7, 8, 9), is not a variety of
Cyclocyathus Fitton, Edw. and Haime (Pal. Soc. Brit. Foss. Corals,
pt. i. p. 63, pl. xi. figs. 38, 8a, 3b, 1850). Neither is it that species.
The species of M. Fittoni was founded upon a solitary yet good
specimen, and the drawings of it were good and from nature. Some
years after the description of the species, I investigated the mor-
phology of Micrabacia coronula, and the results were published
(Quart. Journ. Geol. Soc. vol. xl. 1884, p. 561).’ I pointed out that
there was reason to doubt whether M. Fittoni was a true Micrabacia ;
but that as the type was not accessible, I did not feel disposed to
remove the form until I had an opportunity of investigating it anew.
It was, however, not necessary to place the form out of the Fungida,
to which section it belongs. J should have been glad to have seen
another specimen, but Mr. Tomes did not give me the opportunity,
and I am aware that he has not the type. So it is now necessary to
compare the form I described with the species with which it is
attempted to be associated, namely, Cyclocyathus Fittont.

Amongst the structural details of Cyclocyathus Wittoni, Edw. and
Haime, is a thin epitheca, and the coste of the first and second
cycles are more prominent than the others; these details are not seen
in M. Fittoni. The upper or calicular surface is rather convex

1 Omitted be to noted by Mr. Tomes.

Prof. P. Martin Duncan—On Cretaceous Madreporaria. 53

externally and concave towards the centre, and the fossa is large
and well marked, whilst the columella is fasciculate, broad, and
papillose at the surface in Cyclocyathus; but in Micrabacia
the corallum is hemispherical and there is no large fossa in the
entirely convex calice, and the small columella has no papillz. There
are pali and no synapticule in Cyclocyathus, and there are no pali
and many synapticule in Micrabacia.

The student of the Madreporaria who will turn to the figures of
the types of the two forms in the Pal. Soc. loc. cit. will have no
difficulty in recognizing their distinctness. Cyclocyathus is an
aporose coral, and Micrabacia is a true Fungid. Mr. de Wilde
drew M. Fitioni, nobis, from nature.

Smilotrochus insignis, nobis (Pal. Soc. loc. cit. p. 37, pl. xiv. fig. 18,
1870). This is stated by Mr. Tomes to be a Ceratotrochus. The
morphology of Smilotrochus and Ceratotrochus was considered in my
«Revision of the Genera and Families of the Madreporaria” (Linn.
Soc. Journ. Zool. 1884), and it is noticed that Ceratotrochus is a
Smilotrochoid with a columella. The columella of this genus is
bundle-shaped and broad (fasciculate),1 and processes arise from the
inner edges of the larger septa and ascend into it and add to its bulk.
The top of the columella is papillary and high up in the coral. The
specimen with a so-called columella I had not the advantage of
seeing, but there is a drawing of it in Mr. Tomes’s paper (GEoL.
Mac. 1885, Pl. XIV. Fig. 6), and it is evidently a diagram.
What is considered to be the columella is not a fasciculate structure
gaining processes from the septa, nor is it a spongy columella, but a
mass of matrix which always fills up the lower parts of these corals.
The mass occupies the axis, and the rounded top is artificial.
Smilotrochus insignis, nobis, is not a Ceratotrochus, and one of the
reasons is that it has no columella.

Smilotrochus granulatus, nob. (op. cit. p. 36, pl. xiv. fig. 17). This
is said by Mr. Tomes to be an immature Trochocyathus Wiltshirei,
nobis. I should have been glad to have seen a specimen of the
interesting T. Wiltshirei, and still more to have seen the proofs that
a well-characterized Smilotrochus without columella and pali could
become a form with those essential characters in the growth of one-
tenth of an inch, and also increase from three to four cycles in the
same space. The height of the type T. Wiltshirei, nob., is three-
tenths of a inch, and that of the Smilotrochus is two-tenths of an inch.
The cyclical arrangement and the nature of the coste and of the
calice distinguish the two forms perfectly. There is no evidence that
one form could turn into another, and the species Smilotrochus granu-
latus, nobis, is not the same as 7’. Wiltshirei, nobis, for it has neither
columella nor pali.

Podoseris mammiliformis, nobis, and P. elongata, nobis (Pal. Soc.
loc. cit. p. 25, pl. ix. figs. 2-17). These species are stated to be
species of Rhizangia, Ed. and H. To disprove this it would suffice
to draw attention to the above-mentioned figures of the types and to
the figures given of Rhizangia by Reuss (Denks. d. Wien. Akad. der

1 Not spongy as Mr. Tomes states,

o4 Prof. P. Martin Duncan—On Cretaceous Madreporaria.

Wiss. t. vii. p. 120, pl. 7, fig. 7, 8, and fig. 9-11; also M. Hd. and
Haime, Ann. des Sci. Nat. 3rd ser. t. x. pl. 7, fig. 7 and 8); but it is
as well to call attention to the fact that perfect specimens of Podoseris
have convex and more or less hemispherical upper surfaces, and that
their bases are perforated, whilst there are synapticule between the
septa. The form is not a social one, and never springs from stolons
like Rhizangia, which has a wall, a flat upper surface with a shallow
calice, and is seated upon a stoloniferous base which may extend
beyond and give origin to others.

The figures given by Mr. Tomes (7 and 8) show that there are no
stolons present. A stolon is a structure on which the bases of coral-
lites grow, and it is not a growth from the edge of the base of a
corallite. In the very numerous specimens of Podoseris from the
Red Chalk which the Rev. Mr. Wiltshire placed at my disposal there
were no traces of stolons. No union by stoloniferous growth existed
in the specimens which were exhibited by Mr. Tomes at the Geol.
Soc., and although he states that “three corallites are united by the
stolon” (p. 552), it does not appear in the illustration (Fig. 7). I
especially drew attention to the want of stolons and such union in
the remarks I made on Mr. Tomes’s paper at the Geological Society,
and my remark was published in the Abstract of Proceedings.
Nevertheless, Mr. Tomes persists in stating what he cannot sub-
stantiate.

I draw attention to Mr. Tomes’s Fig. 10, which professes to repre-
sent synapticule. On Plate XIV. is printed “R. F. Tomes, del.,” so
that this is not a mistake of the artist. The figure proves that its
author has views regarding the nature of synapticule which are not
those of any other zoophytologist. Synapticule pass from one
septum to another. In Fig. 9, synapticulee are called dissepiments.
Figure 11 of the Plate is acknowledged to be wrong, and should not
have been printed, for it leads to a mistaken view of the structures it
purports to represent. Syzygophyllum, Reuss, is not in the least
like a Podoseris, and is synonymous with Antillia, nobis, a sub-
genus of Circophyllia; it has no stolons. Podoseris is a well-defined
natural genus and is one of the Fungide, and Rhizangia is one of the
Aporosa.

Turbinoseris, nobis (“Revision of the Genera,” p. 148). This genus
is stated by Mr. Tomes to be synonymous with Leptophyllia, Reuss.
They are distinct for morphological reasons. Pratz in his article
(Paleontographica, 1882, p. 90) has shown that the septa of Lepto-
phyllia are numerous, thin, often uniting and composed of vertical
trabeculee with vertical rows of perforations between them. It may
be remarked that this lattice-work condition is not the result of
fossilization or weathering, but that it is normal, and necessitates the
species being placed with Cyclolites and other forms in a special
family of the Fungide.

Turbinoseris has many species, and I have described them from
the West Indies and from Sind, besides from the British Cretaceous.
In all, the septa are solid, and that is sufficient to separate the two
genera. Turbinoseris remains a member of the Lophoserine group

MM. Reid & Sharman—On the so-called “* Gault” in Norfolk. 55

of the Fungide. Turbinoseris de Fromenteli, nobis, therefore retains
its title, and Mr. Tomes cannot term it Leptophyllia Anglica, Tomes.

Mr. Tomes remarks (p. 545), “Some other compound corals have
been collected at Haldon which, from their unsatisfactory condition,
cannot be determined, though I believe them to be new. As the
Haldon corals are only casts, they cannot be trusted when internal
structure is important. The genus Haldonia is in my opinion a very
doubtful one. Specimens in my own collection from Haldon differ
in the important respect of sometimes having a styliform columella,
and sometimes only a ring of pali, as in Prof. Duncan’s figures.”
Haldonia was described and figured by me (Quart. Journ. Geol. Soc.
1879, vol. xxxv. p. 91), and like all the other forms I studied was
not in the form of cast. Haldonia Vicaryi, nobis, was described from
perfect specimens, and they had no columella. Corals of the same
species, so far as my experience helps me, do not sometimes have a
columella, and sometimes not and only pali. Probably the specimen
seen by Mr. Tomes with a columella was the well-known Actinacis
of Haldon.

I draw attention to the figures on the Plate (Groz. Mac. 1885,
Pl. XIV. Figs. 14-15), and protest against species being determined
from such fragments.

Finally, on looking at Fig. 138, which is said to represent a
Pleurosmilia, it will be noticed that the columella does not terminate
by uniting with one of the principal septa which is more developed
than the others. The form does not belong to that genus, but to
Placosmilia, Ed. and H.

Summary, Ere.

Smilotrochus insignis, nobis, non Ceratotrochus insignis.

granulatus, nobis, non Trochocyathus Wiltshiret.
Micrabacia Fittoni, nobis, non Cyclocyathus Fittoni, Hd. and H.
Podoseris mammiliformis, nobis, non Rhizangia mammiliformis.
elongata, nobis, non Rhizangia elongata.

Turbinoseris de Fromenteli, nobis, non Leptophyllia Anglica, Tomes.
Pleurosmilia neocomiensis, E. de From. fide Tomes, is Placosmilia.
Haldonia, nobis, has no columella.

Syzygophyllum, Reuss, non Rhizangia, Wd. and H.

II1.—On THe so-caLLep “Gautt” or West Derenam, IN NoRFOLE.

By Crement Rerp, F.G.S., and Groner SHARMAN.
(Published by permission of the Director-General of the Geological Survey.)

INCH the publication of William Smith’s Map of Norfolk in
1819, the sections around West Dereham and Shouldham have
been accepted as proving the occurrence of true Gault’ in this part
of West Norfolk. Messrs. Rose,’ Fitton,’ and later writers, all

The Kimmeridge Clay is also locally known as ‘‘ Gault.”
Phil. Mag., series 3, vol. vii. pp. 171—182.
Trans. Geol. Soc., series 2, vol. iv. p. 312.

worn re

56 MM. Reid and Sharman—

accept this determination. Mr. Teall,’ writing in 1878, points out
the close relation of the fossils from the ‘‘Coprolite Bed” of West
Dereham to those of the “‘ Ammonites mammillaris zone ” of Folke-
stone, and correlates the overlying blue marly clay with the Gault,
from the occurrence in it of Ammonites interruptus.”

However, during the Geological Survey of this neighbourhood,
great difficulty was found in separating the so-called “Gault ” from
the Chalk Marl, and after a minute examination of the whole district,
the only boundary-lines which could be traced were, a distinct
line of erosion below the “Coprolite Bed,” and a lithological line
where the hard Chalk rests on the Chalk Marl. Though close
search was made for the more or less phosphatic bed which in many
other parts of England marks the base of the Chalk, no trace of it
could be found, and the conclusion could not be avoided, that the
so-called Gault was both lithologically and stratigraphically merely
part of the Chalk Marl.

The new Coprolite Works lately opened at West Dereham show
the best sections of the Phosphate Bed, and of the Marl immediately
overlying it; but the Marl there is very thin, being partly cut out
by Boulder-clay. In October, 1883, the section seen in the well was:

Ft. in.

( 5. Boulder-clay, very chalky ... ... ... .. 7 O

CHaLk Maru 4. Blue Marl, drying bluish white soo ke ID

|e Comotie Bal oo 0 9

N 2 0
NEOCOMIAN ...

1. Running Sand

The other parts of the works are on lower ground, and show less
Boulder-clay ; though the Marl is about the same thickness, except in
one place, where Boulder-clay cuts through it into the Greensand,
and in other parts where the Coprolite Bed approaches the surface.

Taking the beds in order, No. 1 is undoubtedly Neocomian,
though here it has yielded no fossils. No. 2 is probably also
Neocomian, which has been slightly disturbed, reconstructed during
the deposition of the overlying beds, and subsequently hardened by
infiltration.

No. 8 is the bed for which the deposit is worked. It consists of
a mass of phosphatic nodules in a greenish loamy or sandy matrix,
partly derived from the underlying Neocomian Beds. Mixed with
and occasionally imbedded in the nodules are numerous fossils.
These fossils seem to be mainly derivative, for though most of them,
as Mr. Teall has pointed out, belong to the zone of Ammonites
mammillaris, there is apparently also an occasional admixture of
older and newer forms, including some species, such as Dentalium
ellipticum, probably belonging to the Gault.

The “Coprolite” occurs in this bed in two forms. The more
abundant is a poor sandy phosphate in irregular nodules, which may
have been partly formed in the bed itself. These seldom contain
fossils. The associated mollusca are generally either loose casts, or
are imbedded in a sandy matrix which has not been phosphatized,

1 The Potton and Wicken Phosphatic Deposits, 8vo. pp. 20, 21.
* See also Keeping’s Neocomian Deposits of Upware, etc., 8vo. pp. 11, 64.

2. Hard loamy nodular Greensand

On the so-called “ Gault” in Norfolk. 57

though the shells themselves are usually coated internally with a
smooth-grained black phosphate. Unfortunately, in so coarse a bed
there is not much chance of finding the contemporaneous fauna
preserved, and as nearly all the collecting has been done after the
material has been roughly washed by machinery, any con-
temporaneous shells have probably been entirely destroyed.
Collecting small fossils before the bed is washed is also very difficult,
for it is impossible to see any, and the phosphate bed is not left to
the action of the rain, but is immediately carted away.

Leaving, therefore, the Phosphate Bed, which, though strati-
graphically merely the basement-bed of the overlying Marl, cannot
yet be proved to be so by evidence of the fossils, the undoubtedly
contemporaneous shells of the underlying 3 or 4 feet of Marl (No. 4
of the section) were carefully collected and examined. The result
showed, that while at first sight there was abundance of evidence for
the correlation of the Marl with the Gault, yet closer examination
proved the Gault fossils to be derived, and the contemporaneous
fauna to belong to the Chalk Marl.

The following is a complete list of the fossils obtained in the Marl
at West Dereham Coprolite Works—nearly all of them were found
within two feet of the Coprolite Bed :-—

Pentacrinus, sp. Nucula pectinata, Sow. (cast).
Pseudodiadema, spine. Pholadidea? in wood.
Serpula, sp. Dentalium ellipticum, Sow. (casts).

Ammonites interruptus, Brig. (casts).
Terebratula biplicata, Sow.
Rhynchonella, sp. Belemnites attenuatus, Sow.
minimus ? List.

Anomia, sp. ultimus, D’ Orb.
Exogyra haliotoidea, Sow. Hamites, sp. (cast).
Ostrea acutirostris, Nilss.
vesicularis, Lam. Beryz, sp. (in light-coloured phos-
Plicatula, sp. hate).
Pecten orbicularis, Sow. Cymolichthys 2? (Saurocephalus)
quinquecostatus, Sow. striatus, Ag.
Inoceramus, sp. Odontaspis gracilis, P. & C.
Lima, sp. Pycnodus, sp.

Of these the most conspicuous and easily found, except the Belem-
nites, is Ammonites interruptus, which is a characteristic Gault form.
But this species, and also Hamites, Dentalium ellipticum, Nucula
pectinata, Pholadidea, and the fish are all phosphatized, and usually
rolled. They are probably derived from the Gault. The rest are
white and unphosphatized, and are all known from the Lower Chalk
of other districts. Two, Ostrea vesicularis and O. acutirostris, have
not been discovered below the Chalk.

Around West Dereham numerous trial-holes have lately been
made to prove the Coprolite Bed, and most of these were still open
while the Survey was in progress. Unfortunately, none of them
show more than from two to four feet of the overlying Marl, nor do
the old works appear to have exposed any deeper section. Hvery-
where Belemnites attenuatus, B. ultimus, and B. minimus ?, are abundant,
and associated with them is often found the phosphatized Ammonites
interruptus.

98 MM. Reid & Sharman—On the so-called “ Gault” in Norfolk. .

To obtain the fossils of the Marl unmixed with derivative forms,
an old pit at Muzzle, about a mile W.N.W. of West Dereham, was
searched. This locality has been mentioned by several writers as
showing a typical exposure of Gault, and it is interesting to find
that not a single characteristic Gault form occurred, but that there
were several species which have not been recorded from below the
Lower Chalk.

The section, which is very good, though the pit is now seldom
worked, shows a nearly vertical face of obscurely bedded blue marl
with small black phosphatic concretions. Belemnites are scattered
promiscuously throughout. Several years ago a trial was made in
this pit for the ‘Coprolite Bed,’ and it was reached three feet below
the floor; but only a few nodules were found, and the bed was too
thin to work. This section, therefore, is an upward continuation of the
one at the new Coprolite Works, but the lower three feet of Marl being
unworked, there is no complication from derived fossils. The
following species were obtained, but no doubt longer search would
soon add to the number :—

Pentacrinus, 2 sp. Plicatula, sp.
Pseudodiadema, sp. Inoceramus, sp.
Serpula, sp. Ammonites (fragment).

Belmnites attenuatus, Sow.
Kingena lima, Detr. —— minimus? List.
Terebratulina gracilis, Schlot. — _ ultimus, D’ Orb.

sp.
Ostrea vesicularis, Lam.

All of these occur in the Chalk or Chalk Marl, and the same three
Belemnites are found in the Red Chalk of Hunstanton, which has
lately been shown probably to belong to the Lower Chalk.1 Thus it
seems that the so-called Gault of West Dereham all really belongs to
the Chalk Marl, and in this part of Norfolk the Gault is only
represented by its derivative fossils in the basement bed of the
Chalk. This greatly simplifies the geology, as, instead of two
unconformities close together, there is only one, the Chalk Marl
having cut through the Gault, and having cut also a considerable
depth into the underlying Neocomian.

There is a long dip-slope near West Dereham, which keeps the
Coprolite Bed. conveniently near the surface over more than a
square mile. But the uncertainty of the dip renders it very difficult
to estimate the thickness of the Chalk Marl, which may be only
20 feet or over 50 feet. Unfortunately, the bed can only be traced
for a short distance. East of the Fenland it first rises above the
marsh-level at Wretton, and extends about three miles to the
north-west, to Crimplesham, with an outlier capping the hill
at Muzzle.

At Crimplesham it is lost beneath the Boulder-clay for about
three miles, but reappears south of Shouldham as a bluish marly
Clay full of Belemnites attenuatus, B. minimus? and Plicatula. In

1 See Whitaker, Presidential Address to the Norwich Geol. Soc. 1882, Proc. Nor.
Geol. Soc. vol. i. pp. 207-236.

Fish vertebra.

H. E. Quilter—The Lower Inas of Leicestershire. 59

lithological character and fossils it is exactly like the Marl of West
Dereham, but the Coprolite Bed, though searched for, could not be
found. Only one section, in a deep ditch, could be examined; but
the width of the outcrop shows that the Marl cannot be much less
than 20 feet in thickness, though apparently thinner than at West
Dereham.

TV.—Tae Lower Lias or LeEIcESTERSHIRE.
By H. EH. Quitter.

HE Lower Lias in Leicestershire commences with clays and
limestones (Strensham Series), succeeded by clays and shales.

In its paleontological characters, as well as in its petrological
features, it agrees in the main with the Lias of contiguous districts.

The following life-zones are apparently represented, viz. zones
of Ammonites planorbis, angulatus, Bucklandi, semicostatus, oxynotus,
armatus, Jamesoni and capricornus.

The junction of the Rhetic beds and the Lower Lias may be seen
at Wigston, near Leicester; this section has been fully described.’
In the clay-pits at this place may be seen, resting upon Rheetic
shales, about 9 feet of limestones and shales, containing a Liassic
fauna.

A boring for Coal in 1883 at Crown Hill, near Leicester, after
passing through Lower Lias limestones and shales, penetrated 26 ft.
of Rheetic shales before reaching the Keuper.

Nowhere in the county, so far as I am at present aware, is the
true relationship between the Lower and Middle Lias clays shown.
The paleontological evidence of other exposures, however, favours the
view adopted by the Geological Survey,” that the uppermost beds of
the Lower Lias are those of the zone of Am. capricornus.?

Zone of A. planorbis.

The limestones and clays of this zone (the Fish, Insect, and
Reptilian beds) are well exposed at Barrow-on-Soar, where they are
shown to a thickness of 25 feet. The 9 feet of limestone and shales
resting upon Rheetics at Wigston are the lowest portion of this
zone.

(?) Zone of A. angulatus.

A bed of pyritous shale, nearly 18 feet thick, containing 9.
catenatum, overlying the beds of the Planorbis zone at Barrow-on-
Soar, has been referred to as the representative of the zone of
A. angulatus. The railway cutting on the Uppingham Road, near
Leicester, exposed about 12 feet of blue pyritous shale, also con-
taining Afg. catenatum.

Three or four feet of blue clays exposed in brickyards at Bottes-
ford are supposed to belong to this zone. With this exception,
there does not appear to be any exposure of the beds of this zone.
The position of the thick pyritous clays will be referred to in
general conclusions.

1 Grou. Maa. Sept. 1884, p. 415.

2 Mem. Geol. Survey. Geol. of Rutland, etc. J. W. Judd.
3 This Ammonite was formerly considered to mark the Mcddle Lias (but see p. 86).

60 H. E. Quilter—The Lower Lias of Leicestershire.

Zone of A. Bucklandi.

The beds of limestone and clay belonging to this zone are well
exposed in the district. The chief sections being at Crown Hill.
near Leicester, where nearly 50 feet of limestone and clay are ex-
posed, and at Kilby Bridge, where about 36 feet of the same were
shown. Exposures of a higher series of beds in this zone are given
in a brickyard by the canal side, near Great Glenn Railway Station,
showing 14 feet of dark-blue pyritous shales, with limestone nodules,
full of fossils. At the time of writing, brickyards at Fleckney show
from three to four feet of these clays.

During the excavations for the Great Northern Railway from
Leicester to Tilton, about 12 feet of blue pyritous clays were cut
through at the entrance of Ingarsby Tunnel.

Zone of A. semicostatus.

This zone is not now so well exposed in the Vale of Belvoir as
during the Geol. Survey in 1874. When fully exposed, it was seen
to be a thick hard band of ferruginous limestone. It is fossiliferous,
but the present scarcity of exposures prevents any investigation.

Prof. J. W. Judd, F.R.S., in his Memoir gives a list of fossils.

Zone of A. oxynotus.

The shales of this zone could formerly be examined remarkably
well at a tunnel between Grimston and Old Dalby, on the Notts and
Melton Branch Railway. ‘The section is now unfortunately covered
up, but the heaps of débris on the top of the tunnel show thinly
laminated blue shales, with ferruginous and limestone nodules, and
shelly bands of limestone. The shales when weathered are, in
places, richly fossiliferous, and judging from their present position
on the shale heaps, there would appear to be a regular disposition of
the fossils in bands or levels in the section, species of fossils being
confined to one place or heap in the deébris.

These shales with characteristic fossils are also exposed in a
brickyard between Houghton and Billesdon. The section there
shows about six feet of blue laminated shales, with pyritous bands,
and scattered ironstone nodules, which are more numerous towards
the top of the section.

Zone of A. armatus,

The beds of this zone are well exposed at Loseby brickyard and in
the railway cuttings at Loseby Station.

The sections at both localities show about 26 feet of blue laminated
shales, with numerous ironstone nodules, and a sandy indurated
rock-bed about one foot thick near the base. —

A similar section showing about 20 feet of shales with limestone
and ironstone nodules, which appear to be in beds of this zone, is
exposed at Loseby brickyard.

Zone of A. Jamesoni.

So far as I am aware, there are no good exposures of the beds of
dark blue clays with septaria of this zone. They appear to be
exposed in the brickyard at Woolsthorpe. During drainage opera-

HH. E. Quilter—The Lower Lias of Leicestershire. 61

tions near Woolsthorpe (August, 1884), about three feet of these
clays were shown. Prof. Judd mentions exposures in the banks of
the River Hye.

Zone of A. capricornus.

The beds of this zone were well exposed in a field dug for ballast
during the recent alterations in the railway near Market Harborough.
Six feet of blue shales with abundance of hard limestone nodules
containing fossils were shown. Above these were seven feet of
thickly laminated blue pyritous shales, containing ironstone nodules,
and quite unfossiliferous. A small section of these latter beds is to
be seen in a brickyard at the foot of the hill near Meville Holt.

TABLE OF FOSSILS.
SHOWING THEIR RANGE THROUGH THE ZONES.

ZONE OF
SPECIES. SS Ss PSs ys
a/s]|/a]e)]8}s 8] 8s
Sib St iiss hs SSS
Plesiosaurus megacephalus.........ccccececeees Keyl ee 50. || coo. [}4000) |} 0
Ichthyosaurus communis, ConyD..........--. px : co |) ca0 |) ‘c00.-}), ce
tenuirostris, ConyD........-+..+++ XG) | Precerl|l aes serillseek eal lee
— intermedius, Conyb........2. eee 2 N-506 || a5 || coo |) cco |] cc
platyodon, Conyb...........+2+0.+ Bpeldrset lus || see ws :
QSAUEIAM REMAINS) he. .enece vos serects ee etsoes 2 | G00 |] 25 || doc bo Pee
IDG ROHOUS ORBIB. oo8c0ces5c00680000000000000000080 22 VE So0||~ aco.) poet |e Ba Of 6
Belonostomus acutus, AGAass. ...........00.0.+s aXe | otto see
Pholidophorus Hastingsi@........c.cceceeceees 26-1) o0a. ||, 000 : cao || 0
SHTPUGHETOWO) — cossodocascccaqDeK000056 x : c0.8|Kiaae 900
SEGETLON thea sarees shade tomes oases: 3€ | G60. |! ado. ||| e600 |! d00- i} cao: |} G00 |} coo
LLeptolepis sprattiformis (?) ......c.ce.eceeees Kern lh coarcyel [ae yf eae [te ae
(Bishipre mains) eens. ..8-.ck Secs cee tenecensenss 3€ |] c50 |} 440 |) 000) |} ‘06: |) c09. |] 60
Aigoceras planorbis, SOW.........0.0..0c0eeees %& |} ooo |I 00" || c00 |} «doo. || coo |] “G00
Johnstont, SOW. ....0cecce--0-0--- Ben We peered | ace acre call eae be
GOGH, IDYORDs50n00002000000000000 Rep i|parcon ile seem (Maat caeee lees |tieee
CULENATUN ES OWeu acneeeecen eee meal Ba alll Ser Soi Hiecokal lesan mcs
angulatum, Schloth................ poerllvesse wife kee IN EERE : es
Charmassei, D’ Orb............+06+ see lPivaaien || oe 50
polymorphum, Quenst. .........++5 Ree (reel emo) iar reve | reall Werceya | oss :
FaMesont, SOW.......0.2.0+esse000: erep lisa exe lh eatetsne | ate tl exe ee Pas :
FUMIO, TSIOWo coocsosn096t00000000 B00) |) G00 || Sao | ecoosl hae coo |} ce
Volt, DY OAs sooooscesceoobonec ae |Pesne\Peseare | see [ag ae
Hentleyt, SOW. co. ceseesescensnoees 606 |} o00 || acc ax : x
curvicornum, Schloth. ............ 600 I}! coc |} coc xe illeecee Ite :
QUMACUM,| SOW aeseseseneescaccsees se C Cit lactate. oases yl Wee: S: ol feeies bales
—— striatum, Rencke ................0 Om |iesoced Hacocial Wisco aul (ae Sul bine
brevispinum, SOW. ......sceceeees : Sul ecooul cc 5 es
capricornum, Schloth. ............ sevilla cenlineata ce Rete hee “ x
—— gagateum, Y. & By w...ececccc ees eal het hae ‘ Aon sie: <
Arietites Bucklandi, SOW.....c..-0..seeeeeees cdl] 25° 1N), cos. |) cas S00
Sauzeanus, V)’Orb......-.......-.-. x Shlipere F3
GUESUIUS DIAKC semenasneneneeeeee te: ol) ogo || 2 Sal) 06 500
Conybeart, SOW. ..c.ce.c. ccecee 4 xe : Ae ‘
seypionianus, D’OrD..........06000 coo. |) 28. || cae 50 ||"Ra0 2
—— semicostatus, Y. & By vecccccseces Con ||ees.1\) 2 a flecco: tooo" || eoe
—— ophioides, D’ Orb, .........cecseevee waar Meagan |rertato lb ase ee :

62 H, E. Quilter—The Lower Lias of Leicestershire.

' 1 iy {oak ' ' i u
= = re RWS SS & - | & ‘=
SPECIES. Sg] Ss|Ss]/ SF] So] Ss) se] 8s
SS | eS] E8/58/ 53) =) SE] Sz
STEVES SHS | oe) es | USS tele
a) = oo “3 a s . 25
XN NX N SSIES! N NX XN

Amaltheus oxynotus, QUEN. ...........0s0000 care ARE UG Ee NS SHINES, OnE ks
Phylkoceras Loscombi, SOW. ......2..eseeceees Fee Bill. Shh Ws ceed || Sere ot || PERS eal) ONG || eee eres
Lytoceras fimbriatum, SOW. .........ecee0ee- nce ||| dane tcco, |Ihcooe lh boa. 1 ode, |) coo i 28
(Ammonites latecosta, SOW.) ........0ec000- 000 |} c008 | 000: Hco0.|] 665 I} asa [1-38 |} con
( Normanianus, Sow.) .......000.+ Sooul le eeomnl Nese a cecal Meee terse hy eee lade
INCRTCOUDES ECOCO ES, (SION inaadonssnc500snG0De50000 2565 | ocmniiieeS abe cbotulllasamalllemeon (hamoo. If) aac
truncatus, SOW.......0.0..0: Ricca Kod. || mono Maccm lscoolalinsa, (lle, Il seo: ||) aos
Ties infundibulum, Ph. ........0.c000 Pod lereetie) |) 2 Cil MMHeni eal esa Se, ee
HEDIS, MUN, .osc9s00Ge00050000000000 Bel |isser || exe) | askomnl ABA WTR ra
-——— elegans, SIMS ae kis Se coo |} cea Hh doo. Hf cou. | 28 |} G90 |} G05. |} one
clavatus, Blainy. ............. Seer etccen| Waiccacie oer MET a (Ree AP Sica ese | p26
Dentalium, sp. ......-.0-2- 0008 Re aecessoorsctes ooo || coo || 38 500
Cryptenia one ina, Tate. . ae cece ner salimeeenllseeeu lives x soll
expansa, SOW. ..0.0. sesees Sosgsee Bie [i eet restate CN oR il” gecer | loses 4 eRe
Pleurotomaria anglica, SOW. ...cccreseceees aR netaters| aK gh aes) es
Vecacontan WOsly easchesuacssieeec ti ieee |i teeeull| sete | hieS. al peace l eee beetctaat| toes
OTL CCDS NG ROE ALD irae sects ae eeoll ase te'en ll ee cll eK eee | earl eerste
Trochus Thetis (?), Miinst. ..... ... eponooreel|, coo "| scoo laos [leas Ih 28 P aaah Gooul ece
ee SOW scclsnacneccwaveess sista ill eisoual lt restos eeESulll bared lereat| tess

ccna ce rece eee cecrerseecce sere: coccee| cee see eee x aoo we 500 506

Hucyclus CHa D’ Orb. feteeaiceee Sara eoecie Reece esace ticcel A) eS h odes leeasel| cod
—_— rs VWelits (@) decanoaeccaall 600 |).000, |} 006 |] coo |} 88 Pcao |} doo | oon
conspersus, Tate ........0-2-+0+. Aa ecievnllyastve all | Sa7ely ll (acoteveatl sea serene | ste
elegans, Miimst............0.0-+ «- pests Peeee. pee || east ull ater ( KS [oper

Monro hy FIVe coobenooacoascnesoesqc0ORDNGeCnKs 50571) coo. Ih Goo x
Cenitfiumyiassicum,, MOOLe)teccseces-secesees| eee) |) es) ||) eee) ||eenl eX Aaa Mae
Marios. NUO OTE) cates cece taveceselinees) lt kes aill| Gee etal ise ot MPS meter |e sellin

x

x

CS PAH, WOO s5eno55ocsna5oco.|| cee |) 000 |) c6a || cos
Dee MAC sav sche saneltenescereeneaists|\isess\l(neesodcess allt toss
ligaturalis, Tate ............- SCA HN eCCA |i coeme ll eccresl lee Sail Peadaalhidoos || coda! Gab
subfistulosd, Tate .......e.ceceeeee- 200 |} a60 [ooo |} 28 |] ooo |] ose |] con | cos
Chemnitzia Blainvilled, Miimst. ............| so. | «ee | oo | «| X
semitecta (2), TUE TEN ee codsaaeseopall lana ly G56 e549 | sas fo 2s
citharella, Tate ....-0, Baosesandodebal oni oodelilaeo."|| coset ax
carusensis (?), D’ Orb. .........48. aca coos llcoo |feaca}) 38] ooo, lf, 656 || 00
x
x
x

———— = IORI, IDI Soepacecosseenooe|| co || co9 |) cos" |) coo
Acteonind, sp. ... avgooccaroadsao.oaqs00el| 06071] 000 || aso I} ode
Ostrea Liassica, Strick. aBACaC Mee ae el foctestdce BAD oN xe pan :
— Goldfusst, Bronn. ...c02-...0+s000e: Belg tlh teae: ll tested <cteeill [ose MEX [etter ate ere
CHONG CAG, ILETI, aepecansocencsaronce|| 28 || F |} x || Sef Se P58 Ht cos Il coe
OMAN Gg IUENN, epoeseecneaoeesots||) ase || coa |] o0o || cco! |] oo |] con {P28 Ml cco
OBMGUALA ISOM, jasssokscnasiescseslese|iisseu \llscns || Messe ite eseie lee era | Weseial|peeconllirots
Macullochi, SOW. ...cc.cccoccoess+- a ET Ea SOEs coors tena fects al ere lies
JEG O (RU MCT FOn INCE? oocoosonreecooononenl| 28 || ccc |} 28) |) cos |} aos |} d05 | ced |] 0c
= HATES, SXOUIDUN Ssosqsinctcosocce| 046 |) ooo Iledoe |} 28 |) coo Hose Wh Goo || coo
COP IGENBOS, (SKONifo ooesocnaecoceonsse| ec | apo || coo || 2% 1/28 | cae Ih coo |! coo
LUCIO, INVISIS Sodsdonco990c0003 | 000 |} ona | aod || 26 lo o50 |} con I} oda |} G00
Lima succincta, Schloth. ...,..ceccccesrec-es | X ae abil eee

FCT IATA OlUZ 2 Ailesescesteecmaee te, || excl || vecoudlltetces .|| eet |eXo | paeXoan bate

x

exe

Giganted, SOW. .scosc.essovnnrernes:
pectenoides, SOW. sescesesser:ernee-
punctata, SOW. .....0..- anotononsnoe Sool eoaonl loca, lh e2S0 foaa if vaso |-aga || “coo
RCULICOSTA SCUOLA =, be dene duaieesier| (rece || co sitll caenal Mise evi | Ue sein arco eta eS | ete

NEGUS DeWantieseisusiescleselssisecisieseiessseiscasarionnl|itesie) liseli Xai tess irectnhl Meal Mewes teste

H. E. Quilter—The Lower Lias

of Leicestershire.

63

SPECIES.

PUCAHUASPINOSAs SOW es sovesancocsesccescee
—_§|_— levigata, D’ Orb. (?) .......s0000
Avicula (Monotis) cygnipes, Y. & B. ......
Perna infraliassica, QUeN. ........0-e0ce0ees
Tnoceramus ventricosius, SOW. ....seseesceees
JEG RAR jolla, Sls C2 8) eoobanaeooebeeoandoLoeae
Modiola minima, SOW. ...0..2.+02+20--2-+220-
HIB, SOW cocasdoo00e Aub diseases

JEG, IXO\iFo eccdoos0000c00Gb0se0

Alara OVS aésasnacoseeec0s0
SCALPTWIN, SOWacsecsssenccoseecss-s

Nucula variabilis, Quen. ........... Bes ckawean
Leda galathea, D’Orb. ..... Oh ceceincecnisrecelsl
TOU AOIP SHEEN“ poqesooucsnoosenoGcG
complanata, Goldf. ...........6.--

Cardinia Listeri, SoW..........0.0000: steaeateed
GOGO QUE, acocqecoanensesoc

GDR IBC, Sronccesocosesocoece0

Wanita, SONS oocccoboccooacq50H0Kd

CEHES, SKINS Socooopocseaocodeda5+
Cypricardia cucculata, Mun. ........... Hi
Hippopodium ponderosum, Sow. ...... eRe
Protocardium Phillipianum, Dunk..........
Unicardiwm cardioides, Phill. ........... Bae
Pholadomya glabra, AGass. .........0.eee0e
VENtViCOSA, AZASS. .....ceeeeeereeee
CHONG, SKO\To soenooccese9s9000c3eC
GCUPGHO, VEIETE I, .sccooacscasoscou
Goniomya hybrida, Miinst. .............0000

— PleuroMmyG Strtatula ......cencseceroneceerevoes
unionides, ROM. ....s..000 tskae

—

Spiriferina Walcotti, SOW. .....c.se.00- 3a0

verrucosa, V. Buch........cesse0s:
Terebratula punctata (2), SOW. .sssecseace
Waldheimia numismalis, Liam. ........0+-
——— perforata, Piette ........... Mest
Rhynchonella plicatissima, Quen. .........
tetrahedra, SOW. ....s..0e.20c000-
variabilis, Schloth. ........ fhe
Buprestis (Elytron of), Brodie ...........+4.-
Libellula (Wing of), Brodie ............000+
Eryon Barroviensis, M‘Coy .....+....see0e0e

Jo caeesadanoododeso Seadoo 200000006

(Crustacean remains) ........s00sce-secseereees
Serpula capitata, Phill.............. ScnneoOCes
(SDECIESION) ieocnanseneneenarearscmes
Cidaris Edwardsii, Wirt. ....cccccsec-cccceee-
Hemipedina Tomesii, Wrt. .....0-2-0cecsres:
Pentacrinus psilonoti, QUED. ......2.e0e000-
—— punctiferus, QUED. .scecerercorese
MODUSTUS sy Nits) saeseaseeanee es Le
Montlivaltia Guettardi, Blain. ..... ....0..+
mucronata, Dune.......... eesiesscet
Lepidophyllia Hebridensis, Dune. .........

N
°
A
|
°
ry

a. | Sea Sosa Shale
22/5] §=| 88/88) Fe] Ss
SESS | S| SCS Se1ss
SiS Iss!s jx ix [Se
eee aXe cae x x x
oo eee coe oe x 5
900 Xs 000 500 wae
one x Hop aie nels
Os0 seevul| WRX Xe 4
see x 600 000 nae ue
6G d.€ x oe eee 660
500 p00 x OO tate ete este
SE seas [Bac | ane-< x i Xe
eco a oe eee 5 oo x
0 O nO0 x 50 x
soe 6do x alate!
eee x aiele x 00 CO
eos 90 x 000 500
ooo eae x eo eon
60 x ee 500 5
eee eco x 900 S00
doo ete ene x COO ete
50 x coe x x 50
O00 600 fatale x aad 900
cee D8 x x x x 506
ele x 000 500 sale
oe O00 000 x G00
000 500 000 O00 x pete
ase 60 aes O00 x Ado
. 000 ee wee cos x
600 x 000 x 00
noo 600 x 550 he
co ae eee x 500
ee oe x 300 BS
soo 000 a x d:€ a
ece 000 x fae
eco Xs Ga0
a0 |IMeoa laa IP (26 “ll 560 i
5 x 0 Aan x ate
x G00 x x 008
50 00 904 x cn 50
x 660 500 G0
ial x O DOO
see anc: D6 ate
oe x ay b.§ x 3.¢
Spall) a ? sata tees
eee x aoe oe
ase n'y) 2:¢ Bete
O50 GeI0 ciate x
x aS and
een aiela x aso
sfete pale x cae) ee ann me

64 HT, E. Quilter—The Lower Lias of Leicestershire.

Mr. HE. Wilson, F.G.S., who has rendered me great assistance in the
above list, also informs me that he detected Foraminifera in several
of the Lower Lias clays of the district; in particular from the 4.
oxynotus shales at the Tunnel near to Old Dalby Station, from
whence he has obtained no less than thirty forms, the following
genera being represented :—

Nonionina. Planularia. Nodosaria.

Frondicularia. Textularia. Marginulina.

Involutina. Dentalina. Cornuspira.

Lingulina. Cristellaria. Miliola.

Pulvinulina. Orbulina.

General Conclusions.

Considering the few and comparatively unimportant exposures of
these rocks in Leicestershire, and the consequent difficulty of ob-
taining a complete series of fossils, a classification of the beds into
life-zones would seem hardly feasible. Sufficient has been done,
however, to make the case good. Nevertheless, it would be prema-
ture at present to make any deductions with regard to the passage
of important species from one zone to another.

The apparent non-development of the zone of A. angulatus, and
the intercalation of the zone of A. semicostatus, with the zones of A.
Bucklandi and A. oxynotus, may perhaps be made the subject of
remark. That the beds of the zone of A. angulatus are present is
highly probable.

Mr. J. D. Paul, F.G.S., informs me that 186 feet of Lower Lias
limestones and clay were passed through in the boring at Crown
Hill, near Leicester. Deducting from this,” say 40 feet, for the
maximum thickness of the beds belonging to the zone of A. planorbis,
and 60 feet for the thickness of the lower beds of the zone
of A. Bucklandi, which are, as already mentioned, exposed here,
about 86 feet of the beds passed through in the boring remain to be
accounted for.

As bearing on this point, I would here note the similarity of the
sections at Kilby Bridge and Crown Hill, and the occurrence of Ay.
angulatus in the lower beds of these exposures, showing that these
beds are not far from the junction of the zones of A. angulatus and
A. Bucklandi.

The 86 feet, or thereabouts, remaining to be accounted for, may
reasonably be assigned to the zone of A. angulatus. The thick bed
of clay exposed at Barrow-on-Soar, and in the railway cutting on
the Uppingham Road, near Leicester, has also been thought to repre-
sent the zone of A. angulatus; but if my supposition be correct, this
is not so.

The fauna of this bed is so scanty, containing only “g. catenatum,
Lima gigantea, and Gryphea arcuata (the two latter being dwarf
forms), that we can learn nothing from it; but the occurrence of dy.
catenatum in this bed only is peculiar and interesting. 44g. catenatum
appears to be an evolutionary form between 4%. planorbis or 4g.
Johnstoni and Aq. angulatum.

From this, I] assume this thick bed of clay to be a bed containing

C. Davison—Form of Rock-Surface under a Talus. 65

a transition fauna between the zones of A. planorbis and A. angulatus,
not so well developed perhaps in other districts.

Under these circumstances, should the zone of A. angulatus he
eventually exposed, and with more exposures, an assemblage of
fossils be found in the clays containing A%g. catenatum, then those
clays should be placed in the position of a subzone—the subzone of
A. catenatum. For the present, however, it might be termed the
“ Catenatus bed,” and separated on those grounds from the zones of
A. planorbis below and A. angulatus above.

The occurrence of the interesting zone of A. semicostatus is an
example of the fluctuations of the zones of the Lias formation in
districts or areas, and how species perhaps only of secondary import-
ance in one zone, under certain conditions of environment may be
of capital importance in another.

I have to acknowledge the assistance of Prof. Blake, of Notting-
ham, who has kindly determined many of the fossils for me, and also
that of Mr. H. F. Bates, of Leicester.

V.—Nore on tHE Form or tHE UNERODED SuRFACE OF Rock
UNDERNEATH A 'T'ALUS.

By Cuartes Davison, M.A. ;
Mathematical Master at King Edward’s School, Birmingham.

N the case of a vertical cliff, Mr. Fisher has shown that the
uneroded surface of rock underneath a talus is in the form of
a semi-parabola.’ The object of this note is to show that the form
is parabolic, even if the cliff be not initially vertical, assuming, with
Mr. Fisher, (1) that the cliff-face is weathered uniformly at all
points, and (2) that the disintegrated material is spread evenly over
the surface of the talus, so as to maintain it always at the same
slope. The proposition may be proved analytically, as in Mr.
Fisher’s paper, or geometrically as follows.

Bie te g

- See Halted ‘
D oC, A, lV

1 Rey. O. Fisher, ‘‘ On the Disintegration of a Chalk Cliff,” Guon. Mac. (1866),
Vol. III. pp. 354-356.
DECADE III.—VOL. III.—NO. II. 5

66 C. Davison—Form of Rock-Surface under a Talus.

Let AB, the original face of the cliff, be inclined at an angle
a to the horizon. In any given interval of time, suppose the layer
A Bf,a, to be worn from the face of the cliff, and the material
spread at the foot of the cliff as a,b, ¢, the surface b,c, being plane
and inclined to the horizon at an angle ®. Let A B=h, Aa=a,
ay b= 5

Now, the parallelogram A Bf,a, is equal to a rectangle whose
base is Aa, and height h sin a,

.. area A Bf, a,=hx,.sin a,
and triangle a, b; c;=4 a, ¢, a, 6). sin a,

ae onl song
sin (a—B) sin a.
t sine sin 8

During a second interval, equal to the first, let another layer of
the same thickness be worn from the face of the cliff b, f{, and be
deposited over the débris at the base, and inclined at the same angle
B to the horizon, so as to raise the surface of the talus to b,c. Let
a, b,=y,, and Aa,—a7,—2m,.

Now, area f, b, b, f-=(h—yi) %1.8in a,
and area ¢ ¢, b, b; =a, b, ¢,—a, b; ¢,—a, by by a,
sin (a—f) sina _, _, sin (a—) sina

=F y+ aa ® x Yi - Go —y,%, Sin a
ay ed) (a— B)_,, ee _sin (= —P) 9 hase
sin B sin B
eh en Bp ae sin 8
ee "sin (a—B) " sin aay

Proceeding in this way, we see that after nm layers have been
worn away, we have
es 5} ih _ sin ae
sin (a—f)
Now, let each interval of time be supposed very small; then the
layer disintegrated during each interval is very thin, and the form
of the rock under the talus is a curve which has the property

PNe2 = in,
sin (a—)
and is therefore part of a parabola whose axis is horizontal. The
initial face of the cliff is a tangent to the curve at A, and the final
surface of the talus, when it reaches the top of the cliff at Q, is
a tangent to the curve at that point.

Lye

A. Bell—Succession of the Later Tertiaries in Gt. Britain. 67

ViI.—Tue Succession oF THE LATER TERTIARIES IN GREAT BRITAIN.
By ALFRED BELL.

HOSE interested in the geology of the Upper Tertiaries must
have noticed the divergence in the views entertained by different
writers as to the succession of the various strata of which they are
composed. Sundry causes may be assigned for this, such as the
disposition in some quarters to regard the “lapse of time occupied in
the accumulation of even our later Tertiary deposits” “as repre-
senting but a very brief chapter in geological history,”* or the
massing of the several groups of strata in bulk, or putting aside as
of little value the organic evidence they contain, which, even where
this is appealed to, is too narrowly treated, as where one author—
a specialist in bis own branch —asks, ‘Could the more modern
Tertiaries be classed by their Invertebrata?”

Not alone perhaps; but if all kinds of life are studied in corre-
spondence with their surroundings, a natural sequence can be traced
throughout their entire history.

Astronomical speculations as to the time when the Glacial epoch
commenced or terminated, and the attempts thereby to determine
the existence of Man upon the Earth, may be set aside as of little
value at present; as Mr. Prestwich happily puts it, “the difficulties
arising from astronomical theories are that they differ so much among
themselves.”’?

A fair inference as to the time required may be drawn from the
fossils. My lists give of the Hocene about 2500, and of the later
Tertiaries above 3000 species, hardly any being in common.

In the following notes I have assumed that the constituents of the
different deposits and their fossils are pretty well known to geologists,
and I have therefore not attempted to locate every known bed, but to
indicate the lines on which their classification is possible. A com-
parison betwixt that which I have here attempted and that adopted
by Mr. J. Geikie will, I may say at once, indicate how widely
divergent our respective views are. I take his as a standard of com-
parison as being the most extensive one brought forward hitherto.

I am probably biassed, but I cannot see any evidence in favour
either of the numerous mutations of the surface, or alternate pro-
cession of the Northern and Southern Mammalia suggested in the
“Great Ice Age,” or that Britain was ever otherwise than Continental
from the close of the Middle Red Crag age to that of the minor
glaciation, about which time I consider it ceased to be so.

It may be laid down as a general rule that the fauna and flora
march with the climate, i.e. cold with cold or the contrary, and that
if by any possibility the temperature of any period can be ascertained,
a corresponding organic life existed, circumstances being favourable
thereto.

Of the preglacial deposits the admirable memoirs by Messrs.
Clement Reid and E. IT. Newton leave little to be said. I may,
however, remark that the evidence of the Forest Bed being overlapped

1 Dr. H. Woodward, On Rhytina gigas.
* Quart. Journ. Geol. Soc. vol. xxvul. p. 233.

68 A. Bell—Succession of the Later Tertiaries in Gt. Britain.

by the Bure Valley Beds is not so satisfactory as might be desired.
Iam more disposed to agree with Mr. H. B. Woodward in placing
these marine beds on the same level as the Weybourne Sands, and as
constituting the very upper part of the newer Pliocenes, since I find
that, with the exception of Tellina balthica,} all the mollusca of these
beds are found in the Butley Crags.

The Quaternary, if not a very sound division of the Tertiary,
is at least a very convenient one, and it is with the ‘Forest Bed”
rather than the preceding Passage beds that it may be said to com-
mence.

Mr. H. B. Woodward takes the view that the lapse of time between
the Newer Crag and the Forest Bed may be inconsiderable ; but
there is not only the disappearance of the Mastodon to be accounted
for, but the variation in the Mammalia as a whole; since, leaving
out nine species in the Norwich Crags still existing, only four pass
up to the Forest-bed, where at least 40 others occur for the first
time. (Is there any confirmatory evidence of the existence of
Mastodon in the later Thames gravel as recorded by Mr. Whitaker ?
Mem. Geol. Survey.)

The fluviatile mollusca, except for Lithoglyphus,? does not offer
much for comment. The splitting up of the very minute Hydrobia
by Sandberger into so many new species and a new genus will not
commend itself to Conchologists generally.

Will Mr. Reid allow me to set one of his quotations right? I am
represented as saying (Mem. Country around Cromer, p. 74) that
Mr. Prestwich’s Unio margaritifera in reality is Unio littoralis. If
he will turn to the Gron. Mac. Vol. IX. 1872, p. 214, he will find
I said nothing of the kind, but that it was an Anodon, as he himself
assigns it. The specimen referred to is in the Norwich Museum.
Again, on what grounds does he transfer the Limax agrestis of my
Forest Bed list to L. modioliformis? The Forest Bed Mollusca I
collected myself. Silpha dispar may be also added to the Coleoptera.

Inasmuch as Mr. Newton has rehabilitated in the Forest Bed
Hyena spelea after having once rejected it, I hope he will be able
also to replace the other species he has excised from the Forest Bed
list compiled by my brother and myself.

Between the temperate Forest Bed flora and the intensely Arctic
one above it the measure of time must be a long one to allow for
physical changes, as the Forest Bed must have been submerged at
least six or eight fathoms, that being the average depth at which the
Yoldias found in situ in the intervening beds inhabit our modern
seas, the Yoldia or Leda myalis beds being here 15 feet thick.

One of the chief objections to the Myalis bed being synchronous
with the Bure Valley Beds is the fact that several of the species, Leda

* The presence of this shell seems to indicate that great hydrographical changes
had taken place, probably the influx of a heavy current setting in from the north,
bringing the Tellen in profusion. It sufficiently distinguishes the beds in which it
occurs from the immediately preceding Upper Crag or the Chillesford Series.

* This is the recent species figured in Forbes and Hanley’s British Mollusca as
Natica Kingi, obtained in the rubbish of a fishing boat at Cullercoats.

A. Bell—Succession of the Later Tertiaries in Gt. Britain. 69

included, are found in their living position. It may be also worth
noting that the Leda myalis does not occur in the inland Bure Valley
Beds or the Weybourne Crags, where L. oblongoides (L. limatula) is the
representative species, and of the 18 Bure Valley marine species,
eight do not occur in the Myalis Bed; and of the 15 species in the
latter, nine are not found in the Bure Valley.

T may call Mr. Reid’s attention to a very valuable paper by Dr.
Nathorst, on this Arctic plant-bed, in vol. iii. of the Journal
of Botany, London, which Mr. Reid seems to have overlooked (op. cit.
p- 83), in which the Doctor records the species he obtained, including
a large number of Willows and Mosses now living only within the
Arctic circle.

It is generally assumed that a great elevation of the land was
taking place throughout the earlier part of the major glaciation,
culminating in a rise to at least the 100-fathom line, raising the
whole bed of the North Sea, except a narrow valley towards the
Norway coast—the ice-sheet then generated not extending to the
South of Britain. Of the land or sea life of this period there is no
record in Britain, but it may be surmised that the Mammoth and
Rhinoceros tichorhinus, the Wolverine and the Musk Sheep roamed the
frozen solitudes in scanty numbers. That which would be most con-
sonant with the climate is found in the masses transported bodily from
some unknown deep-sea locality, imbedded in the higher Yorkshire
Clays at Bridlington and elsewhere (vide infra), the few fragments
mentioned by Mr. Reid from the Cromer Drift being doubtfully
m situ.

Subsidence of the land is indicated by the erosion prior to the
deposition of the wide-spread sheets of Middle Glacial sand and
gravel extending from Shropshire to Belgium (if, as Mr. 8. V. Wood
suggested, the Sables de Campine are of this age). ‘These sands are
mainly, and I am inclined to think altogether, unfossiliferous. The
very fragmentary condition of the large number of species (94)
recorded by Mr. Wood from these sands, and the fact that except
six or seven all are present in the Butley Crag, induce me to think,
contrary to the opinion of the Messrs. Wood and Harmer, that, like
the corresponding sands of Slains and Cruden, containing frag-
mentary Red Crag shells, they are purely derivative.’ It is also
difficult to see where such a fauna could have existed in continuity
throughout the preceding stages, if the bed of the North Sea had
been elevated to the extent supposed. These sands and gravels are
apparently due to the fluods let loose by the melting ice, excessive
rainfall, and the sorting action of the sea as a greater area was
brought under its influence while the land slowly subsided. The
immense influx of freshwater would be unfavourable to the develop-
ment of marine life which in the Anglo-Belgian Gulf had ceased to
exist, the incoming northern fauna being unmodified by southern
accretions till the future minor glaciation had passed away, and the
communication re-opened between the Channel and the North Sea.

1 Traces of Red Crag Shells, Pecten opercularis, have also been found in the
westerly extension of the Middle Glacial,

70 A. Beli—Succession of the Later Tertiaries in Gt. Britain.

On the western side of Britain a different set of conditions
obtains in the beds beneath the Till in Kilmaurs, Tangy-Glen, and
elsewhere. Of the 22 species recorded, 17 are still British; but the
remaining five are extra-British, new to the fauna, and of true
northern types corresponding to those on the east coast of Brid-
lington and Fife, as will be discussed presently.

The climax of the Glacial epoch occurs with the Great Chalky
Boulder-clay, the true Scottish Till, the drift and unfossiliferous
Till of the Midlands and north-west from Lancashire to Shropshire.
From the presence of occasional horns, bones, and teeth in the
Scottish clays, the remission at times of the intense cold may be
inferred, as in the Greenland summer. I have no knowledge of the
Crofthead Peat, except from the kindness of Mr. Mahoney, and his
and Mr. Geikie’s papers in the Guox. Mac. Vol. II. 1869; but, con-
sidering all the evidence, I am less inclined to regard it as an
intercalated deposit in the Lower Till than as occupying a depression
at its immediate close, the overlying drifts corresponding more to
the higher English Purple Clays than to true Till. The fauna and
fiora, including Bos primigenius, are certainly not Arctic, as they
should be if Greenlandic conditions prevailed.

The Purple Clays of Yorkshire and Lincolnshire mark the
close of the first Glacial epoch in Britain. The researches of
Mr. Lamplugh have definitely settled the question as to the fauna
of the intercalated masses of sand and clay in the basement
beds not being in position. Of the 120 molluscs on record from
Bridlington,' I find on analysis that 89 are confined to these sands,
and of the others, 22 are now extra-British, all of the species being
still existing. The age when these molluscs lived would probably
be about the time when the Arctic plant-bed was forming on the now
Norfolk coast, the Nucula Cobboldie and Tellina obliqua linking it to
the Newer Pliocene fauna, their habitat in the deep North Sea not
far removed from shore—a few miles perhaps—similar to the Dogger
and Antrim turbot banks, where northern forms still exist. Mr.
Dawson records a similar deposit about eight miles off Cruden, from
whence his dredge always brought up dead shells of northern types ;
of the seventeen species recorded, nearly all are found at Bridlington,
and like deposits are not uncommon elsewhere. The Bridlington
fauna is essentially a deep-sea one, and in no case could have
originated or formed in any of the deposits of the Glacial epoch in
Britain.

With the gradual cessation of Arctic conditions, depression began
again, lasting until the waves of the Atlantic washed the shores of
a coast-line extending in an irregular tract from the Severn to the
Tees, accompanied by excessive thermal changes and the inbringing
of a new series of life forms. Eliminating all the Bridlington
species as of doubtful British origin, and all land and freshwater
mollusea on either side from the list of species before and after the
major glaciation treated of above, there remain of the Newer

1 Dr. Jeffreys in working up the list of species in Mr. Lamplugh’s paper omitted
any reference to Mr. 8S. V. Wood’s, and many other notices on the fauna.

A. Bell—Succession of the Later Tertiaries in Gt. Britain. 71

Pliocene (Butley horizon’) 130 species which do not pass the
barrier, replaced by 160 others; forty to fifty again of these dying
out on or before the succeeding minor glaciation. Mr. Crosskey points
out “that the fossiliferous sands, etc., belong to several ages, the
contents indicating several groups, having their own place in the
gradual transition from a severely arctic to a more moderate tem-
perature.” This transition I am trying to illustrate. The oldest
of the Interglacial marine deposits occur in the flanks of the Boulder-
clay in Fife and Aberdeen, and, as might be expected, yield 22 extra-
British species, of high Arctic types. After these may be grouped
such beds as those of Bute and Arran, containing Saxicava Norvegica,
and other boreal forms, without or with but a small proportion of
more Southern forms, as at Paisley and Dalmeny later on.

Unless the raised beach at Portland Bill is of this age, there is no
Marine deposit in South Britain that can be, so far as ] am aware,
correlated with this older group of Interglacial deposits; and the
Lower Boulder-clays of Lancashire and the West containing Cytherea
Chione are approximated by this shell to a slightly more recent
period antecedent to the Middle Lancashire Sands.

The land fauna of this immediate Post-glacial age in Britain is
very limited, the Mammoth, Woolly Rhinoceros, Bos primigenius,
and the Reindeer, a new arrival, alone indicating the larger life in
the north; but with the disappearance of the ice in lower lands,
immigration began. Traces of such are found in the breccia of Kent’s
Hole, and the corresponding earth of the Brixham Windmill Caves,
in the abundant relics of Cave Bear and the very rare Lion and Fox
(White Fox) (1 jaw of each) and, as shown by his implements, Man.
The presence of these four Carnivora is indicative of the herbivora,
none of which has as yet been found, and Mr. Pengelly would pro-
bably be quite right in his argument that Man arrived in Britain
before the Cave Hyena, if he had added “after the Glacial epoch.”
From all the facts of our present knowledge there seems no escape
from making the earliest Primeval Man (revealed by his works in a
Devonshire Cave, for the first time on record), an Old Devonian and
a real homo, having nothing to do with the Hocene Ape Man of
Thenay, or his Miocene brethren of the Cantal and the Tagus.’

1 T have used this horizon as a standard of comparison throughout, because of its
accepted freedom from extraneous forms ; and its richness in life offers sufficient ground
for such reference.

2 The evidence of Preglacial Man in England is confined to the Red Crag, and
consists, Ist, of a shell with a supposed human face carved thereon (H. Stopes); 2nd,
perforations in sharks’ teeth (. Charlesworth); 3rd, a human jaw deeply stained
with iron irom Foxhall (Dr. Collyer, Anthrop. Review, 1867, p. 221); 4th, a spear-
head from a Coprolite heap, locality unknown (R. J. Mortimer, now in Brit.
Mus.) ; and lastly, a specimen of apparently cut bone in possession of Prof. Prestwich
(Nature, vol. xvii. p. 105). Of these the shell is probably like many other Walton
shells fancifully decorticated ; 2nd, the perforations are shown by Prof. Hughes to
be due to animal action; 3rd, the jaw is repudiated by nearly all scientific men as of
Preglacial age, although certainly old; 4th, Mr. Mortimer’s implement has been
fashioned since the fossilization of the bone. Mr. Prestwich’s [ have not seen.
The absence of Paleolithic Mammals and Implements in either Scotland or Ireland
is strong evidence in favour of an equal absence of dry land there.

72 A. Bell—Suceession of the Later Tertiaries in Gt. Britain.

The submergence of the north-west corresponds with the emergence
or elevation of the east, and in the Glacial beds thus exposed the
Thames river channel was opened, the oldest portion from Hast
London to Ilford, Grays and Crayford, opening southwards
(S. V. Wood), and at a later period, when the North Sea was
resuming its old bed [inhuming the Mammalian fauna, brought up
so frequently from its bottom by fishermen], the present channel
in its entire length opening eastwards. These earlier gravels and
brickearths yield a fauna indicating warmer conditions than now
or at any time since the preceding glaciation. Grouped with
these must be the rich Barnwell river gravels. containing more
extra-British freshwater and land shells than all the other Post-
Tertiary deposits put together, including Helix fruticum, the
only other Post-Tertiary locality for which shell is Stutton on the
Stour, a deposit of similar age, from whence the late Mr. 8. V.
Wood, sen., obtained the specimen (the only one) figured in Mon.
Crag. Moll. I notice here this shell more particularly, because
I shall have to call attention to certain erroneous references
in respect to this species. The well-known deposit at Clacton
Cliff belongs to this series: and here I must demur to Mr. Dalton
collating the fauna at this place with that of Copford, especially
without due revision. The Copford shells were named by one of
the most competent men of his day, the late Mr. John Pickering,
from Dr. Gray’s edition of Turton’s Manual, and the Clacton list by
Mr. J. de C. Sowerby, in which two species are described as new,
one being from the figure a variety of Helix hispida, and the other,
judging from the description, a young Planorbis glaber. Mr. Sowerby
used a different nomenclature from Mr. Pickering, and the incorpora-
tion of both lists into one without the elimination of the synonymic
names unduly inflates the list of species (Memoirs of the Neighbour-
hood of Colchester, 1880).

The Worcestershire Avon gravels may be assigned to this series also,
as, like the older Thames beds, the fauna of all kinds is marked not
only by forms of southern types, but by an almost complete absence
of northern and arctic species. The Musk Sheep would seem not
to be in accordance with this view; but at present I should con-
sider its occurrence at Crayford, Erith, and Freshford near Bath, to
correlate these beds with the same age as the later Thames gravels
near Maidenhead, when the declining was gradual. The Thames
Valley is not a valley of one aspect or geologic stage, but many ;
the great river and its affluents, and the contents of the bordering
gravels and soils sufficiently attest this. Mr. Worthington G. Smith?
points out that three stages at least in the manufacture of palao-
lithic flints are traceable, ranging from the crudest to delicate tools
of beautiful fabrication.

Coincident with the river earths above referred to, is the ancient
peat of Lexden, near Colchester, where the Rev. O. Fisher obtained
so many traces of mired and mud-bound Mammals, and an Insect
fauna of trans-pyrenean growth.

1 Nature, xxvii. p. 270.

A. Bell—Succession of the Later Tertiaries in Gt. Britain. 73

The fauna of the “Mud Deposit” at Selsey, unfortunately so
seldom visible, is exceedingly rich, as is well known, in shells of this
age and character. The gravel beneath it is rich in land shells, but
so rarely viewed as to be almost unknown. As described elsewhere
by myself, I have taken from the mud bed 140 species of shells;
of these about 380 do not come north of the Channel Islands or the
north of Spain, eight being exclusively Mediterranean forms.

This extension northwards of southern types is visible very
notably in the Middle Sands of the North-West of England and
Wales, in the Shropshire and Severn gravels, etc. Undoubtedly all
these are not of one age, but belong to various periods of the great
submergence, as already indicated for the Scottish fauna. The given
fauna from these beds is rich, almost too rich, for there is a shrewd
suspicion that all the species quoted are not genuinely native, especially
when obtained from the workmen. Many quarrymen unhesitatingly
bring recent Naticas and other species, some with Confervz on them,
as the product of the soil. Mr. Darbishire, Mr. Maw, and myself
in a small way have found this, even to the offering of the pearl
oyster and other West Indian species.

Apart from this, the beds exhibit Venus Chione and other southern
shells (and in Ireland Woodia digitaria) at higher latitudes than
those they are now found living in. The finest and most instructive
series, because almost every specimen has been obtained under
the supervision of the owners of the gravel pit from whence
they were exhumed, and preserved with great care, is that in the
possession of the Misses ffarrington, of Worden, Lancashire, in
which every species known to the N.W. gravels is contained with
many others confined to this pit alone. When, by the kindness of
the Misses ffarrington, I had the pleasure of working out the entire
series, I found that from 130 to 140 species were represented, and it
was not only in the number of southern species, but the southern
exuberance of form and sculpture put on by such shells as Murex
erinaceus, still with us, that testified to the extension northward, and
the consequent indication of the southern climate that these showed.

Western currents were at times probably prevalent, since the find-
ing of a West Indian Olive (0. jaspidea apparently from Strickland’s
drawing) and Bulla ampulla’ in the Severn drift implies as much.

I can identify only two deposits in the West of Scotland with this
series—Garvel Park and Loch Gilphead, with perhaps Lochaber.
The presence of Rissoa cancellata and R. striatula (the latter only
known fossil elsewhere at Selsey), so far removed from their present
locality, is remarkable. The “head” over the Portland Beach and the
Crystalline Stalagmite above the Cave Bear breccia of Kent’s Hole
correspond to this open-air earlier deposit.

Hessie Graves, erc.—As the first portion of the Interglacial
series culminated with the deepest submergence of the North and
North-west, so the second part commences with its re-emergence.
It is understood that depression is more pertinent to accumulation than

1 Mr. Mackintosh, I think, is not very favourable to Molluscan evidence. I am
afraid he is hardly a fair judge, as he divides this species into two genera.

74 A. Bell—Succession of the Later Tertiaries in Gt. Britain.

is elevation ; hence there is little to wonder at that marine life in this
stage should be so much less active in appearance than in the preced-
ing period ; and nearly all deposits, whatever height they may occupy,
belonging to this stage, have been deposited in shallow waters.
Present elevation goes for nothing: for example, the living zone of
Saxicava Norvegica is from 30 to 90 fathoms, and of Thracia conveaa
4 to 70 fathoms, yet they occur between tide marks on the same
level on exactly opposite sides of Scotland, namely, at Bute and
the Frith of Forth.

A few of the Scotch shell clays belong to this stage, but the non-
Arctic shell-beds are chiefly of post “‘minor glacial” or Neolithic
age, certainly those in which Pecten Islandicus, Tellina calcarea, and
Astarte borealis, species still living within easy reach of our coasts
(as in Faroe and Norway), are conspicuously absent.

The Marine Gravels of March and Hunstanton below the Fen Peats,
and those of Kelsey Hill in the north, and Chislet in the south, belong
to this era, the association of Corbicula and fluviatile species with
marine forms in the two latter being very noticeable, indicating
beyond any doubt that marine conditions again prevailed in the
North Sea. The March gravels may be of a slightly earlier age,
equivalent to the Barnwell freshwater gravels; they cannot be far
away.

This epoch is the so-called paleolithic or rough stone implement
age of Man, and the prevalence of rough-shapen tools from Peter-
borough southwards, and their absence together with that of the
accompanying Mammalia in Wales, Scotland, and Ireland, affords a
fair inference that these places were under water at the time. Asa
general rule, the more advanced manufactured weapons are in the
newer deposits; but, just as Dr. Schliemann found at Troy a Bronze
people, succeeded by a Neolithic one, so inferior tools occasionally
are supra the better-class weapons. Stratigraphically they must be
received with caution.

In order of time the fauna of the Bedford Ouse and Thet valleys,
the Somerset caves, the Upper Thames gravels, and the Kirkdale
and Settle’ caves, in which Reindeer are few or absent, seem to
precede the Fisherton gravels with Marmot, and the Windsor, Rugby,
Windy Knoll, and Gower Caves in which they are more plentiful,
the Cave earth of Kent’s Hole and Cresswell Crags with bone
harpoons evidently being the most advanced of all. Professor
Prestwich’s suggestion that the Hippopotamus was fitted for a more
northern climate than it now inhabits seems to be irrefutable, since
it is found associated with remains of species widely separated from
it now in space and climate. Such separations among old associates
are common enough among the Mollusca. Taking Butley again for
an instance, of shells which in life were associated, and are now
found side by side fossil, Gastrana laminosa is Natalese, Tellina
a Japanese, Fusus altum North Cape, Admete viridula Green-
andic.

. | The supposition that the lower cave earth here is Preglacial will not bear
investigation.

A. Bell—Succession of the Later Tertiaries in Gt. Britain. 75

Much yet remains to be learnt about the migration of the
Mammalia. The Musk Sheep and Glutton in the Forest Bed again
reappeared, when a colder period was setting in again, in company
with the Northern Lynx and Arctic Fox. But Mr. Howorth has
pointed out that rain and damp are the main agents in the delimita-
tions of range of the Reindeer and Musk Sheep, the fresh skulls
of the latter occurring at lower latitudes than it now occupies.
Prof. Boyd Dawkins has so thoroughly entered into this branch of
Paleontology, that I prefer leaving such questions to him.

The Mundesley river bed may probably belong here. The Hydrobia
marginata (Belgrandia nana, Sandb.) and Elephas antiquus correlates
it to this stage, and if so the presence of the little Chelonian
Emys lutaria may place the fluviatile deposit at Wretham Mere,
Norfolk, with it. I take it that many of the caves just referred to
were inhabited, without cessation, during the following minor
glaciation, from Yorkshire southwards.

I have lately obtained from the pebble beds overlying the London
Clay close to Minster, Sheppey, a flint implement. The two pebble
or gravel beds were probably continuous originally.

The Implement gravels of Herne Bay and the South of Hamp-
shire, and the thick yellow clay with large southern erratic rock
masses overlying the Selsey mud bed, must be placed here. This
clay boulder bed is too often confused with the angular marine
gravel above. This gravel I may say helps to form the mass of
shingle on the beach, but the shingle is not composed only of this fall
or talus, but is augmented by a large accession of rolled pebbles of
all ages, travelling from the westward, a fact often lost sight of.

To this latter half of the Interglacial period I consider the Somme
and Seine gravels belong, not to the earlier Thames (Crayford) por-
tion. The tuffs of Cannstadt and of Moret in the Seine Valley will
probably give the Flora of the time.

Tue Mryor Guactation.—Such period will include the Hessle
Boulder-clay of Yorkshire, the Upper Boulder-clay of the N. West
and Ireland, and probably some of the fossiliferous beds of Scotland,
like Paisley and Kilchattan, not possessing so glacial a character as
the earlier Fife and Bute beds.

In Lancashire and Westmoreland alternations are not uncommon,
peat containing Mosses, Beetles, etc., not being very rare, the marine
fauna in the clays, as in those of the low-lying Caithness lands,
mostly being fragmentary and derivative. In the south its influence
is chiefly felt in the “trail” Loess, Brick-earth, and Contorted
Gravel in the Thames Valley Beds and Tolland’s Bay; and to this age
I am disposed to refer the raised beds on the Sheppey and Pegwell
Bay Cliffs, and the long stretch of marine detritus and gravels
extending from Brighton to Portsmouth, at all heights, from nearly
sea-level to upwards of 200 feet.

The final relics of this era are the Moraines, Eskers, and Kames,
chiefly occurring in Ireland and the North, the Lancashire Shirdley
Hill Sands and the Nar Valley. The numerous raised marine beds
in Devonshire and Cornwall may be referred to here, together with

76 A. Bell—Succession of the Later Tertiaries in Gt. Britain.

the Selsey superficial Brick-earth and the Brighton ‘‘Elephant” bed.
The often-quoted deposit at Copford in Essex, and another con-
taining a similar fauna, with flint flakes, at Stroud, Gloucestershire,
650 feet elevation, belong to this stage, some of the species being
living known only in Yorkshire and far-distant places. Since the
paper on the Copford beds was written by the late Mr. John Brown,
the beds, although visited, I cannot find to have been practically
worked by any one except myself, Mr. Dalton’s memoir being
mainly a recapitulation of Mr. Brown, plus sundry errors.

Will Mr. Dalton kindly say where Mr. S. V. Wood states that
“three of the Helices from the Shell Marl no longer live in England,”
i.e. H. ruderata, H.incarnata, and H. fruticum: of the many thousands
of Copford shells I have had in my hands, I have never seen one of
the latter, and Mr. Wood’s figure, as already mentioned, is that of a
Stutton specimen. Mr. Wood further remarks that the H. incarnata
requires confirmation, and he does not say in what bed the H. rude-
rata was found, simply giving Copford. My experience of the Marl
is that very few shells, except freshwater species, are to be found in
it, and Mr. Brown particularly observes that it is only where the
marl passes into sandy clay at the sides, that they abound, and in the
peat. Dr. Gwyn Jeffreys speaks of the H. fruticum as at Copford ;
the reference, he told me afterwards, was under a misapprehension
of a remark of mine, that I had found the shell in England elsewhere
than at Stutton. Sir C. Lyell, ‘“Student’s Manual,” uses the same
words as Mr. Dalton, but the account of Copford given by Sir
Charles is inaccurate.

I have been a little more prolix than perhaps necessary, because
H. fruticum belongs to a group of shells pertinent to an age long
antecedent to the Copford peats, and the deposit is a typical one,
often-quoted but so seldom correctly, that it is quite as well that an
error should be set right if possible. Curiously enough, Mr. H. B.
Woodward (Geol. England and Wales, p. 833) makes the blue clay
beneath the marl to be the source of the Molluscan fauna. From
this clay I obtained teeth of Rhinoceros, and a nearly complete set
of teeth of a small deer, of which the whole skeleton was found.

Submerged forest and peat beds of this age may be occasionally
seen at Torbay, Anglesey, and beneath the Carse Clays of Falkirk,
and the Lothians, and the Buttery Clay of the Fens. Such peats as
yield Elephant remains may be safely placed here. There is no
improbability in supposing that the Mammoth lived on throughout
the minor glaciation, since we find his remains in the Reindeer
period in Kent’s Hole, the two periods being, if not as they may
probably have been, coeval, yet certainly closely, together in time;
and there is every ‘reason to believe that the Megaceros lived in
Ireland long after its extinction in England, and that the Reindeer
in Scotland was a still later survival.

The Bovey Heathfield Clay with Betula nana and Northern wil-
lows is, I think, an inland bed of this period ; but it is possible that,
like the Cratequs pyracanthus and others obtained from Grays Thur-
rock by Mr. Prestwich and Pinus sylvestris by myself, the flora
belongs to the period succeeding the major glaciation.

A. Bell—Succession of the Later Tertiaries in Gt. Britain. 77

The next or Neolithic stage corresponds with the formation of the
25 feet Raised Beaches of Scotland, comprising much of the ground
bordering the Clyde, especially about Glasgow, in which Tellina
calcarea, Leda pernula and other boreal shells appear for the last time
in Britain. Some of the beds in this district may be newer still, as
in various parts of the town of Glasgow many canoes have been
exhumed, from the large canoe dug out by fire and stone, a beautiful
weapon being found in one of them, to another in which a cork plug
formed part of the equipments, and a well-made clinker-built boat
with metallic (iron) fastenings.

The Carse Clays of East Scotland, and the Buttery Clays, or Fen
Silts of Lincolnshire and Cambridgeshire; the Megaceros Peat and
Bogs of Ireland, the Fen Peats with polished implements ; and most of
the submerged forest or tree patches skirting the coast, many west
country, Scotch and Irish, caves, as Hoyle, Perth, Chwaren, Cefn, and
a portion of the Settle Cave, Yorkshire, Oban and Kirkcudbright all
fall in this period, but so gradually pass up into the more recent
stage that an actual line of demarcation can seldom be drawn.

In these notes I have said but little about Ireland, having entered
fully into the subject in a prior communication ; it will suffice to say
here that every observation made then is fully applicable now, and
varies nothing from the lines worked upon above.

The latest deposits comprise the low level beaches in which the
fauna is still existing, of which Belfast and Largo Bays, and Portrush
furnish good examples, and the Scrobicularia clays and marine
beaches in marshy places, as the Burtle beds of Somerset, from whence
the sea has been comparatively speaking only recently excluded,
the Alluvial flats of Lancashire, and the whole series of intercalated
silts, clays, and peats of Somerset and Cornwall, the silts of tidal
rivers, the now forming sandbanks and shingles of the coast-lines,
the blown sands of Antrim with flint flakes, and of Galway and
Cornwall, containing Helices of types (H. nemoralis in particular)
of a size and structure now unknown, the Megaceros peat bogs
and underlying marls of Ireland, and the forest and surface peats
of Walthamstow, Newbury, Hull, Lincolnshire and Cambridgeshire,
the Caves and Midden deposits of Richmond in Yorkshire, Scotland,
and Ireland, and of Settle and Heathery Burn, the subaerial shell
beds of the Isle of Wight and elsewhere, and the tufaceous marls
formed by incrusting springs in Limestone districts.

Ail of these are due to such agencies as have been in ceaseless
operation since the Bronze dolichocephalic man came into Britain. In
Ireland there is every reason to suppose, and probably in the North
of Scotland also, that stone implements were in use to a much later
period than in England.

It would greatly facilitate the study of the later beds if authors
would, instead of quoting in their lists ‘‘ bones of birds or fish, elytra
of insects,” endeavour to ascertain what they are. Many species are
lost to science for want of such determinations. A list of peat
insects, and another of the plants absolutely found in (I do not
mean a list of those living which make it) the peat are a great
desideratum.

78 Reviews—Geology of Alsace and Lorraine.

In the foregoing notes I have endeavoured to classify the principal
deposits which throw any light upon the succession of the later de-
posits of our country, and by piecing the fauna and flora together to
show that, beyond the vast cessation of life during the great or major
glaciation, the succession of organic forms is one without violent
alterations, or necessitating alternate cold and hot periods. There can
be little reason to fear that ultimately a sequence of these varied
deposits and their contents will be established. The fuller the lists are
made, the sooner such a to-be-wished-for conclusion will be arrived at.

D=y) DEH WF IE DERN Ss

—— SS >

J.—ABHANDLUNGEN ZUR GEOLOGISCHEN SPECIALKARTE VON Hisass-
LovTHRINGEN.

Eiy BerrraG zuR KENNTNISS DER Exsasser Trrtrars. Von Dr. A.
Anprem. Mit 12 lithographirten Tafeln, 2 Kartenskizzen, und
10 Zincographien. Band IJ. Heft. II]. 1884.

Dex DrtuviaALsSAND von HanGENBIETEN IM UnteER-Ezsass, seine
Geologischen und Palzontologischen Verhiltnisse und vergleich
seiner Fauna mit der recenten Fauna des Elsass. Von Dr. A.
Anprem. Mit 2 photographischen Tafeln, einem Profil und
fiinf Zincographien. Band IV. Heft. I]. 1884.

Memoirs For THE SprcTAL GroztogicaL Map or Axsace-LorRAIne.
A Contribution to the Knowledge of the Tertiary Strata of Alsace.
By Dr. A. Anprex. pp. 351,12 4to. plates, 2 maps, and 10
zincographs.

Tur GEOLOGICAL AND PALMONTOLOGICAL RELATIONS OF THE DiLuviaL
Sanp or HanGenBIETEN IN Lower Axsacr, and a Comparison of
its Fauna with the present one of Alsace. By Dr. A. AnpREz,
pp- 90, 2 photographed plates, 1 profile, and 5 zincographs.

N the first of these memoirs a detailed description is given of the
Tertiary strata of Alsace. The lowest beds, which belong
to the Middle Eocene, are freshwater limstones distinguished by
the characteristic Planorbis pseudammonius and containing teeth of
Lophiodon and other mammals. Above these are sandstones with
plant-remains, and then thick beds of dolomitic limestones with
Melania and other freshwater genera, referred to the Upper Eocene.
Beds of Oligocene age are very extensively developed in Alsace, and,
on account of their containing petroleum and bitumen, are economic-
ally important. Borings have been made in them to a depth in
some places of 300 métres without penetrating through them. The
lowest Oligocene strata consist of beds of gypsum, apparently of
brackish-water origin; these are succeeded by petroleum-bearing
marls and sandstones, and then marine deposits of sand, marls,
septarian-clays with numerous foraminifera, and fish-bearing shales,
which belong to the Middle Oligocene. The Upper Oligocene
deposits are marine or strongly brackish marls, sandstones and con-
glomerates.

Reviews—Dr. Ruest—JTurassic Radiolaria. 79

The fauna and flora of these Tertiary deposits are very carefully
described and most admirably illustrated in the accompanying atlas
of plates; the figures have been drawn by the author’s own hand.
Numerous new species of freshwater mollusca and of foraminifera
are introduced.

The second memoir consists of a detailed description of a section
of diluvial or Post-Tertiary sands and marls exposed in the Rhine
valley at Hangenbieten, a short distance from Strassburg. ‘The total
thickness of the deposits is about 15 métres. The uppermost stratum
is a typical non-stratified Loess, containing land-shells exclusively,
which the author regards as Post-Glacial. Beneath this is a Loess
of nearly the same petrographical character as the bed above, but
containing freshwater as well as land-shells. Next below is a reddish
sand—known as renovated Vogesen sand—which contains 17 species
of land and 13 of freshwater shells, and in places remains of Mam-
moth and Reindeer. The author places this, and the Loess above it,
as probably of Glacial age. Under the Vogesen sand are concre-
tionary marls, in which the freshwater molluscs are more numerous
than the land forms, and these are succeeded below by fluviatile
sands in which 79 species of molluscs (48 land and 381 freshwater)
have been discovered. Four of these are entirely extinct species, and
many others have altogether disappeared from the district. A still
lower bed of sand with but few fossils in it forms the base of the
section. These lower beds are regarded as of Interglacial age.

The author furnishes a table in which a comparison is made of the
fauna of the Hangenbieten section with that now existing in Hlsace
and the district of the Upper Rhine, and with that of Mosbach near
Biebrich and of Mauer near Heidelberg. Descriptions are given of
some new forms, and all the species are shown with remarkable
clearness in the appended photographic plates. Ged es

IJ.—Beirrace zuR KENNTNISS DER FOSSILEN RADIOLARIEN AUS
GESTEINEN DES JuRA. Von Dr. Rist, in Freiburg I/B. Paleeon-
tographica, Band xxxi. Mit Tafel iixx. (Cassel, 1885.)

Conrriputions To THE KnowLepGe or Fosstt RapDIOLARIA FROM
Rocks or THE Jura. By Dr. Rvest, of Freiburg. Paleonto-
graphica, vol. xxxi. pp. 51, with 20 plates.

ITH the exception of a few species of Radiolarians from the
Upper Chalk of North Germany described by Zittel, and 18

species from the Lower Lias of the Tyrol, which Dunikowski has
named and figured,’ scarcely anything has hitherto been known of
fossil Radiolaria from strata older the Tertiary, and these minute
siliceous organisms have been regarded as forming but an insignifi-
cant part of the fauna of the older rocks. The present memoir, in
which 234 different species of Radiolaria belonging to 76 genera, are
described from Cretaceous and Jurassic strata, furnishes good evidence
1 Dr. G. C. Wallich has lately called attention to the occurrence of Radiolarians in

the cavities of flints from the Upper Chalk of Surrey, but they have not yet been
described. Ann. and Mag. Nat. Hist. 5th ser. vol. xii. p. 52, 1883.

80 Reviews—Dr. Ruest—Jurassic Radiolaria.

that they flourished as abundantly and in as great variety of form in
the seas of these periods, as in those of Tertiary and recent times.

From the Middle and Upper Chalk Dr. Riist discovered but few
Radiolarians, they were however abundant in Neocomian limestone
at Urschlau in Upper Bavaria. The so-called Aptychus-Schiefer from
Urschlau and several other places in the Tyrol were found to be very
rich in well-preserved specimens. They also occur in the Jasper and
Chert from rocks of ‘Tithon” age in the Upper Alpine Jura at
Allgaiu, near Murnau, and other places in the Tyrol. In the red
jasper the Radiolarians are so abundant that their shells are in close
contact in the rock, whilst in the chert on the other hand they are
comparatively rare. In this latter material the Radiolarians are re-
placed by sponge-remains and foraminifera, and many dark beds of
chert are stated to consist of bedded masses of scattered sponge-
skeletons (in the same manner as turf consists of remains of
Sphagnum), with a few scattered Radiolaria between. The red jasper
however, may be compared to a Radiolarian mud, like that brought
up from the greatest ocean depths by the Challenger expedition.

Fragments of this jasper, containing the same species of Radiolarians,
are found in gravels all over West Switzerland, and they are most
abundant in the Nagelfluh of the Rigi and the conglomerate of
Uetliberg.

In Hungary also, in chert and jasper of the age of the Tithon, the
Malm, and the Middle Dogger, Radiolarians were discovered.

The author obtained his richest harvest of Radiolarians from
Coprolites occurring mingled in beds of iron ore, which are largely
worked at Ilsede, near Peine, in Hanover.' The ore-deposits rest on
Gault-clay and are overlaid by Cretaceous marls, but neither in the
rocks above nor in those below were Radiolarians discovered. The cop-
rolites in these beds are round or cylindrical in form, and vary from the
size of a lentil to that of a goose’s egg, they are largely employed for
making superphosphate. The age of these coprolites was determined
by the occurrence with them of two species of Ammonites; one,
A. torulosus, Zieten, characteristic of the Lower Dogger, and the
other, A. caprinus, Schlot., of the Upper Lias. The author investi-
gated coprolites from the Lias of Lyme Regis and Gloucester, which
corresponded closely in character with those from Ilsede, but only in
those from Gloucester were some few Radiolarian remains discovered.

Further, in red limestones of Middle Lias age, and in Chert of the
Lower Lias in Hungary, Radiolarians were also present.

The author calls attention to the fact that whilst in Jurassic and
Tertiary strata a Radiolarian-fauna is so largely developed, in the
intervening Cretaceous beds hardly a dozen species have been found,
and it seems also to be a general rule, that where sponge-remains
and foraminifera are abundant, Radiolarians are of rare occurrence,
and vice versa.

1 The geological horizon of these coprolitic iron-ore beds appears to be the same
as that of the Cambridge Greensand; and it is worthy of notice that Radiolarians
have been discovered by Prof. Sollas in the Coprolites of this latter deposit, but they
have not yet been described. See Quart. Journ. Geol. Soc. vol. xxix. 1873, p. 78.

Reviews— Prestwich’s Geological Text-Book. 81

With the exception of two, apparently extinct, genera (Podocapsa
and Salpingocapsa), all the Jurassic Radiolarians can be included in
the genera set forth in Hackel’s Prodromus Systematis Radiolarium.
As a rule these older forms are more regular, simpler, and somewhat
larger than the recent, and they have less adornment and armature.

The species described are clearly shown in 18 of the accompanying
plates; most of the figures are drawn to the scale of 300 diameters :
on plate xix. are figures of plant-spores and other doubtful minute
objects met with in connection with the Radiolarians, and on plate xx.
some of’ the spicules of sponges are figured. ‘These belong to three,
if not four, of the principal divisions of siliceous sponges, and
include some very peculiar forms. One of these resembles the so-
called plumose (Tannen-baum) flesh-spicule of certain recent
Hexactinellids, and is the first hexactinellid flesh-spicule which has
been discovered in a fossil state. It would have been more satis-
factory to know the scale on which the spicules have been drawn.

One need hardly state that this memoir is a very important addition
to our knowledge of the microfauna of the Jurassic strata, and is
strong testimony of the patient industry and zeal of the author in
discovering these minute organisms from such various sources. We
are promised future notices of Radiolarians from Triassic and
Permian strata, which will be looked for with much interest.

G. J. H.

III.—Geotocy, Cuemricat, Puystcat, anD STRATIGRAPHICAL. By
JosEPpH Prestwicu, M.A., F.R.S., F.G.S. In Two Volumes.
Vol. I. Cuemican anp Puysicat. Royal 8vo. pp. xxiv. and
478, with three Chromo-lithographic folding Maps, three
folding Coloured Sheets of Sections, and 218 Woodcuts. (Oxford:
At the Clarendon Press, 1886.)

ya is an epoch marked by the production of geological text-
books. Year after year, a steady flow of manuals issues from

the press, and one prophet after another arises, each with some special

claim upon the attention of teachers and students.

Among the vast array of really good books the treatise just issued
by the Clarendon Press deserves our special notice, coming as it
does from the pen of Prof. Prestwich, one of the oldest living exponents
of the science, whose papers upon the Tertiary Geology of the South-
East of England, of France and Belgium, and upon the Geology of
Coalbrookdale, etc., may be found scattered broadcast through the
Transactions, Proceedings, and Quarterly Journal of the Geological
Society, while others upon cognate subjects adorn the Philosophical
Transactions of the Royal Society and the pages of the GroLocicaL
MaGazine.

The volume before us is devoted to Chemical and Physical Geology,
and will shortly be followed by a Stratigraphical and Paleontological
companion. ‘Three very pleasing features in the present book are
the excellency of the paper, the typography, and the illustrations—
matters, alas! too often neglected, but having a most vital importance
in the success or failure of a work. Three chromo-lithographic

DECADE III.—VOL. III.—NoO. Il. 6

82 Reviews—Prestwich’s Geological Text-Book.

folding maps, three sets of folding coloured sections, and no fewer
than 218 woodcuts (many of which are specially prepared for the
present work) adorn and make bright its pages, and render good
service in the elucidation of the author’s views.

Professor Prestwich, in his preliminary remarks, observes that
among geologists two schools have arisen, “one of which adopts
uniformity of action in all time,—while the other considers that the
physical forces were more active and energetic in past geological
periods than at present.”

“On the Continent and in America the latter view prevails, but
in this country the theory of uniformity has been more generally
held and taught. To this theory I have always seen very grave
objections; and I felt I should be supplying a want by placing
before the student the views of a school which, until of late, has
hardly had its exponent in English text-books.” It must be borne
in mind, however, that “the doctrine of non-uniformity must not be
confounded with a blind reliance on catastrophes; nor does it, as
might be supposed from the tone of some of its opponents, involve
any questions respecting uniformity of law, but only those respecting
uniformity of action.”

“J myself have long been led to conclude that the phenomena of
geology, so far from showing uniformity of action in all time, present
an unceasing series of changes dependent upon the circumstances of
the time; and that, while the laws of chemistry and physics are
unchangeable and as permanent as the material Universe itself, the
exhibition of the consequences of those laws in their operation on
the earth has been, as new conditions and new combinations succes-
sively arose in the course of its long geological history, one of
constant variation in degree and intensity of action.”

Prof. Prestwich very properly points out that, for the student, the
first object ‘‘ should be to study the laws to which the materials and
masses he has to deal with are subject, and then to consider what
may have been their action under varying conditions in past time.”
With this object the author has divided his work into four parts:
“The first, treating of the composition of minerals and rocks forming
the crust of the earth; the second, the mode of action of geological
agencies under existing and under past conditions: while the third
and fourth will treat of the succession of the groups of sedimentary
strata and of the life thereof, and of some of the theoretical questions
connected with the physical conditions prevailing during former
periods of the earth’s history.” The four earlier chapters up to p. 61
comprise a consideration of the constituents of the Harth’s crust,
which are enumerated and described, and all the numberless forms of
rocks resulting from the varying combination of their constituent
minerals are discussed and exemplified.

The mode of action of geological agencies should have commenced
at p. 62; but Chapter V. is occupied with an account of the “ Order,
Place, and Range of past Life.” This we venture to think might
have been held over and formed a part of Vol. II, in which the
Life-history of the Earth will be discussed.

Reviews—Prestwich’s Geological Text-Book. 83

We live in an age of change, and in no department have greater
changes arisen lately than in that of Biology. The author has
brought together in this chapter a series of tables of classification
of each group of the animal kingdom; but as these tables are neces-
sarily by various authors, and of very varying dates of publication,
from 1868 to 1883, some at least need emendation.

Thus in the classification of the Mammazia (p. 79) the Seals,
(Prxnipepta) have been placed with the Cetacea, whereas they are
now universally placed with the Carnivora; and the Sloths, Ant-
eaters, and Armadillos (Hpentrata), have been placed between the
Carnivora and Ropentia, whereas they are now placed next the
MarsvpIiaLtia.

The PrososcrpEA, PachypeRmMatTa, SoLipepra, and RUMINANTIA
are not so arranged by later zoological writers, but they form one
great order, the Uncunata (or hoofed quadrupeds) divided into
various sub-orders, as

Sub-order 1. HyracorpEa (Hyrax) ;

. 2. ProgposcrpKA (Elephants) ;

ss 3. AmMBLYpPoDA (Dinoceras, etc.) ;
4. Perissopactyua (Tapirs, Rhinoceroses, Horses) ;
FA 5. Artiopactyia (Pigs, Deer, Oxen, and Sheep).

Happily these and other needful modifications can be made in
Volume II., which deals with the Life-history of the Earth, and is
not yet published.

On yp. 69 the Myrtoropa have accidentally got between the
Decapopa and the Cirriprpra ; and on p. 68 Hntomostraca and
Malacostraca seem of equal classificatory value with InsxEcra,
the word Crustacea, which should be the leading one, being sub-
ordinated. The Aracunipa and Myriopopa should not be bracketed
together, they are really widely separated groups. Neither
should the Marsipoprancuit and the PHARYNGOBRANCHII be
bracketed together (p. 76). The first embraces the “ Hag-fish ”
(Myxine) and “ Lamprey” (Peétromyzon) ; the second a single form
the “ Lancelet” (Amphioxus), so anomalous as to be by some naturalists
relegated to a separate class !

It is, therefore, misleading to the student to bracket these
two together with the remark (after “no fossil forms known’’)
‘<2 Conodonts”; for if the curious little microscopic bodies called
“ Conodonts” met with by Pander in Russia and by Hinde in the
Cambro-Silurian and Devonian rocks of North America, are fish-
teeth, which is very doubtful,’ they must have belonged to the “‘ Hag-
fish ” (Myxine), and could have nothing to do with Amphioxus, which
is destitute of teeth or any other hard organs whatever.

But to pass on to the question [Chapter VI. (p. 82)] how
“Sedimentary strata are formed by river and sea erosion.” Com-
mencing in the truly philosophical ‘ Lyellian’ and ‘ Darwinian’
style to argue from the known to the unknown, we find the author
teaching his students ‘‘ to study the effects of the agencies at present

1 See Quart. Journ. Geol. Soc. vol. xxxv. 1879, pp. 351-368, plates xv.—xvii.
Compare these with the odontophore of certain mollusea, Strombus, Cassis, Triton, ete.

84 Reviews—Prestwich’s Geological Text- Book.

acting on the surface of the globe, in so far as they are of a nature
to furnish evidence which may assist in the interpretation of the
mode of formation of the sedimentary strata, of the disturbances to
which these strata have been subjected, and of the succession of life
of which they contain the remains.”

Then we have Rain treated as a geological agent; the formation
of Deltas, their age; River Denudation; the formation of Valleys ;
Drainage-Influences ; the Canons of the Colorado,—illustrated by a.
page-cut of Marble-canon and a glimpse at the Dolores cation.

From this we pass to the consideration of Marine Action,—the
origin of the coast shingle in the English Channel—illustrated by the
famous case of the Chesil Bank—and the cause of the wear of coasts,
illustrated by the gradual destruction of Lundy Island, an ‘outlier’
of the old North Devon Coast, the Chalk Cliffs of Brighton,
Dover, ete.

In Chapter VII. the subject is continued, and we are invited to
consider waste (by chemical solution) in the soluble matter carried
down to the sea and into lakes by Rivers; its character and quantity ;
and the resultant formation of Calcareous strata.

The Organic origin of Limestones is next touched upon, and the
presence of soluble silica inCretaceous and Jurassic strata is adduced as
evidence that a very different state of things existed then, to any which
obtains in the present seas. May not the soluble silica referred to
have been very largely derived from the subsequent decomposition of
the vast numbers of siliceous sponges which are known to have
existed in the seas of the Secondary period? and may not these
chemical changes have taken place long after the Calcareous muds
forming the sediments of these Mesozoic waters had been ac-
cumulated and to a great extent solidified ?

The author refers to the various modern Calcareous beds now
forming, such as the shell-limestones accumulating along many
coasts like that of Guadaloupe, the Canaries and the Island of
Ascension. He next glances at Deposits in Lakes, of which the
shell-marls always form a es interesting series, often rich in
organic remains.

From these the author passes on to consider those strata which
owe their present state to subsequent chemical reaction, such as
Magnesian Limestone, Gypsum and Rock-salt.

Space does not permit us to dwell longer on this interesting work.
The seventeen-chapters that follow are not merely a bare compila-
tion from the works of other observers, but Prof. Prestwich is able
to bring much of his own original labours in the past to bear upon the
subjects under consideration, and so to exalt the work into a far
higher position than that of an ordinary text-book.

We hope to come back to its consideration at a future day. A
most valuable feature of the book is its excellent Index of 27 pages,
of three columns to a page, which renders the contents easily
accessible to all, and gives the book a very high place as a work of
ready reference.

Reviews—Memoirs of the Geological Survey. 85

1V.—Memorrs oF THE GEOLOGICAL SURVEY.

1.—Turt Geronogy or HoiprerNess, AND THE ADgoINnING Parts
oF YORKSHIRE AND Linco~ysnire. By Cxiement Rei, F.G.S.
Svo. pp. 177. (London, 1885.) Price 4s.

HIS Memoir is devoted to an account of the Glacial and Post-

Glacial deposits of the Holderness district, that are included in

the area of Sheets 85, 86, and 94 of the Geological Survey Map.

The district was surveyed in part by Mr. J. R. Dakyns and in part

by Mr. A. C. G. Cameron, as well as by Mr. Reid, who however has
a personal knowledge of the entire region.

The Drift-deposits of Holderness occupy an old bay bounded by
Chalk hills, a bay whose form is due to the relative hardness of the
lower and upper beds of Chalk, the former standing out in the bold
headland of Flamborough. The Drift-deposits have been banked up
against the old line of Chalk cliffs, in places to a depth of 100 feet,
so that while geologically speaking the ancient Bay of Holderness
has been preserved, physically speaking it has been obliterated or
smothered up.

The oldest Boulder-clay, known as the Basement-clay, is interest-
ing from the occurrence in it of transported masses of sand and clay
full of mollusca. These fossiliferous layers have been described
under the name of Bridlington Crag; but the view that they are
included in the Glacial Drift, advocated by Mr. 8. V. Wood, has (with
a different explanation) been confirmed by Mr. G. W. Lamplugh and
Mr. Reid. It was indeed previously announced in the Grou. Mae.
(Vol. I. 1864), by the late Dr. S. P. Woodward, that the Bridlington
deposit can no longer be considered the equivalent of the Norwich
Crag, being of an Arctic character, a conclusion which, as Mr. Reid
remarks, “subsequent discoveries have only tended to confirm and
strengthen.” A revised list of organic remains from the Bridlington
Crag is now published, and this includes, besides Mollusca, Plants,
Foraminifera, Cirripedia, Entomostraca, and Vertebrata. The Verte-
brata are probably derived from Crag, Hocene, or older deposits.
Remains of Echinodermata and Polyzoa have been fonnd, but these
as yet are undetermined. Mr. Reid observes that while the Base-
ment-clay is the lowest bed exposed in the Holderness cliffs, the
Chalk is generally about 60 feet beneath the sea-level—hence older
Glacial or even newer Pliocene beds may be concealed in places.

Above the Basement-clay, other layers of Boulder-clay, known as
the Lower and Upper Purple Clays and the Hessle Clay, are locally
to be distinguished. Mr. Reid makes some important observations
on the weathering of Boulder-clay, whereby chalky Boulder-clay
passes into reddish-brown stony loam.

Associated with the Boulder-clays are marine Inter-Glacial and
other gravels and laminated clays. The Inter-Glacial beds have
yielded mammalian bones, and a marine fauna indicating a climate
that seems to have been little if at all colder than that of the same
region at present. A full list is given of the organic remains found
at Kelsey Hill, and other places, and a column showing the forms

86 Reviews—Memoirs of the Geological Survey.

found at March in Cambridgeshire is added. A description of the
Post-Glacial deposits and their organic remains, contains the observa-
tion that Felis spelea and perhaps Elephas primigenius are true
Post-Glacial species. The Lion has been found at Hornsea, associated
with the Jrish Elk, Horse, and Red-Deer, apparently in the ancient
deposits of the Mere.

A chapter is devoted to the changes now in progress. The serious
loss of land along the coast-line within historic times is well known,
and this is clearly illustrated by diagrams or reproductions of charts
dating from 1684. Since this period the average rate of advance of
the sea has in places been about 21 yards a year. In other places
land has been gained.

A concluding chapter gives an account of the Economic Geology—
soils, brickmaking, etc., with some mention of the Humber Tunnel.
The Water-supply is also discussed, and details of a number of Well-
sections and Borings are given. An appendix contains a list of
works on Holderness.

2. Tur Grotocy or Bripiineton Bay. By J. R. Daxyns and
C. Fox-Srraneways. 8vo. pp. 18. (London, 1885.) Price 1s.
HIS is a brief explanation of Quarter-sheet 94 N.E. of the Geo-

d logical Survey Map. It includes an account of the Chalk,

Glacial and Post-Glacial Beds. Mr. Reid contributes the List of

Fossils from the Bridlington Crag.

3. THe GroLogy or THE SoutH-West Part or LIncoLNsHIRE, WITH
Parts oF LEICESTERSHIRE AND NorrincHamsHIRE. By A. J.
Jukrs-Browne, B.A., F.G.S. (Parts by W. H. Datron, F.G.S.)
Svo. pp. 180. (London, 1885.) Price 4s.

HIS is a description of the rocks embraced in the area. of Sheet
70 of the Geological Survey Map. The area was chiefly
surveyed by the late Mr. W. H. Holloway, other portions being
mapped by Messrs. W. H. Penning, W. H. Dalton, and A. J. Jukes-
Browne. The rocks include the Upper Keuper Marls, the Rheetic
Beds, the Lias, the Oolites from the Northampton Sand to the
Kimmeridge Clay, and various Glacial and Post-Glacial deposits.
Detailed descriptions of the strata are given, and the palzeonto-
logical divisions, with lists of fossils, are duly noted. ‘The junction
of the Lower with the Middle Lias is taken at the top of the clays
with Ammonites capricornus: so that a number of forms regarded as
Middle Lias in Dorsetshire are now placed in the Lower Lias.
This higher line was adopted by Prof. Judd in the Rutlandshire
district, and hence it was desirable to continue it northwards.
Ammonites communis is noted from the Middle Lias, so that our
notions of the value of Ammonites as indices of zones are liable to
be shaken. It is remarked that the zones of Ammonites Humphries-
danus and A. Parkinsoni are altogether absent from Lincolnshire, unless
the former is represented by the upper portion of the Lincolnshire
Oolite.
The Glacial deposits include representatives of the Chalky Boulder-

Reviews—Memoirs of the Geological Survey. 87

clay, Purple and Hessle Clays, with associated gravels. ‘The large
transported masses of Lincolnshire Limestone and Marlstone, to
which attention was first directed by Prof. Morris, are described ;
and Mr. Jukes-Browne regards them as due, together with the
Boulder-clay itself, to the agency of coast-tce.

Among the mineral resources of the district, the Lincolnshire
Limestone is noteworthy, being largely quarried at Ancaster. Of
the iron-ores, that derived from the Marlstone Rock-bed is most
important, and it has been lately described by Mr. H. Wilson
(“Midland Naturalist,” vol. viii. 1885). The gypsum in the New
Red Marls at Newark is also extensively worked.

4. Tur Grotocgy or EskpaLe, Rosrepaue, ete. By C. Fox-
Srraneways, F.G.S., C. Rem, F.G.S., and G. Barrow, F.G.S.
8vo. pp. 65. (London, 1885.) Price 1s. 6d.

te is an Explanation of Quarter-sheet 96 N.H. of the Geological

_ Survey Map. It contains an account of the Lias, the Oolites
from the Dogger to the Middle Calcareous Grit, and of the Glacial
and Post-Glacial beds.

The Upper beds of the Middle Lias, which constitute the Iron-
stone series, are described in detail. They furnish the well-known
Cleveland Ironstone. The Dogger, which occurs at the base of the
Oolites, is a variable bed changing from limestone to sandstone, and
in places yielding the valuable iron-ore of Rosedale.

In the Lower Estuarine Series, above the Dogger, comes the
Eller Beck Bed, yielding marine fossils, which was described by
Mr. Barrow in the Gronocican Macazine (Decade II. Vol. IV.
p- 552). Higher up there is a bed of coal which has been worked.
The Grey Limestone Series, and the Upper Estuarine Series, the
Cornbrash, Kellaways Rock, Oxford Clay, and Corallian Rocks,
present many features of interest, and their paleontological contents
are duly noted. The Whinstone or Cleveland Dyke is an intrusive
dyke of augite-andesite.

The absence of Drift over most of the country now described is
remarkable. Boulder-clay extends to a height of about 800 feet in
the valleys to the north of the table-land, but is not met with in the
interior, nor has any trace been found there of local glaciation.
Hence it is concluded that the uplands formed an insular space
round which the ice-sheets swept, while these high grounds were
not glaciated.

5.—Tur Gerorocy or THe Coasts ADJOINING Ruyt, ABERGELE AND
Cotwyy. By Avusprey Srranan, M.A., F.G.8. (with Notes by R.
H. Tippemay, M.A., F.G.S.) 8vo. pp. 738. (London.) Price 1s. 6d.
HE area here described is included in Quarter-sheet 79 N.W. of
the Geological Survey Map, and was originally surveyed by
Messrs. W. T. Aveline, W. W. Smyth, and A.C. Ramsay. The
ground having been re-surveyed on the scale of six inches to a mile,
by Messrs. Tiddeman and Strahan, the map has been revised, and
this Explanation published.

88 Reviews—The Geological Record.

The rocks include Wenlock Shales, Carboniferous Rocks, Bunter
Sandstone, Glacial Drifts and Post-Glacial Beds. Between the Base-
ment-beds of the Carboniferous rocks (red conglomerates, etc.) there
exists “one of the greatest unconformities to be met with in the
British Isles,” the Silurian strata having been cleaved, contorted,
and denuded before the overlying rocks were laid down. In the
pebbles of these Carhoniferous conglomerates many Ludlow fossils
have been found.

The principal formation described is the Carboniferous Limestone,
from which many fossils have been obtained. The Millstone Grit is
interesting, from the remarkable development of chert met with.
Mr. Strahan remarks that unlike the bands and nodules of chert in
the Carboniferous Limestone, this chert is probably a siliceous
sediment of extreme fineness; for not only is it well stratified, and
evenly laminated, but, by a gradual lithological change, it passes
horizontally into a fine-grained quartzose sandstone, with bands of
chert, and finally into a quartz grit with quartz pebbles, in which
chert bands are quite subordinate. The Lower Coal-Measures and
Trias are briefly described. The whole of the low ground and the
flatter parts of the high ground are overspread by Drift-deposits
consisting of Boulder-clay and Gravels. The Post-Glacial Beds
comprise Calcareous Tufa, Peat and Alluvium, and Blown Sand.
In a Chapter on Economic Geology accounts are given of Lead and
Zine Ores, Hematite, etc. An Appendix contains a list of works
on the Geology, etce., of Denbighshire and Flintshire, by Messrs.
Whitaker and Strahan.

V.—TuE GrotocicaL ReEcorp.

HE “Geological Record” was founded in 1874, with the object

of publishing a yearly register of all publications relating to

Geology, Mineralogy, and Paleontology. The volumes for the years

1874 to 1878 have appeared with brief abstracts; that for 1879 is in

the press. These have been prepared under the editorship of Mr.

William Whitaker, B.A., F.G.S., who has spared no pains, amid

many disappointments and delays, to render the volumes as complete
as possible.

The British Association gives a grant in aid, sufficing for some
assistance, the correction of proofs, etc. The greater part of the work,
however, is done by geologists who give their help gratuitously.
There are no funds available for the purchase or exchange of pub-
lications. Hence the Editor is to a very large extent dependent on
the exertions of voluntary assistants. No doubt the delays have
tended to damp the ardour of many who have laboured on behalf of
the Geological Record.

Mr. Whitaker has now retired from the position of Editor, and
Mr. William Topley, F.G.S., Assoc. Inst. Civil Eng., has bravely
undertaken to carry on the work. In order to bring the “‘ Geologi-
cal Record” up to date, he has decided to issue one volume for the
five years 1880-1884 with titles only, and to resume the abstracts
for the year 1885.

Reviews—Proceedings of Ohester Natural Science Society. 89

From a circular just issued we learn that the present Editor
would gladly welcome further assistance, and would be especially
thankful if authors would forward to him brief notices of papers, etc.,
appearing in the publications of provincial societies, which are often
not easily obtained in London. Authors, secretaries of societies, and
editors of geological publications would also greatly assist the work
by forwarding copies of their publications to the Editor of the
‘Geological Record,” 28, Jermyn Street, London, 8.W.

VI.—Procrrpines or THE CHESTER Soctery or NATURAL SCIENCE.
No. 3. 8vo. pp. 1384; 9 Plates. (Printed and Published by Giles
Griffith, Chester, 1885.)

({\HE present volume includes fifteen papers upon various subjects

read before the Society from 1878 to 1884. Of these papers
eight are of geological and paleeontological interest.

The first is by the President of the Society, Prof. T. McKenny
Hughes, M.A., F.G.S., entitled ‘Notes on the Geology of the Vale of
Clwyd.” As to the merits of this paper it is sufficient to say
that it is upon a subject which is peculiarly the author’s own. It is
illustrated by eight plates (23 figures), and is a most valuable con-
tribution to the geology of the district. After a short introduction,
the rocks found in the Vale of Clwyd are briefly described in order,
beginning with the oldest or Bala series, and passing upwards to the
recent Cave-deposits. Under each formation we have a list of its
chief fossils and peculiarities of structure and comparisons with the
same horizons in other districts, along with valuable local notes as
to where the most interesting sections may be most easily observed.
There is a valuable note ‘“‘On the Weathering of Mountain Limestone,”
explaining in a very clear manner the formation of those caves with
which we are all so familiar in limestone districts, and at the same
time mentioning places where the effect of the weathering may most
easily be observed. It is impossible to over-estimate the importance
of such a paper as this to local geologists ; for, rich as it is in facts
and details, it is still richer in suggestions which need for their
working out the time and patience of the local geologist ; and we do
not doubt that this paper by the President will originate much good
work, which will appear in future volumes of the Proceedings.

The next paper is by Mr. Aubrey Strahan, M.A., F.G.8., on “ The
Denudations of North Wales.” This is an admirable paper by one
who for a long time was associated with the Society as Honorary
Curator of the museum, when he was engaged in the Geological
Survey of the district. In the present paper Mr. Strahan proposes
to examine the evidence, afforded by examples in this district, of the
fact that “‘ while existing lands, being themselves chiefly formed of
stratified marine material, occupy the sites of seas of former
geological periods, on the other hand these seas overspread the ruins
of still more ancient continents.” This paper is one which all local
geologists should read, and all the places mentioned will well repay
a fresh visit in the new light thrown on them by Mr. Strahan’s paper.

Then follows a paper by Professor Judd, F.R.S.—“ A Problem

90 Reviews—Proceedings of Chester Natural Science Society.

for Cheshire Geologists.” The paper is an abstract of one read
before the Society, Nov. 27th, 1878. Professor Judd shows that
the strata of the various formations were originally much more
widely distributed over the British Islands than they are at the
present day, and that the breaks in their continuity must have
been caused by subsequent denudation. Not only is this true in
the case of the older Carboniferous rocks. It is probable that
before the deposition of the Tertiary rocks, the greater part of
the British Islands was “buried under the thick strata of the
Liassic and Oolitic age, and that a great winding sheet of Chalk
enveloped nearly the whole of the country.” The greater part of
the Secondary strata has now been removed by denudation, and
much interest naturally attaches to these isolated patches or ‘‘ out-
liers.” One such patch is in the district lying between Audlem and
Wem, and the problem for Cheshire geologists, writes the Professor,
is—(1) To determine the exact extent and limits of the outlier.
(2) The relations to the surrounding strata. (8) The nature, thick-
ness, and fossil contents of the outlier. We hope Cheshire geologists
are now on their way at least to the solution of this geological
problem.

We now come to a very short note on “Traces of an Interglacial
Land-surface at Crewe,” by that veteran geologist Mr. D. Mackintosh,
F.G.S. These traces the author supposes he has found in an exceed-
ingly fine and more or less flexible kind of leaf-clay which he
discovered at the Crewe Railway Station.

The next paper is one by Mr. W. Shone, F.G.S., on “ The Silting-
up of the River Dee: its Causes.” As an introduction to his
paper, Mr. Shone first gives us some account of the river both in
historic and in prehistoric times, with some interesting quotations
from early writers. Then follow a number of details—the result of
much patient observation—as to the rate of flow of the tide up
the river, and its rate of outflow back again to the sea. Mr. Shone
attributes the silting-up of the river to several causes combined, the
chief of which are—the tapping of the water at Llangollen for the
canal; the building of the causeway, and the reclaiming of the land
on Sealand. We cannot help thinking that, after all, the real cause
of the silting-up of the Dee is the extremely small amount of fresh
water which comes down from Bala Lake. We know that in dry
seasons, with the exception of a small quantity of water which passes
over the mill, no water at all finds its way over the Causeway,
and of course there would be just the same flow so far as volume is
concerned, whether the Causeway were there or not. But the upper
part of the river instead of being practically a jong lake would be a
shallow muddy river, were the Causeway removed.

Three papers follow by Mr. A. O. Walker, the first two on ento-
mology and the third on a meteorological subject. The first, on
‘Climatic Causes affecting the Distribution of the Lepidoptera in
Great Britain.” The second is ‘‘ A List of the Macro-lepidoptera of
the District.” The third by Mr. Walker is on the “Climate of the
Cheshire District in Relation to Fruit-growing.”

Reports and Proceedings—G'eological Society of London. 91

Dr. Stolterfoth follows with an account of his work at “Sur-
face Dredging in the Dee.” This paper is especially interesting
to microscopists, as it deals entirely with diatoms and the lower
forms of animal life, and shows how very abundant are the lower
forms of life in the estuary of the Dee. Then four papers by
Mr. G. W. Shrubsole. The first a note on the Polyzoon, “ Glauco-
nome disticha, from the Bala beds of Glyn Ceiriog.” In this paper
Mr. Shrubsole describes a new genus of Polyzoon, which for some
time has been regarded as identical with Glauconome disticha from
the Dudley beds. The new name proposed is Pinnatopora Sedqwickit.
There is a list of land and freshwater shells compiled by Mr.
Shrubsole “from local collections sent in from time to time at
the annual conversaziones.” It consists of 95 species and 19 varieties,
and is followed by a few interesting remarks. A paper “On the
Occurrence of Calcisphera (Williamson) in the Mountain Limestone
of the Eglwyseg rocks, near Llangollen,” by Mr. Shrubsole, follows
next. In this paper Mr. Shrubsole has brought together in a clear
and concise manner all that is known about these curious fossil
Rhizopods, about which there has been so much dispute as to whether
we should classify them with the Foraminifera in virtue of the
calcareous material of which their remains are composed, or with
the Radiolaria in virtue of their minute structure. There is also a
brief note by Mr. Shrubsole on the occurrence of Venus mercenaria.
Then follows a paper, by Mr. Ruddy—“ A List of Caradoc or Bala
Fossils, found in the Neighbourhood of Bala, Corwen, and Glyn
Ceiriog ”’—one of the most valuable in this number of the Pro-
ceedings, giving evidence of years of patient work, and which no
one who wishes to work at the Bala beds can possibly afford to be
without. The last paper is a botanical one by Mr. J. D. Siddall, on
“The American Water-weed, Anacharis alsinastrum, Bab.,” illustrated
by a carefully drawn plate.

pees @ ieee) PAN) ike © © ae PINGS:

——_@—__<—_
GrotocicaL Society oF Lonpon.

J.—Dec. 16, 1885.—W. Carruthers, Hsq., Vice-President, in the
Chair.—The following communications were read :—

1. “Old Sea-beaches at Teignmouth, Devon.” By G. Wareing
Ormerod, Esq., M.A., F.G.S.

The author stated that while old records show that no important
changes have taken place in the level of the Teignmouth district
during the historical period, the excavations made in recent drainage-
operations in the present year showed the existence of at least two
series of beaches. The oldest sea-beach, which is a few feet above
the present sea-level, was partly washed away and then covered up
by later deposits exhibiting evidence, in a number of delicate bivalve
shells in an unbroken condition, of having been deposited in a calm sea.

2. “On the Gabbros, Dolerites, and Basalts of Tertiary Age in
Scotland and Ireland.” By Prof. John W. Judd, F.R.S., Sec.G.s8.

92 Reports and Proceedings—

In previous papers published in 1874 and 1876, it has been demon-
strated by the author that there exist in Scotland and in Hungary
igneous rock-masses presenting the most perfectly crystalline
characters and belonging to the Tertiary period. It was further
shown that such highly crystalline, plutonic rocks are seen passing
insensibly into volcanic rocks of the same chemical composition—
gabbros into basalts, diorites and quartz-diorites into andesites, and
quartz-andesites and granites into rhyolites—the lavas in turn
graduating into the perfectly vitreous types known as tachylytes and
obsidians.

The present paper deals with the basic rocks of Western Scotland
and Northern Ireland, which are shown to exhibit the most marked
analogies with rocks of the same age in the Faroe Isles and Iceland ;
these facts lend strong support to the doctrine of the existence of
petrographical provinces. The Tertiary age of the Scotch and Irish
rocks is placed beyond dispute by the fact that they overlie uncon-
formably the youngest members of the Cretaceous system, and are
interbedded with stratified deposits of Lower Tertiary age.

With regard to the nomenclature of these rocks, the identification
of the more crystalline forms with the gabbros, which was made by
Zirkel and Von Lasaulx, is supported; while the use of the term
*¢ dolerite’ as a convenient one for the connecting links between the
gabbros and basalts is advocated.

Of the original minerals contained in these rocks, plagioclase
felspar (ranging in composition from anorthite to labradorite), augite,
olivine, and magnetite, are regarded as the essential ones; while
enstatite, biotite, chromite, picotite, and titanoferrite are among the
most frequently occurring accessories. It is shown, however, that
these original minerals may belong to different periods of consolida-
tion. The Secondary minerals are very numerous, including quartz,
epidote, zoisite, hornblende, serpentine, and zeolites, with many other
crystallized and uncrystallized substances. There are remarkable
variations in the relative proportions of the original minerals in
different examples of the rock; and by the complete disappearance
of one or other of the constituents, the gabbros are sometimes found
passing into picrites, eucrites, or troctolites.

In their microscopic structure these rocks present many interesting
features. From the highly crystalline gabbros there are two lines
of descent to the vitreous tachylytes: one through the ophitic
dolerites and basalts, and the magma-basalts with skeleton-crystals ;
and the other through the granulitic dolerites and basalts, and the
magma-basalts with granular microliths. The former are shown to
result from the cooling down of molten masses which were in a state
of perfect internal equilibrium ; while the latter were formed when
the mass was subject to movement and internal strain.

It is shown that in the most deeply seated of these rocks (gabbros)
the whole of the iron-oxides combine with silica; but, as we approach
the surface, the quantity of these oxides separating as magnetite
increases, until it attains its maximum in the tachylytes. In all the
varieties the order of separation of the different minerals is shown

Geological Society of London. 93

not to depend solely on chemical causes, but to be influenced by the
conditions under which the rocks have cooled down.

Although these rocks are not highly altered ones, yet they afford
admirable opportunities of studying the incipient changes in their
constituent minerals. The nature of these changes is discussed, and
they are referred to the following causes :—(1) the corrosive action
of the surrounding magma on the crystals; (2) the changes produced
by solvents acting under pressure in the deep-seated masses (these
have been already described under the name of “ schillerization ”) ;
(3) the action of heated water and gas escaping at the surface ;
(4) the action of atmospheric agents on the rocks when exposed by
denudation ; and (5) the changes induced by pressure during the
great movements to which rock-masses are subjected.

JI.—Jan. 13, 1886.—Prof. T. G. Bonney, D.Sc., LL.D., F.R-S.,
President, in the Chair.

The President said, It may not be known to all present this
evening that during the past week we have lost a well-known
member of forty years’ standing. Prof. John Morris died last
Thursday, and to-day some of us have stood by his grave
in Kensal Green Cemetery. The Society has lost its most

learned member, and many of us have been deprived of a very
dear friend.

1. “On some Fish-remains from the Tertiary Strata of New
Zealand.” By James W. Davis, Esq., F.G.S.

A number of fossil fish-remains from Tertiary beds in New Zea-
land have been forwarded to the author by Captain F. W. Hutton,
and were described in the present paper. The forms of which
descriptions were given are two new species of Lanna, Carcharodon
angustidens, Agassiz, and a new Carcharodon, one new species of
Notidanus, one of Myliobatis, and one referred to Sparnodus. All
the above are founded on teeth. A vertebra of Lamna and a fish-
spine were also described, and the collection contained a specimen
regarded by the author as a fragment of a Reptilian tooth.

2. “On a recent Section through Walton Common, exposing the
London Clay, Bagshot Beds, and Plateau-gravel.” By W. H.
Hudleston, Esq., F.R.S., F.G.S.

During the past autumn the widening of the line between Walton
and Weybridge stations has afforded a very interesting section in the
above beds, showing their relations to each other with considerable
clearness. Walton Station is 68 feet above O.D., and immediately
to the westward the section described in the paper commences, the
surface of the country gradually rising to a height of about 120 feet
in the plateau which separates the drainage of the Mole from the
drainage of the Wey. This plateau is connécted on the south by a

94 Reports and Proceedings—Geological Society of London.

slope with the higher and far narrower plateau of St. George’s Hill,
having an elevation of 246 feet.

For convenience of reference the portion of the section more
particularly described, and which has a length of 1070 yards, is
divided into four blocks :—

Block A extends from Walton Station to where the unaltered
London Clay is seen—310 yards.

Block B extends from this to the point where the Bagshot beds
are first seen in situ—d45 yards.

Block C extends from the above to the point where the Bagshots
are first cut through to the level of the line, and the hollow filled up
with Plateau-gravel—165 yards.

Block D exhibits the relations of the Bagshots to the Plateau-
gravel, where the latter is most fully developed—247 yards.

Details of Block A.—This portion of the section rises from zero to
12 or 14 feet; the first bed which becomes visible is the “Top
Sand,” and on advancing further westward portions of a peculiar
mixture of gravel and lumps of brown clay form the sides and floor
of the cutting. This is evidently a disturbed series, and has peculiar
relations with a mass of yellow sand, mainly false-bedded, which is
70 yards long, and from 12 to 14 feet high at the west end. The
London Clay in situ rises very suddenly beyond this. Reasons were
given for supposing this sand to be a superficial deposit against a
steeply eroded surface of London Clay.

Details of Block B.—The London Clay of this block has yielded
no fossils, nor are any Septaria visible. The bedding is difficult to
distinguish, but recent weathering has made it more plain. This
seems to establish a very slight dip towards the west. The surface
of the London Clay is undulating, and it is overlain by from 6 to 7
feet of Plateau-gravel.

Details of Block C.—In this block, where the cutting has a depth
of about 24 feet throughout, occurs the junction of the Lower Bag-
shots with the London Clay, and this is apparently an unconform-
able one. Both the lithology and the stratigraphy favour this view.
Nothing in the nature of a lithological passage exists. The lowest
bed of the Bagshots here is remarkably clear sand full of false-
bedding, and is succeeded by an argillaceous series, also somewhat
sandy. It was suggested that this latter might be the equivalent of
the ‘‘ Ramsdell Clay.”

Details of Block D.—Here the Plateau-gravel attains its maxi-
mum thickness, since the Bagshots are cut through to the level of
the line in three places—depth of cutting from 24 to 27 feet,—thus
affording a fine opportunity for the study of this peculiar deposit.
Three horizons were roughly made out, or, rather, three varieties
occurring one above the other. Beyond the limits of the section there
is more distinct evidence of at least two groups in these Plateau-
gravels. No materials from the northern drifts are found.

Other sections in the superficial beds were noticed, and more
especially one about the 180-feet line on the north slope of St.
George’s Hill, where the contortions are of considerable interest.

Obituary—Professor John Morris.

PROF. JOHN MORRIS, M.A. CANTAB., F.G.S., ETC.
Born Fesruary 19ru, 1810; Drep January 7TH, 1886.

[For more than twenty years one of the Editors of this Macazrne.]

The new year has gathered into its earliest garner another
ripened human intellect, whose influence and usefulness in the
Geological world for nearly 50 years have done much to promote
in others a love for our science to which that life was devoted.

Professor John Morris was born in the very dawn of
accurate Geological thought in this country.

Hight years before his birth, in the spring of 1802, Playfair
had published his celebrated “Illustrations of the Huttonian
Theory.” In 1807, a handful of scientific men met together
and founded the Geological Society of London; and from 1799
to 1815 William Smith (better known as “the Father of
English Geology ”) was plodding over England, with quiet
unobtrusive labour, preparing, unaided, his work, entitled
« Strata Identified by Means of their Organized Fossils,” and
his great “Map of the Strata of England and Wales.”

In June, 1812, James Sowerby commenced to publish (in
about bi-monthly parts of 5 plates each) his “Mineral
Conchology of Great Britain.”

Such was the condition of the literature of our science in
England early in this century. There were no text-books for
young geologists in those days, and the science of Geology
was no easy path to pursue; yet John Morris had already
taken up the study of rocks, minerals, and fossils, and com-
menced to collect materials for his ‘Catalogue of British
Fossils,” before the first edition of Lyell’s «: Hlements” had
been printed, and as early as the first appearance of his
“Principles of Geology,” a little book of one volume 8vo.,
which saw the light in January, 1830, whilst Morris, then
twenty years of age, was engaged in business in Kensington
as a Pharmaceutical Chemist.

The modest precursor to Morris’s Catalogue was printed
at Norwich, and designated ‘“‘ A Synoptical Table of British
Organic Remains, in which all the edited British Fossils are
systematically and stratigraphically arranged in accordance
with the views of the geologists of the present day, and a
reference given to their localities, strata, and engraved figures,
by Samuel Woodward.” This little book of fifty pages, which
appeared in 1830, gave all that was known at that date con-
cerning our British Fossils.

Morris published the first Edition of his Catalogue in 1845,
but he had issued preliminary notes, section by section, in the
“ Magazine of Natural History” from 1889 to that date.

The second edition appeared in 1854; but though constantly
urged by his friends to do so, and incited by the awards of the
Geological Society, he never achieved a third edition.

96

Obituary —Professor John Morris.

From 1854 to 1877 Prof. Morris held the Chair of Geology
in University College, and during that period he delivered
no fewer than 1100 lectures to his class, besides directing
field-excursions, and giving demonstrations in the Museum.

Of the details of his life and work and the well-merited
honours that have been conferred upon him, a full account
will be found in the Grotogican MaGazine, Decade II. Vol.
V. November 1878, pp. 481-487, accompanied by a portrait.

Like all men of great mind, Prof. Morris had his peculiar
traits of character; but he will be remembered by one thing,
more than any other, namely, his extreme readiness to impart
scientific information to those around him out of the vast (one
might almost say inexhaustible) stores of knowledge which he
had for years accumulated in his retentive mind, and yet could
retail again most accurately when needed, and even recall the
very place in the work from whence he had culled it.

Professor Morris was essentially a ‘young-hearted’ man
with his friends, and especially so when out with his class,
or with the Members of the Geologists’ Association. Indeed,
one has to compare events and dates in order to show that he
was in reality a survivor in our time from the prehistoric age
of geology. Morris was in fact the contemporary of Mantell,
Buckland, Fitton, Searles V. Wood, Bowerbank, Scrope, Owen,
Murchison, and Lyell; and of his earlier personal friends
amongst the great geologists—alas ! now few indeed in number
—only Prof. Prestwich, F.R.S., of Oxford, remains.

It is not without interest to record that almost the last piece
of work in which he engaged was to arrange, compare, and
verify the original specimens of the ‘ William Smith Collec-
tion,” preserved in the Geological Department of the British
Museum, the first collection formed with a view to prove that
strata could be identified by their fossil contents.

Ill-health has prevented Prof. Morris for the past two years
from attending scientific meetings or visiting his friends, as in
days of yore; but up to the last he was cheered by nothing so
much as a visit from a geological friend and a chat about some
new geological book. And whenever his health permitted, he
amused himself by continuing the preparation and revision of
the lists of fossils for the third edition of his Catalogue.

He died on the 7th January from heart-disease, and was
interred on the 18th at Kensal Green Cemetery, where many
of his fellow-geologists assembled to do honour to so veteran
an associate.

It will gratify the admirers of Prormssor Morris to learn
that it is the wish of his friends and family to raise a suitable
and lasting Monument to his memory, and that this memorial
shall take the form of a Tutrp Epirion or Morris’s CataLocur
or Bririsa Fossrzrs.—H. W.

THE

GEOLOGICAL MAGAZINE.

NEW SERIES. DECADE III. VOL. Ill.
No. I1].—MARCH, 1886.

(Gre kG MEIN ary va Sy abun ahs).

———=" > ——

J.—On THE PERMANENCE OF CONTINENTS AND OcEAN-BASINS, WITH
SpectAL REFERENCE TO THE FoRMATION AND DEVELOPMENT OF
THE NortH AMERICAN CONTINENT.

By Prof. JosepH Lr Conve.

NDER the influence, perhaps, of the prevailing idea of evolution
in all things, the conviction has been growing in the minds of
geologists in recent times that the larger features of the earth’s
surface have grown from the earliest times, and therefore that the
places of the continents and ocean-basins have been substantially
permanent. Prof. Dana is largely the originator and expounder of
this view, and he has applied it with great skill to the American
continent. But while I believe the view is substantially true,
I cannot but think that it may be, and has been, pushed too far. It
is true indeed that the opponents of the view have attributed to its
advocates a strictness in the use of the term ‘ permanent’ which they
have never urged. Itis true that by permanence is meant only per-
manence of place, not of outline, and that substantial permanence is
not inconsistent with very large changes by oscillation, especially at
the end of the great Hras. But, making every allowance for such
latitude of meaning, there has been, undoubtedly, some confusion
of thought and looseness of statement on this subject. We give
a few examples.

Prof. Dana in his admirable manual, p. 149, gives a figure (fig.
206), which he calls ‘‘ Archean map of N. America.” This is really
a map of Areas of exposed Archean rocks, and for such it is doubtless
intended. It cannot, of course, be a map of the land of Archean
times (since Archean rocks were formed on sea-bottom), but
is approximately a map of land of early Silurian times. But being
called an Archean map of the continent, and being found in the
chapter on Archzean times, the inattentive reader is led to infer that
it represents land of that time; more especially as the rest of the
present continent is spoken of and represented as submerged, and
therefore by implication this part as, then, land. And as Prof.
Dana afterwards treats these areas as the nucleus from which the
continent was developed, he seems to begin this development from
the land of Archean times. I am quite sure that many have been
misled by this figure and the accompanying statements.

Again, Prof. Chamberlin in his excellent ‘‘ Geology of Wisconsin,”
vol. i. p. 62, gives a map somewhat similar to Dana’s, which he

DECADE III.—VOL. III.—NO. Ill. 7

98 Prof. J. Le Conte—Permanence of Continents, ete.

calls a “ Map of Laurentian land.” It is, of course, again a map of
Laurentian rocks, and therefore not of land of Laurentian times.
But being evidently intended as a map of land of some time, and
being given in the chapter on Pre-Laurentian history, the inference
is unavoidable that it is intended to represent the land at the
beginning of the Laurentian (Archean) time. It is hardly necessary
to say it is, again, approximately a map of earliest Paleozoic
(Primordial) times. Thus it has come to pass that many, without
reflection, have held that the development of the American continent
may be traced from a nucleus existing in Archean times. But of
this there is in fact not the slightest evidence.

On the other hand, Prof. Hull has recently published a very
interesting and suggestive paper ‘“‘On the Geological Age of the
North Atlantic Ocean,” + in which he tries to show that the places
of the present continents were not declared until the Mesozoic. If
this be so, then indeed the doctrine of the permanence of continents
must be given up entirely; for the Mesozoic and Cainozoic together
form but a small part of the entire history of the earth.

I believe that the truth lies between these extreme views.
I believe that the place of the American continent was established
and its nucleus formed at the beginning of the Primordial time ; and
that thus, in regard to the development of earth features, no less
than of earth faunas, the name Primordial is peculiarly appropriate.
This, I think, is the real view of Dana. I wish now to give
as clearly and as briefly as possible what seem to me the main
steps in the history of the American continent from the earliest times.

1. Of all rocks the Archzean are by far the most widely diffused
on the American continent, although of course largely covered by
later deposits. Not only do they form the surface rocks over large
areas, but they seem everywhere to underlie other rocks; for wher-
ever these latter have been pierced by wells or cut through by
caiions, we find the Archean beneath. It is hardly too much to say
that they form the foundation rocks of the whole continent. If so,
then, of course, in Archean times the American Continent was all sea-
bottom. Where was the land at that time ? We know not for certain ;
but the subsequent development of the continent southward and
westward suggests that its place was to the north-eastward. This
view is farther strengthened by the fact that the development of the
European continent south-westward would point to the north-west-
ward as the place of the earliest land. Prof. Hull therefore, with
much show of reason, assigns the North Atlantic as the place of the
Archean continent. The land from which such enormous masses of
sediments were derived must have been indeed of continental pro-
portions, and must have existed during immense periods of time,
perhaps equal to all subsequent times put together. Its débris
carried into south-eastward and south-westward seas formed the
Archean rocks of Europe and America.

2. At the end of the Archean, America (and probably Europe
also) became largely land. This is a point of very great importance,

1 Trans. Roy. Dub. Soc., 1885, vol. iii. p. 305.

Prof. J. Le Conte—Permanence of Continents, etc. 99

but not generally recognized. The evidence of this fact is found in
the eroded condition, universal so far as known, of the Archzan
rocks underlying all other rocks, even the lowest primordial. No
one has ever seen conformable relation between the Archean and any
other later rocks. Not only is this unconformity found all about the
border of the Canadian Archean area and the Appalachian area and
about all the smaller areas in the most widely separated parts of the
continent, but the grand Caiion of Colorado cuts through the whole
stratified series and into the Archean exposing the line of contact,
and we find the same unconformity ; the St. Louis Artesian pierces
the whole Paleozoic, and again from the sudden change in the
character and condition of the rocks from unmodified into metamor-
phic, we must conclude unconformity. But unconformity means
eroded land surface. Therefore we must conclude that well-nigh
the whole continent was land at the end of the Archean. It is
almost certain therefore that at the end of the Archean, there was
a veritable exchange of sea and land, and that the North Atlantic
Archzean continent became sea at that time. If so, the strata which
were then formed, and of which the eroded surface of Archean rocks
is the sign and measure, are now beneath the sea, and therefore irre-
coverably lost. This period between the Archean and the Primor-
dial I have elsewhere! called the ‘‘ Lost Interval,” because we have
no record of it in the stratified rocks.?, Judging by the amount of
erosion of Archean rocks, and also by the prodigious advance in the
progress of life when the record commences again in the Primordial,
this lost interval must have been a period of immense duration.
There are in the history of the earth many other intervals, partially
or locally lost, represented by local unconformities, the most im-
portant of which occurred at the end of the Paleozoic; but none of
these are to be compared with that which occurred at the end of the
Archean.

3. The Paleozoic commenced with another large crust-movement,
but not a complete interchange of sea and land as before. The
American continent was again largely, but not completely submerged.
It went down until only the now-known Archean areas, together
with an eastern area of unknown size now covered by the sea, were
left. The continent then consisted of a large V-shaped land-mass
corresponding to the well-known Canadian Archean area, a large
eastern land-mass, including the Appalachian Archean area, but
extending eastward at least as far as the submerged continental
border, and a large mass in the Rocky Mountains, and especially in
the Basin region, while a great interior continental sea occupied the
position of the drainage basin of the Mississippi river. The so-
called map of Archean land of Dana and Chamberlin would repre-
sent approximately the condition of things at this time, if the eastern
border-land were extended as far as the submerged continental

1 Am. Journ. Science, 1877, vol. xiv. p. 101. Le Conte’s Elem. of Geol. p. 291.
2 Some intermediate rocks have been found, e.g. the Kewenawan series, but the
gap is still immense,

100 = Prof. J. Le Conte—Permanence of Continents, ete.

border.! This, the Primordial continent, was the nucleus, from which,
by gradual growth, as so well shown by Dana, the American con-
tinent was formed. This growth was somewhat regular during the
Paleozoic, but with another large oscillation at its end. The
American continent existed, indeed, before, not however during the
Archean, as many seem to think, but during the “lost interval” ;
but it was almost destroyed at the beginning of the Paleozoic, to
recommence its development with the nucleus already described.
Thenceforward the plan thus outlined was apparently never lost.

4, During the Paleozoic the growth of the continent was com-
paratively regular, but at its end coincidently and correlatively
with the formation of the Appalachian Range, the eastern land-mass
was greatly diminished by submergence, and the eastern coast-line
advanced westward far beyond its present position, especially in the
southern part, probably as far as the well-known position of the
Tertiary coast-line. After this oscillation, the development was again
more regular, and in its broader outlines is well known. The great
interior Paleozoic sea was diminished and became the interior Cre-
taceous sea, and this later retreated southward, to become finally the
present Gulf of Mexico. There were probably many other times of
lesser oscillation. The last of these was in later Tertiary and early
Quaternary, during which the continent in its northern part again
extended to the submerged continental border, with probable con-
nection with Hurope in the North Atlantic region.

Prof. Hull, in his paper already referred to, makes the changes in the
latter part of the Palzeozoic and at its end much greater than I have
supposed, in fact equivalent to another almost complete exchange of
sea and land. According to him (see his map, fig. 3), during the
Carboniferous the whole of the North Atlantic and the northern
parts of North America and of Europe formed together an enormous
continental mass, the oceanic part of which was again submerged at
the end of this period, to nearly the present limits of the two con-
tinents. It is not impossible nor even improbable that during the
later Palaeozoic the American continent may have grown on its
eastern margin; or even that at some time during the long Paleozoic
era there may have been a connection far to the north between the
two continents ; but of the complete abolition of the Atlantic Ocean,
as shown on his map, I confess I see no sufficient evidence. The
great thickness of the Carboniferous strata would, it is true, require
a large land-mass to the east; but there is no reason why the eastern
land-mass, which sufficed to contribute the 30,000 feet of Silurian
and Devonian sediments, should not have been sufficient to con-
tribute the much smaller amount of sediments of the Carboniferous
period. ;

To re-capitulate briefly: 1. During the Archean the American
continent probably did not exist at all. 2. The first evidence we find

1 The Silurian continent has been thus extended by Prof. Hull in his map, fig. 2;
but why he has carried the northern part of the continental border westward so as to

cut through Labrador, I cannot imagine. The whole of Labrador was surely land in
Primordial times.

Sir J. W. Dawson—Rocks of Assouan on the Nile. 101

of its existence is during the “ Lost Interval.” It was then a large
land-mass of unknown size and shape, but evidently of continental
proportions. 3. At the beginning of the Paleozoic this continental
mass was nearly lost by submergence ; all that remained being the
well-known Archean areas, with a large extension on the eastern
margin of the present continent. The masses formed the nucleus
from which grew the present continent, with more regularity than
before, but with some very large oscillations, the greatest of which
was at the end of the Paleozoic, and the last of which was at the end
of the Tertiary and beginning of the Quaternary.

BERKELEY, CaLiForNiA, January 14th, 1886.

IJ].—Note on THE GerotoGgioaL ReLations oF Rocks From ASSOUAN
AND 17s NEIGHBOURHOOD.

By Sir J. Witt1am Dawson, C.M.G., LL.D., F.R.S.

R. BONNEY having been so kind as to examine microscopically
and describe a collection of crystalline rocks which I made
in the vicinity of Assouan on the Nile, I have prepared the following
notice of the geological conditions, to accompany his descriptions,
referring, however, to the notes on the locality given in my paper
in the GrotogicaL Macazine for Oct. 1884. Reference may also
be made to the paper of Lieut. Newbold in the Journal of the
Geological Society, vol. iv., and to that of Mr. Hawkshaw in the
same journal, vol. xxiii. Lartet has given in his Geology of Pales-
tine asummary of the observations of Russegger, Riviere and Figari
Bey on the crystalline rocks of the Nile, and the allied rocks of the
Sinaitic Peninsula have been described by him, by Bauerman? and
by Holland,? and more recently by Hull.* All these authors have
given, more or less distinctly, a series of gneisses and micaceous
and hornblendie schists associated with intrusive granites and
diorites as the oldest rocks of these districts, and succeeding these
in geological age, certain slates and associated rocks, with porphyry
and basanite in beds and veins.

The best section which I had an opportunity to examine of the
older series was near the town of Assouan, in a railway cutting
crossing the ridge between the river and the valley lying to the
east of the town, and which exposed the beds in a perfectly fresh
and unweathered state for about a quarter of a mile, beyond which
they were more or less imperfectly seen for about 800 yards, until
they were covered by the lower beds of the Nubian Sandstone un-
conformably superimposed on them.

I have given a section of the beds exposed in this cutting in the
paper above cited. They are nearly vertical with a strike N. 10° E.
As seen in the cutting, about four-fifths (Series A in Note) of the
thickness exposed consisted of schists with black mica and black
hornblende, the remainder being orthoclase gneiss regularly strati-
fied and numerous dykes of reddish hornblendic granite (Series B.
in Note). Further to the south the same rocks are seen to be

1 Quart. Journ, Geol. Soc. vol. xxy. ? Ord. Survey Sinai. 3 Mount Seir.

102. Sir J. W. Dawson—Rocks of Assouan on the Nile.

traversed by great dykes of diorite, and the mass or dyke of granite
which has been the most extensively quarried is situated to the north
along the course of the same ridge. Some of the crumbling schists
seen in the valley behind the town may have been calcareous, and
may be associated with limestone now concealed, but no limestone
was observed, though the character of the beds in comparison with
those I have elsewhere seen might lead to the expectation of its
occurrence in the vicinity.

The Nubian sandstone, where it rests on these rocks, has, in its
base, layers of conglomerate and of a calcareo-argillaceous indurated
marl, but holds no fossils. It may be of Cretaceous age, but I should
infer, from the character of the fossil wood (Araucariorylon
igyptiacum)' found in it elsewhere, and described by Schenk
in Zittel’s work on the Geology of the Nubian desert, that its lower
beds at least may be Permian or Carboniferous.

The lithological aspect of the beds seen in the cutting at Assouan
is that of the Middle or Grenville series of the Laurentian in
Canada; indeed I find on comparison that the greater part of the
rocks are not distinguishable in hand specimens from those occurring
in this series on the Ottawa River.

In the Island of Biggeh, above the cataract, and on the higher
parts of the mainland in its vicinity, there appears another formation
(Series C in Note), very different in its mineral character, which,
though older than the Nubian sandstone, I believe to rest uncon-
formably on the older Assouan Series. In Biggeh the latter is seen
in the lower part of the island in a vertical attitude and with strike
N. 10° W. Strikes ranging from about N. 10° W. to N. 10° EH.
appear to prevail in this series, in the vicinity of the cataract, though
in one place east of Assouan it was observed to be N. 70° H. Rising
above the lower series, and apparently resting upon it unconformably,
is a second series of beds nearly horizontal, and about 100 feet in
thickness. They are composed as follows in ascending order :—

(1) Hard dark-coloured quartzose porphyry, with crystals of red
orthoclase.

(2) Fine-grained granulite or granite, possibly a remanie rock.

(3) Black fine-grained laminated and in some places shaly rocks,
referred by Professor Bonney to quartziferous kersantite.

(4) Granulite, like No. 2.

(5) Dark-coloured porphyry, with dark crystalline paste, and large
crystals of opaque brick-red orthoclase.

The last is a very thick bed, and dividing along straight joints into
huge cubical blocks, gives a castellated appearance to the hill and
cliffs composed of this formation.

As seen from a distance, these rocks of the Second or Upper
Assouan series appeared to be intrusive masses; but on nearer
examination, they showed horizontal bedding, and at the base of the
cliffs and in their ravines were seen to rest on the older series.

Assuming on the evidence of mineral character the Lower Assouan
series to be Laurentian, and of Middle Laurentian age, the next

1 See W. Carruthers in Grou. Mac. 1870, Vol. VII. p. 306, Pl. XIV.

Prof. T. G. Bonney—Structure of the Rocks of Assouan. 103

rocks to be expected in ascending order would be the Upper Lauren-
tian or Norian and the Huronian. To the former the second Biggeh
series bears no resemblance, but there are known to be in the Arabian
chain, and probably associated with the equivalents of the Assouan
rocks, Norian rocks of the character of anorthosite gneiss, a rock
which was used by the ancient Egyptians for statuary,’ but is gene-
rally called diorite by antiquaries, though it differs very much from
the true diorites of the country.

Dr. Schweinfurth has sent me from the districts of the Arabian
chain north of Assouan, a rock similar to the more compact variety
of the dark Biggeh rock, which he states forms ridges parallel
to the main chain of crystalline rocks. Newbold refers to greenish
and chocolate-coloured schists and quartzite, as bordering the older
schists and granites, and Lartet notices talcose and chloritic slates
with granulite in a similar relation, crowned by the celebrated green
conglomerate and breccia of Kosseir and Gebel Doukhan. Further,
Russegger connects the red porphyry and petrosilex porphyry with
large felspar crystals of Gebel Doukhan with this second series, and
Lartet has described the quartziferous porphyry of Mount Hor as
lapping around the granite nucleus of that mountain.

It would thus appear that the old Laurentian gneisses and schists
of Upper Egypt and its eastern mountain chain are succeeded by
formations which may be held to represent the Norian and Huronian
series at least, and I would regard the Biggeh formation or Second
Assouan series as consisting mainly of bedded volcanic material
representing some portion of the Huronian, a formation which would
seem to have been more largely developed or to be better preserved
in some parts of the Arabian chain to the north and east, where it is
also overlain by slaty rocks, and by the green conglomerate which
either constitute an Upper Huronian series, or may represent the
Ammiké and Kewenian formations of America. There would seem
in this district to bea great geological hiatus between these old rocks
and the Nubian Sandstones.

I1I.—Nore on tHe Microscoric StructuRE OF somME Rocks FROM
THE NEIGHBOURHOOD OF ASSOUAN, COLLECTED BY Sir J. W. Dawson.

By Prof. T. G. Bonnuy, D.Sc., LL.D., F.R.S.

HAVE not deemed it necessary to examine microscopically the
whole of the collection made by Sir J. W. Dawson, but have
selected a series of fairly representative specimens, sufficient, I think,
to give a general idea of the principal varieties. For purposes of
identification I leave the reference numbers borne by the specimens,
though their sequence is accidental.

(A.) OLDER Gwetssic Series, ASsouAN.
(3.) A moderately fine-grained holocrystalline pink and white
rock, speckled with black, of slightly gneissic aspect.
Microsc.—Quartz, felspar, orthoclase with some microcline and
plagioclase, biotite, occasionally showing signs of alteration to the

1 The fine statue of Kaphra or Cephren in the Boulak Museum is of this stone.

104 Prof. T. G. Bonney—Structure of the Rocks of Assouan.

usual green mineral, a little apatite, and a small yellowish mineral
probably sphene. The rather irregular outline of the felspars and
the granular aggregation of the quartz resembles in some respects
the structure of a gneiss rather than a granite, but it is very probable
that this structure is the result of some pressure and crushing after
the consolidation of the rock, of which the hand specimen gives
indication: in all other respects one would not hesitate to call it
a granite.

(4.) A rather fine-grained holocrystalline rock, speckled pinkish
and dark coloured.

Microse.—Quartz, felspar (orthoclase, microcline, and plagioclase),
with a considerable amount of brown mica, a little apatite and
epidote or sphene, with a very little iron peroxide. It is extremely
difficult to say whether this be a gneiss or a granite crystallizing
after the vein granite type (granulite of Fouqué and Lévy), modified
slightly by subsequent pressure. After all, perhaps, some of the very
coarse ancient gneisses may be only crushed and recemented granites.

(5.) A rather fine-grained holocrystalline rock, speckled pinkish
and dull green; general tint inclining to dark.

Microse.—The remarks on (4) will apply here, except that there
is rather more biotite and apatite. The structure also is more
gneissic, but it is very doubtful from indications given by the slide
whether we can trust this, and whether the rock may not originally
have been a granite.

(7.) A dark erystalline hornblendic rock, with a slightly fissile
structure.

Microse.—Holocrystalline ; hornblende and felspar (chiefly plagio-
clase), a little epidote (probably) and magnetite, a flake or two of
biotite, and a very little apatite. Very difficult to decide upon the
origin of this rock. I incline to think it igneous, and a diorite.

(8.) A rather dark grey and pink, somewhat finely crystalline rock,
with fairly distinct foliation.

Microse.—Quartz, felspar,—orthoclase, a little microcline, plagio-
clase (? albite),—biotite, with a little iron peroxide, and a very little
apatite. The structure much resembles that of one of the old
Laurentian gneisses, which is also in accordance with the macro-
scopic aspect of the rock.

(11.) A gneiss distinctly streaked with pinkish felspathic and dark
hornblendic or micaceous bands; the former, with occasional rounded
felspars, have an aspect suggestive of much crushing. This
appearance is fully confirmed by microscopic examination. The rock
has evidently been once either a hornblendic granite or a granitoid
gneiss, and its present structure is due to great crushing, so that in
parts it is like an ordinary fragmental arkose. The dark mineral
appears to be chiefly hornblende, though much biotite is also present ;
its crystalline grains are mostly small. Orthoclase, microcline and
plagioclase were probably among the felspars of the original rock.
There is some apatite, also sphene (?), ilmenite (?), and a crystal
of a dark brown mineral unknown to me.

(12.) A very dark distinctly foliated schist, composed chiefly of

Prof. T. G. Bonney—Structure of the Rocks of Assouan. 105

mica and a decomposed (?) felspathic mineral ; some of the mica has
a brassy lustre. The attempt to obtain a slice of this rock has been
a failure, as it is so friable.

(13.) A hard quartzose schist, with not much mica, and little
signs of foliation.

Microse.—The principal constituents are quartz, felspars of more
than one species, and brown mica. The rock appears to have been
squeezed, but not crushed. It has the aspect of a true gneiss, one of
the fine-grained kinds that rather resemble quartzites.

(14.) Rather like (12), but with a felspathic vein.

Microse.—Dominant minerals, plagioclase, biotite, hornblende,
some quartz, but variable in distribution. Parts of the slide might
thus be called hornblendic gneiss, the rest rather hornblendic mica-
schist. The rock certainly must now be called one of the above
names, but there are peculiarities in its structure which prevent me
from making any confident statement as to its origin.

(15.) A rather ‘slaty’ fine-grained gneiss, related to (13), but
more fissile.

Microse.—It has a general similarity to (13), but contains more
mica. Also it has yielded more to pressure.

I may add that among the specimens from this series are several
rather fine-grained dark mica-schists or very micaceous gneisses,
varying between (12) and (15), which are so obviously representatives
of the ‘‘ metamorphic” group of rocks, that I have thought it needless
to examine them under the microscope. They have a general re-
semblance to schists not unfrequent in the upper parts of the Hebridean
series of Scotland, and may be compared with some of those which
occur (for example) in the neighbourhood of Gairloch (Ross).

(B.) Rocks Intrustve (Dyxes, Erc.) tN Serres A.

(1.) A holocrystalline rock, mottled dark green (almost black) and
light yellowish, with porphyritic felspar crystals of latter colour,
sometimes about one inch long.

Microse.— Consists of quartz, felspar—orthoclase, microcline, plagio-
clase (albite ?)—hornblende, biotite; with a little magnetite, a good
deal of apatite in well-defined hexagonal prisms, and a little of a
granular yellowish mineral, probably sphene. Thus the rock is
a hornblendic-granite ; it is not very rich in quartz.

(2.) Coarsely crystalline rock, with large pinkish-red felspar
erystals, quartz, some whitish felspar and black mica. One of the
granites commonly used in Egyptian monuments, and, as is often the
case with these, it has a gneissoid aspect.

Microse.—Holocrystalline ; quartz felspar, chiefly microcline, with
some plagioclase, brown mica, with a little hornblende, a little mag-
netite, some apatite, and a yellowish mineral ; sphene, or perhaps
epidote. The irregular outline of the felspar and the aggregated
granules of quartz resemble a gneiss, but this may be due to subse-
quent crushing.

(6.) A holocrystalline rock, moderately coarse, speckled with light
greyish colour and black (mica).

106 Prof. T. G. Bonney—Structure of the Rocks of Assouan.

Microse.—Quartz, felspar (orthoclase, microcline, and plagioclase),
a good deal of biotite and hornblende, rather rich in apatite, some
magnetite, some sphene (one crystal rather large), also several long
colourless needles, ? sillimanite ; a hornblendic granite, rather poor
in quartz.

(C.) Upper Series at Braces (Assovay).

(9.) A dark rather compact rock, with but slight indication of a
schistose structure.

Microse. —Holocrystalline ; quartz, felspar (apparently both ortho-
clase and plagioclase, but not very well characterized), biotite and
hornblende, with a little magnetite, apatite, and sphene. It resembles
a hornblende schist, but slightly foliated, rather than an igneous rock.

(10.) A dark rather compact massive rock with rectangular
jointing.

Microse.—Holocrystalline, but not coarse, composed of biotite,
rather dark-coloured, but partly altered into a greenish mineral, and
hornblende with some quartz, and a fair amount of felspar, which
seems commonly to be plagioclase; a little apatite, magnetite or
hematite, and sphene. The mica (with perhaps the hornblende)
appears to have been the first mineral to crystallize. The rock
appears to me to belong to the mica-trap group, and to be a quartz-
iferous kersantite.

(16.) A dark rather fissile rock, looking more like a bad slate
than a true schist.

Microse.—At first glance it seems very fragmental, but on careful
examination I feel convinced that we are dealing with a crushed
crystalline rock, which has consisted chiefly of felspar and horn-
blende. There is a fair amount of apatite, and some of the hexagonal
crystals appear to have escaped the crushing, or have been sub-
sequently formed. I notice a few flakes of brown mica and there
are indications of iron oxides. Thus it is now a schistose rock,
not of a highly metamorphic aspect, but has been made out of a
diorite or a hornblende schist.

The “coarse dark-coloured porphyritic rock” from this series
(No. 1 of Sir J. W. Dawson’s series at page 440 of the volume of
this Macazine for 1884), if I have rightly identified the specimen,
is holocrystalline and it appears to me to be a true granite. I may
add in regard to this “upper series” that, if I am right in my
interpretation of (16), the specimens do not suggest to me the
necessary existence of a wide gap between them and those of the
lower series; that some appear to me igneous rocks, and that the
others, if not igneous, belong to a highly crystalline group of rocks.

REMARKS.

I have had to speak with some hesitation as to the nature of certain
of the above described rocks. This is always needful in dealing
with any series of very old rocks, especially when one has not had
the opportunity of examining them in the field, because we are not
yet sure of the significance of certain structures and their relation to

R. F. Tomes—Liassic Madreporaria. 107

the origin of the rock. But while I cannot positively assert that
some of the rocks included in series A (Older Gneissic Group) may
not be rocks of igneous origin, to which a schistose structure has
been imparted by subsequent pressure, I think it highly probable
that they assumed their present character at a very remote period in
the world’s history, and may remark that this difficulty is one which
frequently confronts us in examining the older Archean series. But,
while admitting this uncertainty, I observe in some of the specimens
the structures which I have been accustomed to note as characteristic
of the older gneisses, and was independently struck with the resem-
blance which some of them presented to specimens collected by
myself in Canada and in N.W. Scotland, especially in the case of
(18), which is very like to a “ quartzose gneiss,” high in the Grenville
series, shown to me by Sir W. Dawson in 1884, near Papineauville
Station on the Ottawa river. Thus the series as a whole may safely
be regarded as petrologically “‘homotaxial” with the middle part of
the Canadian Laurentians.

ITV.—On tHe Occurrence or Two Species oF MADREPORARIA IN
THE Urrrer Lias oF GLOUCESTERSHIRE.
By Rozert F. Tomss, F.G.S.

HE few recorded Madreporaria of the Upper Lias possess con-
siderable interest on account of the great generic as well as
specific differences which exist between them and those from the
Middle and Lower Lias, though it might seem probable that the dis-
covery of a greater number of species would diminish that dis-
crepancy. Such a conclusion has not, however, by any means been
substantiated by further acquaintance with those from the Upper
Lias of the district of which I am about to speak.

The late Mr. Charles Moore in his exhaustive paper, “‘On the
Middle and Upper Lias of the South-West of Hngland,”? gives
sections of the Upper Lias exposed in quarries on the hills at Stanley
and Dumbleton. Both these places are in the eastern part of
Gloucestershire, and a reference to the paper above quoted will show
that the sections there very closely resemble each other. The quarry
on Stanley hill is now closed, but a waste heap yet remains, on the
upper surface of which are numerous little hillocks of weathered
clay and shale. They represent the barrow loads of clay from near
the bottom of the quarry, which have been wheeled out by quarry-
men preparatory to lifting the Middle Lias Marlstone below. The
influence of weather having first reduced these hillocks to a light
blue or grey mud, and afterwards dried them into the consistency of
ashes, a considerable number of small lenticular corals were found
on their surface, and many were collected during the summer of 1885
by my friend Mr. T. J. Slatter, and myself. Belemnites occurred in
great abundance, as well as small Ammonites (probably Ammonites
Hollandrei), but although in near association with the corals, they
were not found mixed together. In much nearer approximation were

1 Proceed. Somerset Arch. and Nat. Hist. Soc. vol. xiii.

108 RL. F. Tomes—Liassic Madreporaria.

numerous small glittering crystals of pyrites, small Gasteropoda,
fragments of Pentacrinites, and Acrosalenias.

With a view to determine, if possible, the precise stratigraphical
position of the corals, I visited the Dumbleton hill quarry, only three
miles distant, still in work, and satisfactorily determined their horizon.

The following i is an accurately measured section, showing the beds
at present exposed : —

ft. in.

L.. Sunface Oils. .cssienwaate de axemmyhnensducbeseokeabesbaeeisie sf akve Baba ciatates 4 0
2. Fish bed, fine-grained and laminated stone, with Saurian remains,

Leptulepis concentrocus, and insects ..........sesesseceeernsceneennce 1 0
3.) Waminatedubliershallesme: sar ese ee res cgeeeene ce) nate ete eentane Heb AD
4, Layer of intermittent nodules of hard atone ‘containing fucoids ...... 0 3
5. Laminated blue shale, like No. 3.................. 3 0
6. Whitish grey clay, hard and breaking up into angular lumps, ‘and

weathering into a soft light- coloured CLAY ite ccaetancae ten anancre 0 9
7. Hard light blue shale, in the lower part of which are many Belemnites,

and in the upper part numerous small cubes of pyrites, small
Ammonites (4A. Hollandrec) and Gasteropods ................00006 1 3
8. Friable shale, having the appearance of soft marlstone, brown or

ferruginous i in colour, and sometimes Micaceous ..........0. se 1 0
9. Middle Lias Marlstone) very tossilitterOusigh..meccreressresetradeee-remsiese 3 (0
28 3

All the beds downwards, until we arrive at No. 6, are finely
laminated, and it would be time wasted to seek for corals in them.
However beds 6 and 7 are wholly different. The first of these,
No. 6, is light-coloured and hard, breaking up with the hammer into
more or less square or angular lumps. It appears to contain very
few fossils. No. 7, like the one above it, is not laminated, but is
bluer, softer, and much more fossiliferous. Near to the bottom of
it are Belemnites in abundance, and it also contains a great many
small specimens of Ammonites Hollandret. Very near to, or at the
top, are a great number of crystals of pyrites, similar to those at the
Stanley hill quarry. These two beds weather down into a soapy and
disagreeable mud, and this perhaps accounts for their having been
wheeled well back on to the top of the waste heap out of the way,
both at Stanley and Dumbleton. The corals are much less common
at the latter than at the former place, only two specimens having
been met with. Both were in close proximity to the layer of pyrites,
and in the top part of bed No. 7, or in the division between that bed
and No. 6. At Stanley hill, where the corals are plentiful, they
were found either in association with the pyritic crystals, or in a
lighter coloured mottled clay, such as would be caused by the
weathering down and mixture of beds Nos. 6 and 7. The conclusion
at which I arrived, after making examination, was, that they lie
chiefly between the two above-mentioned beds, and that they denote
a quiet period during the deposition of the transition beds from the
Middle to the Upper Lias. This is also the position of the peculiar
so-called Montlivaltia which occurs in the transition beds from the
Middle to the Upper Lias at Adderbury and Chipping Warden,
Oxfordshire, to which I gave the name of Montlivaltia tuberculata.

Bed No. 8 is, without doubt, the top of the Middle Lias, dif-

R. F. Tomes—Liassic Madreporaria. 109

fering only from the Marlstone beneath in being less compact.
As I have already stated, the late Mr. Moore gave sections of the
Upper Lias exposed in the quarries on the hills at Stanley and
Dumbleton, areference to which will show that the two sections
very closely resemble each other.

In the paper alluded to is also a detailed section of the Upper
Lias at Ilminster, from which Mr. Moore obtained the corals figured
by MM. Milne Edwards and Haime, under the names of Thecocya-
thus Mooreit, and Trochocyathus primus. A comparison of the
Ilminster section with the one here given of the Upper Lias at
Dumbleton hill will show that the corals from the latter place and
from Stanley hill occupy a very different place in the section to the
species just mentioned; but they, as already observed, correspond
stratigraphically with those from Adderbury and Chipping Warden,
and one of the species, as J shall show, is the same.

Two species, representing two genera, were collected at Stanley
hill, namely Thecocyathus and Trochocyathus.

THECOCYATHUS TUBERCULATUS, Tomes.
Montlivaltia 2 tuberculata, Tomes, Quart. Journ. Geol. Soc., vol. xxxiy. p. 192,
1878 (read 1877).

The greater number of the specimens collected at Stanley hill are
referable to the species which I have erroneously, but with an
expression of doubt, described as a Montlivaltia, under the name of
Montlivaltia ? tuberculata. Their state of preservation being very
superior to that of the Oxfordshire specimens, from which I took my
description, I am now enabled to amend it very considerably, and to
place the species in another genus.

All the Stanley hill specimens are rather smaller than the ones
from Adderbury or Chipping Warden. The general form of the
corallum is similar in the specimens from all these localities,
and the calice of those most satisfactorily preserved is superficial,
and varies from a slight convexity to a slight concavity. There are
three complete cycles of septa and a rudimentary fourth. Those of
the first pass quite into the columella, and those of the second
approach it very nearly. The septa of the third cycle are two-thirds
the length of those of the second. Those of the first and second
cycles have their outer half crenulated rather than tuberculated,
while their inner half has strongly marked paliform tubercles,
which are four in number on the primary septa, and three on the
secondary ones. Sometimes there is a single paliform tubercle on
the septa of the third cycle, but this does not seem to be a constant
character, and its appearance is perhaps regulated by the age of the
individual. In some specimens these tubercles are much more
prominent than in others, but all in the same calice have an equal
prominence and are equal in size. The columella has very little
prominence; it is small, porous, and irregular, and the tubercles on
its upper surface correspond with those on the septa from which, in
the unworn calice, they are undistinguishable. The appearance
presented by the most perfect examples is that of a central area
filled with equal, round, and equally prominent tubercles ; but when

110 R. F. Tomes—Liassic Madreporaria.

the calice is rubbed or worn down, these all disappear, and the
simple septa are seen to pass quite up to the columella. The sides of all
the septa have rather distant but well defined and prominent tubercles.

Compared with Thecocyathus mactra, the present species differs
in its smaller size, its much more rugose epitheca, and in its pali,
the margins of which are much more tubercular. The tubercles
are undistinguishable from those of the columella, with which they
appear to blend.

I may take this opportunity of observing that with access to a
considerable collection of specimens of Thecocyathus mactra, and
Thecocyathus tintinnabulum, as well as to a number of species of
Thecocyathus Moorei from the Upper Lias of Ilminster, Iam not only
satisfied of the distinctness of the species from the Upper Lias of
Gloucestershire and Oxfordshire from the others, but am fully pre-
pared to follow M. de Fromentel in putting together as one species
Thecocyathus mactra and Thecocyathus tintinnabulum.

I also avail myself of the present occasion to make a few remarks
on the genus Thecocyathus. Amongst the most ancient of the
Turbinolida, this genus might not unnaturally be expected to possess
characters approximating it in a greater or less degree to the Lower
Mesozoic Astreide, with which in time it is so nearly associated.
None of the Turbinolide have to my knowlege been met with in the
Lower or Middie Lias, but I may observe that although the Mont-
livaltia radiata, of Duncan, which occurs in the bottom of the Middle
Lias, or perhaps at the junction of the Middle with the Lower Lias,
has an abnormal and primitive number of primary septa, it never-
theless has a very thin epitheca scarcely obscuring the costae,
which is quite unlike that of any genus or species of older date.

Again, the sides of the septa of Montlivaltia mucronata, which is
found associated with the last species, are ornamented with thickly
crowded flattened tubercles, instead of the vertical ridges which
characterize nearly all the Jurassic Montlivaltig. These peculiarities
seem to indicate some affinity in both these species with more recent
forms.

In Thecocyathus tuberculatus we have a very modified development
of the inner ends of the principal septa, which is no doubt equivalent
to the growth of pali, and the same sort of development takes place
to a considerable though more limited extent in Thecocyathus Moorei,
for I observe that when the calice is ground or worn down, the pali
are with difficulty traceable. Some of the much worn specimens are
undistinguishable from Montlivaltig, having columellze formed by
the fusion of the septa in the centre of the visceral cavity. The genus
Thecocyathus must therefore, I think, he regarded as very sub-typical
of the Turbinolide—the precursor, in fact, of the more typical genera.

Nearly allied to Thecocyathus is Trochocyathus, but unlike the
former, which continued into the period of the Lower Oolite and
no longer,’ the latter lived on through the Secondary and into

1 I limit my remarks to such species of Thecocyathus as have been met with in

this country, one of which has been obtained from the Inferior Oolite of Dorsetshire.
M. de Fromentel describes four as occurring in the French Oolites.

W. Whitaker— Water Supply from Wells. 111

Tertiary times. Trochocyathus primus, which has been found
associated with Thecocyathus Mooret high up in the Upper Lias
of Somerset, is a very doubtful form, and the same may be said
of the still earlier species spoken of in the present paper. But in
Trochocyathus magnevillianus we have proof of the occurrence of an
unquestionable and more typical Turbinolian in the Inferior Oolite.
Of its precise position there I am unable to speak, but have great
reason for supposing that it is only a little removed from the Cepha-
lopod bed of the Upper Lias.

TROCHOCYATHUS,

With the preceding species occurs another coral which I refer to
the genus Zrochocyathus. All the specimens, which, however are few
in number, are small in size and broadly attached, and in this
respect are more like examples of the genus Paracyathus than
Trochocyathus. They are wholly destitute of epitheca, and their
mural costz are well defined and have transverse crenulations. The
calice is ovoid, convex, and consists in all the specimens I have
examined of a confused mass of tubercles, which are more distinct
towards the centre than outwardly. Neither the cycles of the septa,
nor the pali can be satisfactorily traced.

Height of the corallum, 1 line. Greatest diameter of the calice,
14 line.

V.—On a Recent Leeat Decision, oF ImporTANCE IN CONNECTION
with Watrer Suppty From WELLs.!

By W. Wuriraxksr, B.A., F.G.S., Assoc. Inst. C.E.

BOUT, or nearly, forty years ago, two deep wells (with borings)

were made at Brentford, which, passing through Gravel, London

Clay, and the Lower London Tertiaries, reached the Chalk at a
depth of about 315 feet, and were carried some way into the last.

One of these wells is at the Brewery on the southern side of the
High Street, now known as the Royal Brewery, and it continued in
use till its water became unfit for brewing-purposes, from the cause
noted below. The other is 99 yards off, north-eastward, at some
printing-works at the back of the houses on the other side of the
street. This one was made for a Distillery which has long ceased
to exist; the well too having been abandoned, at least for its original
purpose of water-supply.

Unfortunately, however, some years ago (from 1874 to 1882) the
Distillery well, as we may call it, was turned to a baser use, being
made into a cess-pit, by turning into it the drainage of the privy
belonging to the printing-works. This misuse has ceased for some
three years ; but not before a considerable deposit had been formed
in the well.

The water of the Brewery well, once of good quality, having
been found to have become gradually contaminated, the owner, Mr.
M. Ballard, sought to discover the cause, and, the misuse of the

' Read before the Congress of the Sanitary Institute of Great Britain, at Leicester,
Sept. 25, 1885. Extracted from vol. vii. of the ‘Transactions of that Institute.

112 W. Whitaker— Water Supply from Wells.

Distillery well having come to his ears, he was led to attribute to
that the falling off in quality of his own well-water, the use of
which was at once discontinued.

This led to his bringing an action against the owner of the
Distillery well, Mr. Tomlinson, for heavy damages, and, although
the misuse of that well was then stopped, of course its effects on the
water of the Brewery well did not cease, and were not likely to for
some time. Having, in the course of the proceedings, been consulted
on the Plaintiff’s behalf, I may be allowed to call public attention
to the importance of the question at issue.

That the two wells get their water from one common source, the
Chalk (and perhaps, to some extent, from the overlying sands), is
incontestable. When no pumping goes on at either, the water-level
is the same at both, about 27 ft. down in the Brewery well, and 37 ft.
in the other, the site of which is some 10 ft. higher.

Practical evidence, however, of the communication between the
two was given by the Brewery well being pumped for 48 consecutive
hours, whereby its water-level was lowered 78 ft. 9in., and that of
the Distillery well 14 ft. In order, moreover, to make assurance
doubly sure, the lithium-test was applied at the suggestion of Dr.
Frankland, and some of the lithium-chloride put into the Distillery
Well was found to have been drawn to the Brewery well 48 hours
afterwards. a

The question, therefore, of communication between the two wells
could not be disputed; it was clearly a fact, and the Defendant’s
case was based on purely legal points, which amounted practically
to the statement that any man could do as he liked with his own
well, a contention which was successful at the trial before Mr.
Justice Pearson, in February, 1884.

The judge ruled that, as it had been decided in the well-
known case of Chasemore v. Richards, no one had a right to under-
ground water so far as quantity is concerned, or in other words that
neither Plaintiff nor Defendant could be restrained from pumping
each other’s wells dry, or from carrying out works that might take
away each other’s supply, so also there was no right in quality ;
but that the Plaintiff, whilst having a perfect right to pump as much
water as he liked, so as to draw away water from the Defendant’s
well, must take that water subject to everything that has occurred
to it. If he did not pump up the water from his own well, he
would not get the bad water from the neighbourhood of the
Defendant’s well. I must own that to my unlegal mind the idea of
having a well without pumping water from it was somewhat
amusing, and I was inclined to infer that if it had been a case of an
overflowing well, from which the water was delivered by the natural
force of gravity, instead of by the artificial force of a pump, the
decision might have been different, though why I do not see.

Tn his decision the judge seems to have been somewhat influenced
by the possibility that, if the law were otherwise, actions might
ensue for like pollutions at great distances, instead of the trifle of 100
yards as in this case, and, in his judgment, he imagines a series of

W. Whitaker— Water Supply from Wells. 113

litigants spreading the grounds for such an action over a distance of
60 miles. Though to a lawyer this may seem an inconvenient
prospect, I think that sanitarians may be inclined to look on it with
no disfavour.

The result of such a judgment amounts of course to saying that
no underground water-supply is safe from contamination, even if
wilfully brought about. Should your neighbour have a well with
a good supply, and you wish to spite him, or to spoil his business,
all that is needful would be to put down a bore to the source of
supply, and to pour some poison down it! This matter, I believe,
was noticed by one of the Plaintiff's counsel. Perhaps, however, in
in such a case, or in one where sewage containing typhoid, or chole-
raic, evacuations was knowingly poured into a well, so as to foul
a neighbouring one, the offender might be convicted of manslaughter,
in a criminal case, thongh (under Mr. Justice Pearson’s judgment)
he would get the best of a merely civil action! This would certainly
be a somewhat anomalous state of things, even as regards English
law!

So many towns, institutions, and manufactories now get their
water-supply by wells in the Chalk, and in other great water-bearing
beds, that the result of such a judgment passing unchallenged would
have been most serious. It would possibly indeed have been a great
check to enterprise in that direction, as water thus got, perhaps at
great expense, might at any time be made worse than that got from
streams which are more or less contaminated.

The Plaintiff, however, was advised to take the case to the Court
of Appeal, and all folk interested in the getting of pure water should
thank the Master of the Rolls, and the Lords Justices Cotton and
Lindley, for unanimously over-ruling the judgment of the Court
below, as they did in February, 1885.

The Master of the Rolls holds that “although nobody has any
property in the common reservoir or source [of underground water ],
yet everybody has a right to appropriate it in its natural state, and
no one of those who have a right to appropriate it has a right
to contaminate that natural source so as to prevent his neighbour
from having the full value of his right of appropriation ;” and he
goes on to say, in answer to an objection that the water is got by
artificial means (pumping), that ‘however ke [the Plaintiff] may
appropriate the water from the common source, he has a right to
have that common source uncontaminated by any act of any other
person.” With regard too, to the question of distance, his judgment
is equally satisfactory; for he says that ‘the question does not
depend upon the parties being what is called contiguous neighbours.
If it can be shown in fact that the Defendant has. ... fouled...
the common source, it signifies not how far the Plaintiff is from him.”

Lord Justice Cotton draws attention to the fact that the Defendant
was not using the water from his well, but only putting filth down
the well, which does not amount to using a natural right, and by so
doing, he “‘interferes with the exercise by the Plaintiff of a natural
tight incident to the ownership of his own land.”

DECADE I1J.—yOL. I1.—NO. II, 8

114. Dr. H. Woodward—Recent and Fossil Hippopotami.

Lord Justice Lindley remarks that the case “really involves the
question whether a person who has a well on his own land is at
liberty to poison the water which supplies that well and a large
district round about it. The defendant says he has such a right.
It is a startling proposition to say the least of it.” He adds that
“the right to foul water is not the same as the right to getit.....
Prima facie no man has a right to use his own land in such a way
as to be a nuisance to his neighbour..... If a man chooses to
poison his own well, he must take care not to poison waters which
other persons have a right to use as much as himself... . . The
right of a man to get water from his well is to get the water as
nature supplies it.” |

As a geologist, much interested in the question of water-supply
from underground sources, it was with a feeling of great relief that
I heard of the view of this case taken by the Court of Appeal, and
I read the full report of the judgments (from which the above
quotations have been made) with much pleasure. I am inclined to
think, indeed, that Mr. Justice Pearson, albeit he seems to hold
strongly to the opinion that this is a free country, may feel relieved
rather than grieved at the reversal of his decision. Had it been
upheld, there would clearly have been great need of a little law-
making.

Although all sanitarians must be glad of the final decision in this
case,—for it will not be carried to the House of Lords,—yet it seems
unfortunate that the privilege of bringing up so important a matter
for settlement should have fallen to individuals instead of to corpora-
tions or to companies, on whom the expense would have more
fairly fallen. It may be but a poor consolation to both Plaintiff
and Defendant, that their names will become famous, like those of
Chasemore and Richards, from the case of Ballard v. Tomlinson
being one that is likely to be quoted for many years, as giving a
most important decision in the law of water-supply from wells.

Whilst it was decided, in the earlier case, that every owner has
the right to draw underground water to an unlimited extent, the
decision now noticed is to the effect that no owner has the right to
pollute a source of water-supply common to his own and other wells.
Whatever may be the fate of the former decision, it is to be hoped
that the latter one will never be altered.

VI. —Recent anp Fossit Hrerorotamt.
By Henry Woopwarp, LL.D., F.R.8., F.G.8., ete.
(PLATE III.)

N September last, I drew the attention of the readers of the Gro-
LogicaAL Macazrne (Decade III. Vol. II. pp. 412-425) to a singular
group of vegetable-feeding aquatic animals, the SirEn1A, represented
at the present day by two genera, Manatus and Halicore, and by at
most six species, three or four of which are probably only varieties.
A peculiarity of this group of animals is that whereas the two living
genera are distributed in the subtropical regions Hast and West of

Grou. Mac. 1886. DEcADE III. Vou. III. Pu. III.

A

>

2 ms “ .
AL
uM m ))))

ae

GH; t)
4, Mf Z
Ra MM

SG

Fics. 1, 2. Hippopotamus amphibius, Linn. (recent).
9» «3-5. Ae stvalensis, Fale. & Caut. (fossil).

Mae yin By Se nae od

Rist aR AE BAe

ree (uinatowee ji
; fh ies veel ase

wai saith st i uy saute
en Ae ae ie j

Dr. H. Woodward—Recent and Fossil Hippopotami. 115

the African continent, and to its rivers and opposite coasts, the
ancestors of the Halicore and Manatee (the Halitherium, Felsino-
therium, and some ten other fossil genera of Sirenians) probably inter-
mingled and extended 30° further north than at present from the West
Indies and Carolina through England, Belgium, France, Germany,
Italy, and North Africa, whilst Rhytina, the largest of them all, only
became extinct 100 years ago on the shores of Behring’s Island,
Kamtchatka. The evidence which the fossil remains of S1RENIA
afford of a more northerly geographical extension of subtropical
mammalia in Tertiary times, is abundantly confirmed by other
genera, to one of which only, the Hippopotamus, I will here refer.

It has always seemed at first an anomalous circumstance to find
the remains of the Hippopotamus and the Reindeer in the same
Tertiary deposits, the latter belonging to the extreme northern
lands of Europe, Asia, and North America, and the former to Central
Africa; but in late Tertiary and early Prehistoric times, when our
island formed a part of the mainland of Europe, the migratory
herds of Reindeer not only reached this country in winter, but
advanced as far south as into France and Spain; whilst the rivers of
Italy, France and England were all the summer, if not the winter,
the resort of the Hippopotamus, which has left its remains as far
north as Leeds and Kirkdale in Yorkshire.

Jt was formerly customary to refer the numerous remains of the
large species of Hippopotamus found fossil in this country, in France,
and in Italy, to the H. mayor, of Owen (1843), or to the H. antiquus,
of Desmarest (1822) ; but the researches of Prof. Boyd Dawkins have
led to the conclusion that they all undoubtedly belong to the living
African Hippopotamus, H. amphibius of Linneeus (1766).

Like the “Manatee,” the Hippopotami, where undisturbed, fre-
quent with equal pleasure the coast, as they do the rivers. North
of Port Natal they are said not only to abound in the rivers, but upon
the sea-shore, retreating to the sea when disturbed or attacked.

Such evidence as this enables us to understand the presence, in
prehistoric times, of the Hippopotamus in Britain, at least during the
summer season, even after its partial isolation from the continent.

Its remains have been found at Kirkstall, near Leeds; in the
Norfolk Forest-Bed-series at Bacton, and Hasbro’; at Lavenham in
Suffolk ; at Barnwell, near Cambridge; at Chelmsford, Cold Higham,
Grays, and Walton, in Essex ; in the Valley of the Ouse at Bedford ;
at Greenwich, Kent; Peckham, Surrey ; in Camden Town, in fact,
very generally in the Thames Valley : often associated with remains
of Reindeer, Rhinoceros, and Mammoth.

Hippopotamus-bones are less frequently found in caves, than in
river-valley deposits; but in several their remains are recorded,
associated with those of the Reindeer, namely :—Pont Newydd near
St. Asaph, N. Wales; Kirkdale Cave, Yorkshire; Gower Caves,
Glamorganshire; Cefn Cave; Settle Cave; and Durdham Down
Caves. :

An interesting and abundant find of Hippopotamus-remains was
recently obtained at Barrington, near Cambridge (noticed by Mr. P.

116) Dr. H. Woodward—Recent and Fossil Hippopotami.

Lake, Grou. Mac. 1885, pp. 3818-320. The geology of the locality
and its superficial deposits have been very accurately described by the
Rev. O. Fisher, M.A., F.G.S., see Quart Journ. Geol. Soc., 1879,
vol. xxxv. pp. 670—677.)

Of the European localities three may be specially noticed as
yielding remains of Hippopotamus amphibius in considerable numbers,
namely, at Perrier and Puy de Dome in France, and in the Val
d’Arno in Tuscany.

I have argued from the presence of remains of SrreniA so
widely distributed in the European Tertiaries a generally warmer
climate, and I am glad to find that the late Dr. Falconer adopted
the same view from the fact of the presence of remains of Hippo-
potami in so many English localities. This accomplished naturalist
thus sums up his views:—‘‘Jn speculating about the probable
climatal conditions on the land in Europe during the Pliocene
period, one of the fossil pachyderms has appeared to me capable
of throwing more light than all the others, namely, Hippopota-
mus major. ‘Two living species of this genus are known, the
one Hippopotamus amphibius, and the other the small Hippopotamus
Liberiensis. They are both found in the tropical or warmer parts
of Africa. In their habits they are strictly aquatic, plunging into
rivers during the day, and emerging at night to pasture along
the river banks. They always hug the margins of the rivers
or lakes, and are not known to make inland journeys away from
them. When they migrate, they either float with the stream, or, if
moving against it, they walk along the bed of the river, only leaving
it for a short distance, when their course is interrupted by rapids, and
replunging into the stream when the obstacles cease. Wherever they
are found, they enjoy open water all the year round. Their un-
wieldy heavy form and short limbs are admirably adapted for their
aquatic habits, but unfit them for journeying by land.

‘There is no reason to believe that the huge European fossil species
was in any respect less aquatic in its habits than its living congeners.
Wherever its remains have been discovered in the greatest abundance
and perfection, it has invariably been along the margins of rivers or
great lakes, such as the Val d’Arno, where the bones of hundreds
of individuals have been observed. It appears to have been spread
over nearly the whole of the Pliocene area of England, since bones
and teeth have been described from the valleys of the Severn, the
Avon, and the Thames, Kirkdale Cave, Kent’s Hole, and Durdham
Down. The general argument, so ably discussed by Dr. Fleming,
that we cannot predicate, in many cases, what the food and habits of
extinct species of the same genus may have been, will not apply to
the fossil Hippopotamus major, which must have lived in open water
free from ice, if it lived the whole year round in England. That it
was capable of migration by land more than the existing species we
have no grounds for believing; and if it is argued that there may
have been large rivers flowing from the south during the Pliocene
period, along the course of which the Hippopotami could have
migrated during winter, the argument might apply to the population

Dr. H, Woodward—Recent and Fossil Hippopotami. 117

of one or two river-valleys, but it would hardly extend to the
Hippopotami spread over the broad area of England. In balancing
these various considerations, it seems to me most probable that the
Hippopotamus major was a permanent resident in the country during
the Pliocene period. This would involve a comparatively warm
temperature throughout the year as late as the deposition of the
‘Grays Thurrock’ beds, and the same would seem to be indicated
by the presence of some southern freshwater shells,’ which are now
extinct in England.” ?

The living Hippopotamus amphibius appears to be met with on all
the tributaries of the Nile, and was in earlier times abundant in
Egypt also. It is still found on the Senegal and the Zambesi, and
along the course of most of the rivers of the eastern coast, and
along the coast itself, at many spots south of the equator to near
Natal.

There is a second living species of Hippopotamus (H. Liberiensis),
which is a much smaller animal than the common Hippopotamus. It
rarely attains a weight exceeding four hundred pounds, or a quarter
of a ton, as distinguished from the four tons weight attained by the
male (Obaysch) which died at the Zoological Gardens in 1878, then
twenty-nine years of age. One of the most important differences
between the two consists in the fact that the Liberian Hippopotamus
possesses only two incisors in the lower jaw.

The Siwalik Hills of India, whose older Pliocene deposits are so
rich in the remains of Proboscidea and other Ungulata, have also
yielded three species of Hippopotami, namely, £7. sivalensis, F. and C.;
HT. Travaticus, F. and C.; H. namadicus, F. and C., and one from
the Narbadas, 1. paleindicus, F. and C.

The first of these, H. sivalensis, is figured in our Plate (Plate III.
Fig. 3-5); it is somewhat smaller than the existing species, /.
amphibius, and has six incisor teeth in each jaw. This led Falconer
to propose for those Indian forms with six incisors a new generic
division, Hexaprotodon, the others being Tetraprotodont. H. pale-
indicus and H. namadicus evidently offer in the gradual diminution
and squeezing out of one pair of their incisors, a distinct passage
from the hexaprotodont to the tetraprodont type of the modern
HT. amphibius.

Prof. A. Gaudry has described a Pleistocene (?) species, H. Hippo-
nensis, from Algeria. A small species of Hippopotamus has also been
found fossil in Madagasear (Dawkins).

But perhaps the most interesting species met with in a fossil
state are the Hippopotamus Pentlandi, H. von Meyer, and the
H. minutus of de Blainville. The latter is from the Pleistocene
Caves and fissures of the Island of Malta, where it has been
found associated with the remains of the pigmy Hlephant ;
the former was obtained from the Grotta di Maccagnone, near

1 Cyrena fluminalis is common in the Brickearths of the Thames Valley in associa-
tion with Rhinoceros Hlephas and Hippopotamus. Now it is found living in the
Nile, and in India and China.

2 « Falconer’s Paleontological Memoirs,’’ vol. ii. pp. 207-208.

118 =Dr. H. Woodward—Recent and Fossil Hippopotami.

Palermo, Sicily. So abundant were the remains of this species
(H. Pentlandi) in the various caverns near Palermo, that, for
many years, the bones were exported by shiploads to England and
Marseilles, for the manufacture of lamp-black for sugar-refining.
Two hundred tons were removed from one cave (San Ciro) in six
months. Dr. Falconer writes that literally tens of thousands of
two species of Hippopotami have been found fossil in Sicily alone.
Mr. Lydekker considers there is a complete gradation in size from the
largest fossil individuals of H. amphibius through H. Pentlandi to the
smallest specimens of H. minutus. Prof. Boyd Dawkins evidently
considers that H. minutus and H. Pentlandi are varieties of the same,
and that they extend from Malta to Sicily, and thence to Crete and
the Morea. He adds, “It is closely allied to the Liberian species,
although it is pretty certain that it differed from it in the form of
its molar teeth.” The Hippopotamus possessed the following series
of teeth, viz. :—
bs
incisors — canines a molars = 40,

The molar teeth were of the bunodont type, their crowns being
tuberculated (as in the Pigs, Mastodon and Manatee), and wearing
down with use, so as to produce the characteristic double trefoil
pattern (see Plate III. Fig. 5). j

So far as at present known, the Hippopotamus is exclusively con-
fined to the Old World, no member of the genus having as yet been
met with in any Tertiary deposit on the American Continent.

We had, then, in Europe, in later Tertiary and early Quaternary
times, at least two species of Hippopotamus, agreeing in size, and
probably also in identity, with the two existing African species ;
whilst in India, in late Miocene or early Pliocene times, we had four
species marked by differences in their dentition, and evidently be-
longing to an older and earlier type than the preceding.

3
3

* In H. sivalensis we should have incisors -

+ Or molars oo
6 6

EXPLANATION OF PLATE III.

. Palatal view of the skull of the recent Hippopotamus amphibius from Africa.
. Lower jaw of same seen from above.
(Both figures greatly reduced.)
. Palatal view of skull of Hippopotamus sivalensis, F. and C.
. Front or symphisial portion of lower jaw of H. sivalensis, showing the six
incisors and the tusk-like canines.
(Both figures one-eighth natural size.)
», 5. Molar tooth of same species, showing the worn-down double trefoil pattern
of the crown (one-half natural size).
Figures 1 and 2 are taken, by permission, from Cassell’s Natural History,
vol. iil. p. 349, article by Prof. Boyd Dawkins and H. W. Vakley.
Figs. 8—5 are reproduced from Prof. H. A. Nicholson’s Paleontology,
vol. ii. p. 843, Fig. 640 (after Falconer and Cautley).

.
=
Noe

i oO

Notices of Memoirs—B. Stuerts— Paleozoic Starfishes. 119

INF OQMBIKe AS) Owes IMs MitOunswsea

I.—Beirrac zur Kenntniss PaLmozoiscHER SEESTERNE. Von
B. Srurrz, in Bonn. Paleontographica, Band xxxii. 1886.
Mit 7 Tafeln.

A ConrrrsutTion To THE KNOWLEDGE oFf PALMOZOIC STARFISHES.
By B. Srurrrz, in Bonn. Paleontographica, vol. xxxii. pp.
75-98, pl. vill.-xiv.
ERD. ROEMER called attention * some years since to the echino-
dermal fauna occurring in the roofing slates of Bundenbach
near Birkenfeld in Oldenburg, which belong to the horizon of the
middle beds of the Rhenish Lower-Devonian. More particularly,
Starfishes, including in the term the Asteroidea and Ophiuroidea, are
abundant. The calcareous tests of these animals have been replaced
by iron pyrites, and they are firmly imbedded in the hard slate in
such a manner, that at the time when Rvemer wrote, only the
general outline of the animals could be discerned; but within the
last year or two means have been found by which the slaty matrix
can be entirely cleaned away, and the skeleton of the animal laid
bare, so that the arrangement of the plates of the test, both on the
ventral and dorsal surfaces, can be ascertained. The insight thus
gained of the skeletal structure of these Devonian Starfishes has
enabled Herr Stuertz to make a comparison between them and the
more recent fossil and existing members of the group, and amongst
other results of his work he has discovered true Ophiuroids, with a
structure corresponding with that of living forms, which have not
previously been known from Paleozoic strata. These were associated
with the simpler Palaeozoic Ophiuroids. There are also in these beds
a number of true Asterids, associated with Encrinasters; and a re-
presentative of the existing genus Astropecten.

The single species of the Ophiuree vere belongs to the genus
Ophiurella, Ag., and is named O. primigenia, St. In the group of
the Protophiuree are included Paleozoic Ophiuroids which possess
corresponding ambulacral plates on the ventral side of the arms.
The author agrees with Litken in regarding these as doubled ventral
shields, which cover the ambulacral system. In this group the
author places the Protaster Miltoni, Salter, and P. leptosoma, Salter,
and also a new genus, Furcaster, with a single species, F. palgo-
zoicus, St.

Fresh observations have been made on the doubtful genus Helian-
ihaster, Roemer, examples of which also occur in Devonshire as well
as at Bundenbach, but they are still insufficient to determine its true
position. The author regards it as an Ophiuroid Starfish with from
14-16 arms and a tolerably large disc.

The author gives the name Ophio-Encrinasteria to a group of
forms which stand in near relationship to Ophiuroids, but possess
peculiarities of structure which ally them to the Encrinasteride. In

1 Paleontographica, Band ix. 1862.

120 Notices of Memoirs—K. A. Penecke—FKocenes in Carinthia.

addition to a new genus, Bundenbachia, this group also includes the
genera Teniaster, Billings, Eugaster, Hall, possibly also Ptilonaster,
Hall, and Protaster Forbesi, Hall, with Protaster Sedgwicki, Forbes.

Under the Asterie vere, or true Starfishes, are placed Roemeraster
asperula, Roemer sp., Astropecten Schlueteri, St., Palastropecten
Zitteli, St. n. gen. et sp., Holuidia Decheni, St., n. gen. et sp., and
Protasteracanthion primus, St. n. gen. et sp.

The following genera and species are placed in the group of the
Encrinasteria: Aspidosoma Tischbeinianum, Roemer; Loriolaster mira-
bilis, St.; and Palasteriscus devonicus, St.

The species described are all figured in the accompanying plates
and enlarged representations are given of their structural characters.

Gaepla.

I].—Tuer Eocrnr Srrata or tHe Krapprenp, Cartnrura. By K.
A. Penecks. Imper. Geol. Inst. Vienna, Meeting 17th Novem-
ber, 1885. Communicated by Count Maxrscuatt, F.C.G:S.
NLY small portions of the Hocenes, resting partly on Cretaceous

rocks and partly on Paleozoic schists, have escaped denuda-
tion. In one of these patches, the succession (upwards) is—

1. Lower red clays, with gravelly beds and conglomerates. 2.
Modiola-marls, with, for the most part, badly preserved remains ;
Modiola, sp. (compare crenella, Desh.), is the most frequent. 3. Two
or three seams of bright coal, with bituminous shales, containing
brackish-water shells as Faunus combustus, Brongn., F. undosus,
Brongn., Melanopsis, sp., Planorbis, sp., and Cytherea Lamberti,
Desh. 4. Gasteropod-marls; similar to the foregoing marls, and
abounding with well-preserved shells, as Zurritella Fuchsi, sp. nov.,
Cerithium mutabile, C. Canavali, sp. nov., Natica perusta, and Ostrea
Canavali, sp. nov.,; together with Nummulites contortus, Desh., Ser-
pula spirulea, Modiola crenella, Cyrena Veronensis, Faunus combustus,
F. undosus, Fusus longevus, etc. 5. Nummulitic Marls. Here Gas-
teropods are gradually being superseded by Nummulites. The
prevalent fossils are: Orbitoides Fortisii, Operculina Karrert, sp.nov.,
Nummulites complanatus, N. perforatus, N. Lucasanus, JV. contortus,
N. exponens, Natica Vulcani, and Cerithium Canavali. 6. Nummu-
litic Limestones gradually coming out of the uppermost horizon of
No. 5. They contain many Hchinids, Molluscs, ete., as Alveolina
longa, Nummulites complanatus, N. perforatus, N. contortus, Conocly-
peus conoideus, Echinolampas (comp. Suessi), Pygorhynchus Mayeri,
Tinthia Heberti, Ostrea rarilamella, Velates Schmiedeliana, Ovula
gigantea, etc. 7. Variolarius-strata. Rather thin sands, and beds
of compact sandstone, full of Nummulites variolarius,

Some of these beds, toa greater or less extent, are wanting, or are
represented by other deposits, elsewhere in the Krappfeld. At one
place some fine sands occur in the uppermost horizon of the Nummu-
litic Marls; and they contain good specimens of Hchinanthus tumidus,
Agass., Linthia scarabeus, Lbe., L. Heberti, Cott., and Ottiliaster
pusillus, nov. gen. et sp. A comparison of the several sections proves
the existence of two special horizons in the Krappfeld Hocenes: an

Notices of Memoirs—Geology of Afghanistan. 121

upper, marine, with abundance of Nummulites, and assuming a
brackish character to the north, and a lower partly brackish horizon.
The fauna throughout is Lower Eocene, and has several species in
common with the fauna of Ronea, and presenting some analogy to the
Sables inférieurs of the Paris Eocenes. This fauna numbers about
85 species,—among them are 6 Nummulites, 4 other Foraminifera,
11 Echinida, 2 Serpule, 1 Terebratula, 1 Dentalium, 25 Bivalves, 29
Gasteropods, and 1 Nautilus, besides remains of Fishes and Crusta-
ceans. The new forms are——l. Operculina Karrert, with conspicuous
transverse ribs. 2. Oittiliaster pusillus, new genus of the Hchino-
lampas type, the anterior ambulacra having but one series of single
pores; approaching Holampas, Dune. and Slad., from Sind, India.
3. Ostrea Canavali, Grypheea-like, allied to O. cymbiola. 4. Arca
Rosthorni, very small, with craticulate sculpture. 5. Corbuia semi-
radiata, somewhat like Neera radiata, fore-part radiately ribbed.
6. Turritella Fuchsi, approaching T. imbricataria, Lamk. 7. Natica
Ottilie, a small and rather indifferent form, resembling WV. Woodi.
8. Cheilostoma Rosthorni, like some species from the lowermost
Belgian Eocenes. 9. Melanopsis? Reinert; the genus uncertain,
most of the specimens being crushed. 10. Cerithium Canavali, very
near to C. lunatum, Mstr. 11. Nautilus Seelandi, very broad and in-
flated. 12. Myliobates Haueri, near to I. goniopleurus, Agass.

IJI.—Tue Rock-satt Formation or Wie ttczKa, Gatrora. By J.
Nizezwirecet. Imp. Geol. Instit. Vienna, Meeting 17th Novem-
ber, 1885. Communicated by Count Marscuatt, F.C.G.S.

HE borings, undertaken in order to explore the supposed west-
ward continuation of the Salt beds, gave the following results.
An alluvial deposit, 13 meter thick, covers a grey clay (partly a
marl), with seams of micaceous sand, and boulders of compact marl.
This clay continued to the depth of 20435 meters, and contained some
few stalks and leaves of plants, with Foraminifera (Globigerina, Poly-
morphina, and Truncatulina). This may be regarded as an eastward
continuation of the sulphuriferous deposits of Swoszowice, which
likewise has terrestrial plant-remains and marine shells. Coarser
sand, or friable sandstone, with thin intercalations of clay, fibrous
gypsum, and pieces of anhydrite, continues from 2044 to 210 meters
depth. Between this and the present depth of the bore (2274
meters), saliferous clay, with scattered granular rock-salt, gypsum,
and anhydrite, was pierced. Water drawn from this depth was
highly saturated with salt.

1V.—Geotocicat Formations 1n Arcuanistan. By C. L. Gries-

BacH, F.G.S. Imper. Geol. Inst. Vienna, Meeting 38rd Novem-
ber, 1885. Communicated by Count Marscuatt, F.C.G.S.

l PLIOCENE. Sandstones and loose sands, with great deposits of

» loess, and badly-preserved Mammalian remains. 2. Pliocene.

Red and light-coloured clays, with beds of loess and gypsum. Nos.

1 and 2 may be equivalent to the Manchhar and Siwalik Formation

122 Notices of Memoirs—Dr. MW. Schuster—Atmospheric Dust.

of India. 38. Miocene (and Eocene?). Thick deposits of green and
red clays, with friable limestones, and salt-beds. Miocene fossils in
the upper horizons. 4. Cretaceous. Inoceramus-beds, marls (mostly
variegated), and limestones with Cretaceous fossils. Marine lime-
stones abounding in organic remains. 5. Jurassic and Lias. Light-
coloured sandstones and grit, with marine limestones, and plant-
remains. 6. Triassic. “ Red-grit Group ;” an enormous assemblage
of red sandstones, conglomerates, breccias, and volcanic tuffs, with
intercalated eruptive rocks (mostly melaphyres), and several horizons
of Brachiopod limestones. 7. Permian. Green and grey schists,
sandstones and conglomerates, with ‘Boulder-beds,” thin coal-
seams and imperfect impressions of plants 8.H. of Herat and in
Khorassan, alternating with hard limestones, containing Brachiopods,
Conchifera, and Fusuline. Nos. 5, 6, and 7 may possibly cor-
respond to the Gondwana Formations of India. 8. Carboniferous
(and Devonian?). Very thick, compact, grey limestones, with sub-
ordinate shales, containing Fenestella, Productus semireticulatus,
Athyris Royssyi, ete., in the upper horizons. No. 8, answering to the
Kulling strata of Cashmere, constitutes the lowermost horizon in
the large folds of the Dayendar, Doshatch, Bizd, and other mountain-
chains.

V.—ArmospHertc Dust. By Dr. M. Scuuster. IJImper. Acad.
Vienna, Meeting 14th January, 1886. Communicated by Count
Marscuatt, F.C.G.S.

HIS dust was collected at Klagenfurt in Carinthia, after a rain of
muddy substance, which had taken place on the 14th October,
1885. The chief constituents of the dust are minute fragmentary
crystalline granules and flakes of the following minerals :—quartz,
opal, orthoclase, biotite, phlogopite, pyroxene, amphibole, light-
coloured mica, talc, kaolin, chlorite, rutile, anastase, zircon, tourma-
line, ferruginous clay, spinel, magnetite, pyrites, magnetic pyrites,
calcite, magnesite, ferruginous dolomite, and apatite. The presence of
metallic iron could not be ascertained. The microscope showed
a prevalence of siliceous, silicified, and calcareous remains of organ-
isms, especially of Diatomacee, either in single or in pairs, together
with a few carbonaceous or carbonized substances, such as the spores
of Fungi and such like, filaments of Alge and other plants, silicified
membranes of parenchymal cellules, and pyritized and silicified
spherules, resembling pollen. This dust bears a great general
resemblance to the atmospheric dusts described by Ehrenberg and
Silvestri. The reddish-yellow colour, which it has in common with
the “ Passat” dust, may be an objection against its having come
direct from the Sahara.
[Compare the results of Prof. Judd’s examination of Nile mud,
Proc. Roy. Soc. vol. xxxix. No. 240, p. 216, Nov. 1885. |]

Reviews— Prof. Dr. Nicholson—British Stromatoporoids. 128

o5¢/ 22h Wh 2G deh WwW Se

I.—A MonocrapH or THE British SrRomatoporoips. By H.
Atnryne Nicuotson, M.D., D.Sc, etce., Regius Professor of
Natural History in the University of Aberdeen. Part I. General
Introduction, pp. iii. and 180, with 11 Plates. (Paleeontographical
Society’s Volume for 1885.)

HE nature and systematic position of the widely-distributed

groups of Paleozoic fossils, known generally as_ the

Stromatopore, now styled by Prof. Nicholson ‘“ Stromatoporoids,”

have given rise to very varied differences of opinion, ever since

the first genus was described by Goldfuss in 1826. The group has
been alternately regarded as belonging to Foraminifera, Sponges,

Polyzoa, Corals, and finally to Hydrozoa. Such diversities of opinion

have not merely been maintained by those earlier authors, whose

knowledge of the organism was limited to its form and other external
features, but they have been also held by later investigators, who
have studied its microscopic characters in thin sections. The
opposing views may be to some extent explained by the different
appearances presented by the fossils under different conditions of
fossilization, by limited investigation, and in no small degree by the
influence of previous lines of study on the part of the respective
authors. Thus, for instance, Sir J. W. Dawson finds certain
structures in Stromatoporoids resembling those in the supposed
Foraminifer, Hozoon Canadense, and dismisses almost with con-
tempt the view of Mr. H. J. Carter that Stromatopore are
skeletons of hydroids allied to Hydractinia. This latter view is,
however, now generally received; whilst Sir J. W. Dawson’s opinion’
that ‘Stromatopora and Hozoon may both be regarded as large,
sessile, laminated calcareous Rhizopods,” has not been supported by
later authors. Prof. Sollas, on the other hand, places Stromatopora
among the Vitreo-hexactinellid sponges, an opinion which was
subsequently qualified by the statement that Stromatopore included
organisms of very different affinities, some being siliceous sponges,
some related to Millepora and Hydractinia, and some with relation-
ships yet undetermined. Baron Rosén referred the group to Keratose
sponges, in which the fibres had become silicified or calcified in
fossilization. Prof. Nicholson also, in a joint memoir with Dr.

Murie, reached the conclusion that the Stromatopore belonged to

a peculiar extinct group of Calcisponges. To Mr. H. J. Carter

belongs the credit of having first indicated the relationship of the

Stromatoporoids to the recent Hydractinia, and their extinct allies,

and this view has gradually been adopted by paleontologists

generally.

The difficulties attending the study of this group of fossils may
readily be inferred from the various opinions held with respect to
their characters, and the present attempt to overcome the obstacles
which have baffled previous observers implies no small amount of
courage on the part of the author. The only sure method of investi-

1 Quart. Journ. Geol. Soc. vol. xxxv. 1879, p. 50.

124 Reriews—Prof. Dr. Nicholson—British Stromatoporoids.

gation rests on the study of the minute structure of the skeleton,
and this can only be known by means of thin microscopic sections.
Of these, the author states that he has made considerably over a
thousand with his own hands, whilst most of the specimens were
collected by himself, from the Paleozoic strata of this country,
North America, Germany, and Russia. By thus comparing the
microscopic characters of all, or nearly all, the known forms of the
group, under the different conditions of mineralization, it has been
possible to obtain a more complete knowledge of these organisms
than heretofore, and many features of importance, both as regards
the structure and relationship of the group, have been discovered.

The first part of the Monograph contains the ‘‘ General Introduc-
tion,” which is treated under the following heads: (I.) Historical
Introduction. (II.) The General Structure of the Skeleton. (III.)
Systematic Position and Affinities of the Stromatoporoids. (IV.)
Sketch Classification. (V.) Families and Genera of the Stromato-
poroids. (VI.) The Nature of Caunopora.

(1.) Under the first head an account is given in chronological order
of the various memoirs on the group. From this we learn that the
type-specimen of Stromatopora concentrica, Goldf. (now preserved in
the Bonn Museum), which is the type species of the genus, exhibits
a structure greatly different from that which has generally been
regarded by paleontologists as characteristic of the genus Stromato-
pora. The typical figured specimen of Goldfuss is a large mass of
numerous thick concentric strata (“latilamine’’), more or less undu-
lating, from 1:5 to 3 mm. in thickness, and separated by narrow
interspaces. Microscopic sections show that the skeleton is essen-
tially a complex net-work of anastomosing calcareous fibres, so
disposed as to inclose correspondingly complex anastomosing canals.
The minute characters of this typical form had not previously been
subjected to microscopical examination, and consequently the forms
assigned to the genus by Bargatzky, Carter, and others, which
possess structures of a different character, must necessarily be
included in a new genus, which the author proposes to name Acti-
nostroma, and which forms the type of the group Actinostromide.

(II.) Treating of the general strueture of the skeleton of the
Stromatoporoids, the author states that the typical form is that of a
hemispherical mass or a flattened expansion, attached by a narrow
peduncle, or directly to some foreign body, but having the under
surface covered by a concentrically wrinkled imperforate epitheca,
while the apertures for the emission of the polypites are carried
upon the upper surface. Certain forms are ramose or dendroid, and
some habitually encrust other organisms. The skeleton was
originally of granular carbonate of lime, probably in the form of
arragonite, but this is now replaced occasionally by silica and by
crystalline calcite. One distinctive feature of the whole group of
the Stromatoporoids is the constitution of the skeleton of super-
imposed concentric layers. In some cases these are very thick,
strata-like, and made up of a series of vertical rods (“ radial
pillars”), which run from the top to the bottom of the stratum, and

Reviews—Prof. Dr. Nicholson—British Stromatoporoids. 125

are united at irregular intervals by oblique or horizontal processes.
Between the vertical rods are the tortuous, tubular, and often tabulate,
canals, in which the zodids were lodged. In other cases, the skeleton
is made up of numerous closely-approximated concentric laminz, not
in absolute contact, but separated by interlaminar spaces, which are
intersected by vertical columns or “ radial pillars,” which connect
the laming, and may pass through several laminz and interspaces.
The calcareous fibres of the skeleton are probably in no case compact,
sometimes they are filled with what appear to be minute pores or
vesicles, at others by complex ramifying tubuli. Nothing of the
nature of definite spicules has been noticed in any example of the
group.

According to the general arrangement of the “radial pillars” and
“concentric laminz ” two principal sections of Stromatoporoids are
distinguished, the Milleporoid and Hydractinioid sections. In the
first of these, represented by the genus Stromatopora, Goldfuss, the
radial pillars and concentric laminz are completely amalgamated,
and, as arule, cannot be recognized as distinct structures. Tan-
gential sections of the skeleton appear to be continuously reticulate,
resembling that of Millepora, whilst in vertical sections the radial
pillars appear as thick, irregular and flexuous, and the concentric
laminz are only represented by irregular lateral outgrowths, which
spring from the pillars and unite them into a continuous framework.
Jn the “ Hydractinioid” section, represented by the genus Actinostroma,
the radial pillars and concentric layers are present as distinct, though
closely connected structures. In vertical sections of A. clathratum,
the skeleton appears as a series of parallel vertical rods, nearly
equi-distant from each other and connected at regular intervals by a
series of parallel horizontal lamine. Ina tangential or horizontal
section, the transversely-divided ends of the radial pillars appear as
rounded or stellate dots, placed at tolerably regular intervals. The
radial pillars give out at regular intervals, verticils of horizontal
connecting processes or arms, which join one another to form a com-
plete network, and the concentric lamine are, in reality, formed of
these united horizontal processes. When the section passes through
the plane of one of the concentric lamina, the cut ends of the radiate
pillars have a stellate form, and their united arms form an angular
mesh-work, not unlike that of a hexactinellid sponge, but if the
section is through the interlaminar spaces, then only the cut ends of
the radial pillars are visible. Thus the concentric lamina is, in
reality, merely a porous mesh-work, through the openings of which
in the upper layer the zodids could extend.

In the genus Clathrodictyon, Nich. and Murie, the radial pillars
are incomplete or almost obsolete, whilst in Labechia they are highly
developed. The author states that the radial pillars are not invari-
ably solid, a minute central canal can be detected in many, but even
where this exists, it does not appear to have been open at the sum-
mit. There is no ground for the supposition that the pillars were
inhabited by zodids, or that they can be compared in any way with
the zovdidal tubes of Millepora. In one singular form, Hermatostroma

126 Reviews—Prof. Dr. Nicholson—British Stromatoporoids.

Schluteri, there are large canals in the radial pillars, which send out
branches into the connecting processes forming the concentric
lamina, and this fact indicates that the fibres of the concentric
lamina generally may be hollow.

One obstacle to ranging the Stromatoporoids with the Celenterata
has been the apparent absence of any tubes for the lodgment of the
zooids, but the author has made the important discovery that the
skeleton of the typical Stromatopore is penetrated by numerous
minute, flexuous, but essentially parallel, vertical tubes, which are
not bounded by definite walls, but simply inclosed by the vermicu-
late fibres of the coenosteum, precisely like the zodidal tubes in
Millepora. Further, these tubes are traversed at intervals by
calcareous plates, similar to those of Millepora and tabulate corals.
These tabulate zodidal tubes can be clearly distinguished in different
species of Stromatopora, and also in such genera as Idiostroma,
Winch., and Stachyodes, Barg. Definite tubes are not clearly recog-
nizable in the Hydractinioid section of the group, but there are
zooidal cavities in Actinostroma, and in Labechia it is probable that
the zodids were given off from the surface layer of the ccenosare.

The author agrees with Mr. Carter in recognizing the stellate
canal system on the surface of the concentric laminz as the homo-
logue of the branching of the ccenosarcal grooves on the surface of
the skeleton of many Hydractiniz, and adopts for it Mr. Carter’s
term Astrorhize. These canals, though not invariably present, are
yet found in so many different forms of the group, that they cannot
be accepted as of generic value, and consequently the genus Cono-
stroma, Winchell, in which they are regarded as an essential
character, cannot be retained.

In some anomalous, cylindrical or dendroid, Stromatoporoids,
placed in the genera Idiostroma, Amphipora, and Stachyodes, there
is a central, axial, tabulated tube, without proper wall, giving off at
times lateral branches, which also divide. These ‘‘axial tubes” are
quite distinct from those of the so-called Caunopora, and the author
thinks they may have lodged a stolon or axis of the coenosarc, and
that the smaller lateral tubes may have been occupied by a special
series of zodids.

Certain large-sized lenticular vesicles, resembling the ‘‘ ampulle”
of the recent Stylasteride, are present in Amphipora ramosa, Phill.
sp., and may probably have lodged the reproductive zodids, and
large tabulated vesicles in Idiostroma capitatum, Goldf. sp., may also
have served for the same purpose.

(III.) Systematic Position and Affinities. —The author frankly accepts
the views of Carter, Lindstrom, Zittel, and others as to the ccelen-
terate affinities of the Stromatoporoids, and regards them as a special
group of the Hydrozoa, having relationships on the one hand with
Hydractinia, and on the other with Millepora. A detailed com-
parison between Hydractinia echinata, Flem., and forms of dctino-
stroma, Nich., shows that there is a remarkable similarity between
the minute structure of the chitinous skeleton of the former organism
and the large calcareous coenosteum of the latter; and a similar but

Reviews—Prof. Dr. Nicholson—British Stromatoporoids. 127

not so striking a resemblance is also seen when the comparison is
made with the Hydractinia circumvestiens from the Red Crag of Sut-
folk, which possesses a calcareous coenosteum. The typical Stromato-
pores, on the other hand, are more closely comparable with the coeno-
steum of Millepora. But as both the groups of Stromatoporoids are
linked together by intermediate forms, and thus constitute a natural
series, it is better to retain these fossils as a peculiar division of the
Hydrozoa

(IV.) Sketch Classification.—This is to be accepted as largely tenta-
tive, as many of the types have not yet been properly examined.
The following tabular view is given by the author.

Order.—StromaropororpEA, Nich. and Murie.
Section A. (‘‘ Hydractinioid” Group).
Fam. 1. Actinostromide, Nich.

Genera—Actinostroma, Nich.; Clathrodictyon, Nich. and Murie;
Stylodictyon, Nich. and Murie (?).

Fam. 2. Labechiide, Nich.

Genera— Labechia, E. & H.; Rosenella, Nich.; Beatriceu, Bill. (?) ;
Dictyostroma, Nich. (?).

Section B. (‘ Milleporoid” Group).
Fam. 3. Stromatoporidz, Nich.
Genera—Stromatapora, Goldf.; Stromatoporella, Nich. ; Paralleto-
pora, Barg. (sub-genus ?) ; Syringostroma, Nich. (sub-genus ?).

Fam. 4. Idiostromide, Nich.

Genera—Idiostroma, Winch.; Hermatostroma, Nich.; Amphipora,
Schulz; Stachyodes, Barg.

(V.) Families and Genera of the Stromatoporoids.—Detailed descrip-
tions are given of the characters of the various members of the
group, to which space prevents further reference, but the inclusion
of the peculiar forms known as Beatricea, Bill., as a genus of
Stromatoporoids, calls for some notice. ‘These fossils are cylindrical
or angulated rods or stems, often of considerable size, some reaching
10 feet in length by one foot in thickness. They possess a central,
relatively large, axial canal, without definite walls, and divided by
superposed, curved, tabule. Between the central canal and the
exterior of the fossil, the skeleton consists of concentric layers of
vesicular tissue. The position of these fossils has long been regarded
as uncertain, and one observer, Prof. Hyatt, who formerly referred
the genus to the Cephalopoda, now degrades it to the Foraminifera.
The general opinion has been in favour of its alliance to the
Cystiphylloid Corals. The fossils are generally very imperfectly
preserved, but Prof. Nicholson has detected, in some specimens,
structures radiating from the central canal towards the circumference,
which he regards as “radial pillars” essentially similar to those of
the genus Labechia. The axial tabulate tube is regarded as parallel
with the tubes in Idiostroma, Stachyodes, and Amphipora. But the
axial tubes in these forms are so much smaller than those of Beatricea,

128 = Reviews—Prof. Dr. Nicholson—British Stromatoporoids.

that whilst it may seem reasonable to suppose that the former were
occupied by a stolon or axis of the ccenosarc, the same explanation
will hardly suffice for the latter, in which the axial canal is some-
times 10 mm. in diameter. On the whole, whilst fully appreciating
the significance of the facts brought forward by Prof. Nicholson, we
should feel disposed to wait for further evidence before definitely
accepting Beatricea as a genus of Stromatoporoids.

(VI.) The Nature of Caunopora.—The author discusses in detail the
much-debated subject of the nature of the Stromatoporoids, in which
the coenosteum is traversed by thick-walled tubes at right angles to
the concentric lamin of the fossil. These tubes are frequently
tabulate, and in some cases they possess spines resembling the spinal
septa of "Favosites or Syringopora, and they are usually all connected
together and open into each other, whilst at the same time no com-
munication can be traced between them and the interlaminar spaces
of the Stromatopora itself. Prof. Nicholson has established the fact
that in several distinct species of Siromatopora and Stromatoporella,
there are two states of the same species occurring in the same locality,
one, in which the so-called ‘‘ Caunopora” tubes are present, and the
other in which these structures are entirely wanting. It follows from
this, that the existence of these tubes can in no wise characterize a
particular genus, and therefore the names of Caunopor a, Phill., and
Diapora, Barg., must be abandoned.

In character these “‘ Caunopora”’ tubes closely resemble the tubes
of Syringopora and Aulopora, and by Roemer, Carter, and others
they are believed to be independent organisms enveloped in the
growth of the Stromatopora. There are certain difficulties against
the acceptance of this theory; one is the fact, that many of these
tubes are not known independent of their Stromatopora envelopment.
The ‘‘ Caunopora” tubes often occur also in localities where indepen-
dent forms of Syringopora are altogether absent, and on the other
hand, where the corals are abundant, the “Caunopora” forms of
Stromatopora are rare. It is possible that, owing to the commensal
mode of growth, distinct forms of Syringopora and Aulopora may
have been produced. ‘The author arrives at the conclusion that
“the fossils ordinarily called ‘ Caunopore’ and ‘ Diapore’ are the
result of the combined growth of some Stromatoporoid with some
Coral, the former usually being a species of Stromatopora or Stroma-
toporella, and the latter generally belonging either to Syringopora or
to Aulopora.”

In concluding this notice, we may call attention to the beautiful
plates in which the minute structures of the organisms described are
fully illustrated. The plates have been drawn by the author and
lithographed by Mr. Hollick. This first part of the Monograph
needs no commendation. It is a very important contribution to the
knowledge of a most puzzling group of organisms, and the subject is
treated with that thoroughness which specially characterizes Prof.
Nicholson’s work. G. J. H.

Reviews—J. F. Whiteaves—Canadian Paleontology. 129

TJ.—Report on THE INVERTEBRATA OF THE LARAMIE AND CRETA-
cEous Rocks or tHe Norru-west Territory. Contributions
to Canadian Paleontology. By J. F. Wurrnaves, F.G.S., ete.
Palzontologist and Zoologist to the Survey. Vol. I. Part ie
Svo. pp. 89 and 6 Plates. (Montreal, Dawson Bros., 1885.)

NDER the title of ‘Contributions to Canadian Paleontology,’ it is
proposed to publish such papers as cannot be conveniently included
in either of the volumes on the Paleozoic or Mesozoic Fossils of
Canada, now in course of preparation. This first part contains a deter-
mination of the marine, brackish, and freshwater invertebrate fossils
—with one exception, all mollusca—collected by Dr. G. M. Dawson
and others in the North-west Territory of Canada. Many of these
fossils have already been described by Messrs. Meek and Hayden
and other United States paleontologists, and of these reference is
made to the synonymy, and the localities are given where they occur.
The new forms are fully described and figured. They include Unio
Albertensis, Anomia perstrigosa, Corbicula obliqua, C. perangulata,
Panopea simulatrix, P. curta, Acella, sp., Physa Copei, var. Canadensis,
Acroloxus radiatulus, Patula angulifera, P. obtusata, Anchistoma
parvulum, Valvata filosa, V. bicincta, Gervillia recta, var. borealis,
Modiola dichotoma, Cyprina ovata, var. alta, Protocardia borealis,
Panopea subovalis, Scaphites subglobosus, Crenella (?) parvula, Unio
supragibbosus, Rhytophorus glaber, Planorbis paucivolvis, Hydrobia
subcylindracea, and the solitary Crustacean Hoploparia 2? Canadensis.
The rocks from which these fossils have been obtained are fully
described by Dr. G. M. Dawson in the Report of Progress of the
Geological Survey of Canada, 1882-4. In the Laramie Group are
included, (1) Porcupine Hill beds, of freshwater sandstones and shales
—2500 feet; (2) Willow Creek beds, also freshwater—450 feet; (3)
St. Mary River Series, nearly all freshwater—2800 feet; thus making
a total thickness of 5750 feet of strata assigned to the Laramie
Group. In the underlying (so-called) Cretaceous series the following
subdivisions are made: (a) Fox Hill Sandstones, brackish-water,
80 feet ; (b) Pierre shales, marine, 750 feet; (c) Belly River series,
910 feet; (d) Lower dark shales, 800 feet; in all a total thickness
of 2540 feet. he stratigraphical disposition adopted by Dr. G. M.
Dawson of a Cretaceous series and an upper series— the Laramie—
of extra Cretaceous rocks, is not, according to Mr. Whiteaves,
supported by the paleontological evidence. This author states that
the “invertebrate fauna of the ‘Belly River series’ seems to be
essentially the same as that of the Laramie of the United States and
Canada, unless more than one formation has been confounded under
the latter name, and that it is at present scarcely possible to separate
the ‘Lower Dark Shales’ of Dr. Dawson’s Report from the ‘ Fort
Pierre and Fox Hill Groups’ on purely paleontological grounds.”
If this statement is correct, that the fossils of these two important
series of strata are similar, it would be interesting to know the
reasons which have led to the separation of the Laramie division
from the Cretaceous in Canada. G. J. H.
DECADE III.—VOL,. I1I.—NO. II. 9

130 Reviews— The Paleontographical Society.

I1J.—Puszications oF THE PALHONTOGRAPICAL Socrrty, Lonpon.
Ato. Vols. XX XIII.—XXXIX., 1879—1885. President: Sir
Richard Owen, K.C.B., M.D., D.C.L., LL.D., F.R.S., F.G.S., ete.
Secretary: Professor T. Wiltshire, M A., F.G.S., 25, Granville
Park, Lewisham, §.E. Treasurer : Robert Etheridge. Esq., F.R.S.,
F.G.S., British Museum (Natural History), Cromwell Road, $.W.

HE Paleontographical Society was established in the year 1847,
for the purpose of figuring and describing the whole of the
British fossils. Hach person subscribing One Guiza is considered
a Member of the Society, and is entitled to the Volume issued for the
year to which the subscription relates.

Surely this is a Society that has the highest possible claims upon
the consideration of every geologist, who must, as a matter of course,
be deeply interested in the past Life-history of the Earth whose
crust he is bound, hammer in hand, to explore,

It seems rather surprising that only 475 Members should at present
be found willing to subscribe an annual guinea for so grand a publi-
cation, one which, in a mere mercantile sense, is richly worth two guineas,
in a scientific point of view, would be cheap at four guineas a year !

The following is a summary of the contents of the last seven
volumes issued :—

Vol. XX XIII. for the year 1879, contains :—

The Kocene Flora, Part I. by Mr. J. 8. Gardner and Baron Ettingshausen,
5 plates. —Second Supplementtothe Crag Mollusca (Univalves and Bivalves), by
Mr. 8. V. Wood, 6 plates. (Complete with Title page and Index).—The Fossil
Trigoniea, No. V. (Conclusion), by Dr. Lycett, 1 plate-—The Lias Ammonites,
Part II. by Dr. Wright, 10 plates.—Supplement to the Reptilia of the Wealden
(Goniopholis, Brachydect«s, Nannosuchus, Theriosuchus, and Nuthetes, No. 1X. by
Prof. Owen, 4 plates.—The Fossil Elephants (Z£. primigenius), Part II. by Prof.
Leith Adams, 10 plates.

Vol. XXXIV. for 1880, comprises :—

The Eocene Flora, Part II. by Mr. J. S. Gardner and Baron Ettingshausen,
6 plates. - The Fossil Echinodermata, Oolitic, Vol. II. Part III. (Asteroidea and
Ophiuroidea), by Dr. Wright, 3 plates. (Complete).— Supplement to the Fossil
Brachiopoda, III. (Permian and Carboniferous), by Mr. Davidson, 8 plates.—
The Lias Ammonites, Part III. by Dr. Wright, 22 plates.—The Reptilia of
the London Clay, Vol. II. Part I. (Chelone) by Prof. Owen, 2 plates.

Vol. XX XY. for 1881, embraces :—

The Fossil Echinodermata, Cretaceous, Vol. I. Part IX. by Dr. Wright, 6 plates.
— Supplement to the Fossil Brachiopoda, Part 1V. (Devonian and Silurian, from
Budleigh-Salterton Pebble Bed), by Dr. Davidson, 5 plates.—The Fossil
Trigonize (Supplement to No. 1), by Dr. Lycett.—The Lias Ammonites, Part
IV. by Dr. Wright, 10 plates.—The Reptilia of the Liassic Formations, Part
III. (Conclusion), by Prof. Owen, 13 plates. —The Fossil Elephants (4, primi-
genius and E, meridionalis), Part I11. (Conclusion), by Prof. Leith Adams, 13
plates.

Vol. XXXVI. for 1882 includes :-—

The Eocene Flora, Vol. I. Part 111. (Conclusion), by Mr. J. S. Gardner and Baron
Ettingshausen, 2 plates.—Third Supplement to the Crag Mollusca, by the late
Mr. 8. V. Wood, 1 plate. (Complete).—The Fossil Echinodermata, Cretaceous
Vol. I. Part X. (Conclusion), by Dr. Wright, 5 plates.—Supplement to the Fossil
Brachiopoda, Vol. IV. Part V. (Conclusion), by Dr. Davidson.—Supplement to
the Fossil Brachiopoda, Vol. V. Part I. (Devonian and Silurian), by Dr. Dayid-
son, 7 plates. —The Lias Ammonites, Part V. by Dr. Wright, 22 plates.

Reports & Proceedings—Royal Geological Society of Lreland. 131

Vol. XX XVII. for 1883, contains :—

The Eocene Flora, Vol. II. Part I. by Mr. J. S. Gardner, 9 plates.—The Trilo-
bites of the Silurian, Devonian, &c., Formations, Part V (Conclusion), by the
late Mr. J. W. Salter—The Carboniferous Trilobites, Part I. by Dr. H. Wood-
ward, 6 plates.—Supplement to the Fossil Brachiopoda, Vol. V. Part II.
(Silurian), by Dr. Davidson, 10 plates.—The Fossil Trigonize (Supplement
No. 2), by the late Dr. Lycett, 4 plates. (Complete).—The Lias Ammonites,
Part VI. by Dr. Wright, 8 plates.

Vol. XX XVIII. for 1884, comprises :—

The Eocene Flora, Vol. II. Part II. by Mr. J. S. Gardner, 11 plates.—The Car-
boniferous Entomostraca, Part I. No. 2 (Conclusion), by Prof. T. Rupert Jones,
Mr. J. W. Kirby, and Prof. G. 8. Brady, 2 plates.—'The Carboniferous Trilo-
bites, Part Il. by Dr. H. Woodward, 4 plates. (Conclusion). Supplement to
the Fossil Brachiopoda, Vol. V. Part III. (Conclusion), by Dr. Davidson,
4 plates.— The Lias Ammonites, Part VII. by Dr. Wright, 10 plates.

Vol. XX XIX.* for 1885, embraces :—

1. The Eocene Flora, Vol. II. Part III. (Conclusion), by Mr. J. S. Gardner, F.G.S.,
with 7 plates.—2. The Stromatoporoids, Part I. by Prof. H. Alleyne Nicholson,
M.D., D.Sc., F.R.S.E., F.G.S., with 11 plates.—3. The Fossil Brachiopoda
(Bibliography), Vol. VI. (Conclusion). by the late Dr. Davidson, F.R.S., and
Mr. W. H. Dalton, F.G.S.—4. The Lias Ammonites, Part VIII. (Conclusion),
by the late Dr. Wright, F.R.S., with 1 plate.

From this it will be seen that seventeen Monographs are brought

to a conclusion and have their Indices and Title-pages provided for
them; whilst fresh Monographs are announced as in progress, On
the Fossil Tertiary Plants, by J. Starkie Gardner, F.G.S.—On the
Coal-Plants, by Prof. Williamson, F.R.S., of Manchester.—On the
Stromatoporoids, by Prof. H. Alleyne Nicholson, M.D., F.R.S.E.,+
ete.—On the Fossil Sponges, by Dr. G. J. Hinde, F.G.S.—On the
Gasteropoda of the Jurassic Rocks, by Wilfrid H. Hudleston, M.A.,
E.R.S., F.L.S., F.G.S.— On the Oolitic Cephalopoda, by Mr. J.
Buckman.—On the Phyllopoda of the Paleozoic rocks, by Professor
T. Rupert Jones, F.R.S., F.G.S.—On the Entomostraca of the Cre-
taceous formation, by Prof. T. Rupert Jones, F.R.S., F.G.S., and Dr.
G. J. Hinde, F.G.S.—On the Trilobita of the Silurian and Cambrian
formations, by Henry Woodward, LL.D., F.R.S., F.G.S., and On
British Fossil Malacostraca, by the same author.—The Graptolites of
the Cambrian and Silurian formations, by Prof. Charles Lapworth,
LL.D., F.G.S., ete.—The Fishes of the Carboniferous Formation, by
Dr. R. H. Traquair, F.R.S., F.G.S., ete.
. Other Monographs are no doubt forthcoming; but with such an
attractive bill of fare for the present and future years, who, that is
interested in paizontology, can withhold his subscription in support
of so splendid and National a work ?

eee Oise AN) OC Aa aD LE ING-S-
eae
J.—Royan Grotocican Socrery or IneLanp. (ABsTRACT.)
At the Anniversary Meeting on the 17th inst. (February) a paper
was read by Mr. A. B. Wynne, F.G.S., ‘On some recent discoveries
of interest in the Geology of the Punjab Salt Range.”

* Completed and ready for issue on February 15th, 1886. + See ante, pp. 123-128.

182 Reports and Proceedings—

The author refrained from attempting any lengthened treatment
of so large a subject as the geology of this region, having already
contributed various reports and papers to the mass of information
existing in some forty publications which formed the geological
literature of the Range during the last fifty-seven years. Of these
numerous publications, some, if not absolutely mythological, trenched
largely upon the limits of romance; some, like Dr. Fleming’s, were
most valuable records of close scientific observation; and others,
such as Dr. Jameson’s, possessed historic interest, and showed
the difficulties under which the pioneers of geological research
explored that country. This officer related how—in his progress
through the then native territory of the Salt Range, etc., in order to
investigate the causes of those debacles which sometimes carry de-
vastation along the course of the Upper Indus towards the Plains—
his party was beset in the Kotul Pass in the year 1841, his followers
killed, and his personal effects and MS. notes all plundered by
Afridi robbers, he himself escaping with his life only to be im-
prisoned in the fort at Kohat.

Some reference to the position, etc., of the Salt Range was neces-
sary, in order that people at this distance from that locality—some
5000 to 6000 miles—might more readily comprehend the references
to be made. The Range was described as subtending that angle of
Northern India embraced between the Great Himalayan and Suliman
Mountains. It would almost appear to have yielded to the thrust
from these vast masses at each end so as to have assumed curvature
amounting to sigmoid flexure along the strike, in the effort to adapt
itself, so to speak, to restricted limits; while its geological series
forming a semi-anticlinal arch, as a dominant feature, presented a
grand facade of precipices with a general height of 2000 feet, and a
culminating one of over 5000 feet above the sea; overlooking the
plains and deserts to the south, and rising from amongst chaotic
masses, the wreckage and ruins of their own materials. On the
north it sloped more gently beneath the elevated steppe-like plateau
of Rawul Pindi, this having a height of 1600 to 1700 feet above sea-
level.

The range possesses interest geologically, as affording almost the
only opportunity of studying an extensive series, embracing groups
belonging to nearly all the chief periods from early Paleeozoic to
later Kainozoic time; geographically interposed between the re-
markably dissimilar geological areas of Peninsular India and the
Himalaya, each of which had a geological history peculiarly its
own. But the Salt Range was also important by reason of the great
value of its inexhaustible mineral resources; its 500 feet of rock
salt beds, traceable for 130 miles, producing an increasing annual
revenue, some years since estimated at over £382,650 sterling ;
resources which now require a special branch railway and bridge
across the River Jhélum (the ancient Hydaspes) to transport
the salt.

Certain varieties in the relative fullness of the sections displayed
at the centre and at each end of the Range were described, such as

Royal Geological Society of Ireland. 133

the limitation of the “Carboniferous or Productus Limestone” to the
west of the Range: a formation also remarkable for its having afforded
the earliest known Ammonite and the peculiar Brachiopoda Lyttonia
and Oldhamini (Waagen), found only in two other, distant, Kastern
localities, one of them being in China. The last-named of these
forms had been previously described as a Bellerophon, whilst the
rugose interior aspect of the larger valves of Lyttonia had been
regarded as fish teeth.

Attention was called to the absence of any recognizable Devonian
group in the Range and to the recent interesting discovery by Dr.
H. K. Warth, Ph.D., Indian Public Works Department, of what are
claimed to be Devonian fossils ; particularly those of the genus Conu-
laria ; inclosed both as rolled fragments in the matrix and also in
derivative pebbles, within a certain conglomerate-layer, traceable for
miles in the eastern part of the Range above the Mayo Salt Mines,
and included in the upper part of an olive group of rocks referred
by Dr. W. Waagen and the author, when jointly classifying the
Salt Range series, to a presumably Cretaceous horizon. Specimens
of the Conularia were exhibited, which, on being compared with a
published figure of Conularia ornata from the Devonian formation,
presented a striking identity, but no published determination of
these Salt Range forms was as yet known.

It was pointed out that none of the Himalayan or other neighbour-
ing rocks (including those of the Salt Range) contained any established
Devonian horizon, nor any beds with which the pebbles containing
these fossils could be actually identified. Still their pale colour might
suggest that they came from some part of a very pronounced group
in the lower part of the series which had been called the ‘‘ Magnesian
Sandstone Division,” resting upon the Silurian or “ Obolus zone.”
The group had, however, hitherto proved quite unfossiliferous.

Turning unwillingly from this conjecture, if another origin for the
pebbles were to be sought, the next most possible supposition would
be that the parent rock lay to the south and belonged to a land long
since buried beneath the alluvial plains and deserts which stretched
southwards into Scind ~a land perhaps connected with the lost conti-
nent of Lemuria, supposed to have united India with Africa.

One small group of hills called the Korana Hills projects from
the plains of the Chenab river, about forty miles southward of the
Salt Range; these had been visited by both Dr. Fleming and by
Mr. Theobald. Their dark slaty rocks, however, as described by
those gentlemen, afford no clue to the identification of the derived
Conularia pebbles, and present no similarity either to any belong-
ing to the Salt Range.

Instances of the occurrence of other detrital deposits in the Range,
the coarse materials of which were likewise untraceable amongst
the surrounding rocky tracts, were alluded to as strengthening the
supposition of a lost continent to the south, which had furnished hard
metamorphic detritus at various periods in the history of the Salt
Range. These deposits were found immediately overlying the salt
and gypseous marl at the base of the series: again near the Silurian

184 Reports and Proceedings—Belfast Natural History Society.

horizon, and in the “Olive group” with the Conularia layer, but
lower in position. From these Mr. Theobald had obtained at least
one glaciated boulder. A still newer band marked by boulders of a
red granite, the source of which was quite unknown, occurred in the
Tertiary beds above the Eocene Limestone of the Range.

The interest of Dr. Warth’s discovery was enhanced by the con-
spicuous absence of known Devonian rocks among the formations of
Northern India, if not from Indian series generally, and in the hope
that some further determinations would be made, the specimens
kindly sent from the Punjab by Dr. Warth were handed over by the
author to the Museum of Trinity College, Dublin, through its
Curator, the Professor of Geology, etc., W. J. Sollas, D.Sc., LL.D.,
who promised attention to the subject, and noted much similarity
between the contents of the Salt Range Cretaceous deposits and con-
ditions, and those of Cambridge.

IJ.—Bertrast Naturat History Socrery.
Mosasaurus gracilis, Owen, from the Irish Chalk.

At a meeting of the Belfast Natural History and Philosophical
Society, held in their museum on Tuesday, February the 2nd, the
President, W. H. Patterson, Hsq., M.R.I.A., in the Chair, a short
communication was brought forward by Mr. W. Swanston, F.G.S., on
the occurrence of remains of Mosasaurus gracilis, Owen, recently
presented to the Museum by Mr. Turner, Mountain Bush, in whose
quarries at Whitewell the specimen was found. The fossil is por-
tion of the caudal vertebra, consisting of three joints attached, very
closely resembling the specimen figured in the Paleontographical
Society’s Journ. 1851, vol. viii. fig. 8. This is the first record of the
species from Irish strata. The quarries from which the specimen
was obtained are in the White Limestone (Upper Chalk), most pro-
bably the zone of Ammonites Gollevillensis, representing, according to
Professor Ralph Tate, F.G.S., the Upper Chalk of Norwich, and the
““Craie de Meudon,” and some of its fossils point to even a higher
parallel, that of the Maestricht Chalk (Quart. Journ. Geol. Soc.
London, 1865, vol. xxi. p. 86).

IIIJ.—Geroxrocicat Socirty oF Lonpon.
I—Jan. 27, 1886.—Prof. T. G. Bonney, D.Sc, LL.D., F.R.S.,

President, in the Chair.—The following communications were read :

1. “On the Fossil Mammalia of Maragha, in North-western
Persia.” By R. Lydekker, Esq., B.A., F.G.S., ete.

The author alluded to the important memoirs of Messrs. Grewingk,
Pohlig, and Rodler on the Maragha mammalia, and having expressed
the hope that his notice would be regarded as an attempt to assist
rather than to interfere with their work, mentioned a collection of
specimens from Maragha sent by Mr. Damon to the British Museum.
He fully confirmed the conclusions already arrived at as to the
identity of many of the Maragha mammals with those of Pikermi,
and thought that Giraffa atticu, Paleoryx Pallasi, Sus erymanthius,

Geological Society of London. 135

Mastodon pentelici, and Helladotherium Duvernoyi might be added to
the list of species already recorded. He also recorded the French
Felis brevirostris ; a Rhinoceros, apparently allied to R. antiquitatis ;
and R. Blanfordi, of the north-west portion of India and China. The
paper concluded with some observations regarding the relations of
the Paleearctic and Oriental Pliocene faunas.

2. “On the Pliocene of Maragha, Persia, and its resemblance to
that of Pikermi, in Greece; on Fossil Elephant-remains of Caucasia
and Persia; and on the results of a Monograph of the Fossil Hle-
phants of Germany and Italy.” By Dr. H. Pohlig. Communicated
by Dr. G. J. Hinde, F.G.S.

The principal object of the author in making a geological tour
through part of Persia, in 1884, was the exploration of.a deposit
containing Pliocene mammals, discovered thirty years ago near
Maragha, east of Lake Urumia, by Gobel and Khanikoff. The first
part of the present paper gives a brief account of the results of this
exploration, together with a list of the fossils.

The ossiferous deposits near Maragha are of fluvio-lacustrine
origin, and consist chiefly of reddish marls, similar to those of
Pikermi, and formed from the detritus of the voleanic mountain of
Sahend. These Pliocene beds rest upon horizontal Cretaceous strata,
and pass upwards into Pleistocene deposits with erratic blocks.

In the list of fossil mammalia it is shown that several are the
same as Pikermi forms. A Hipparion, probably identical with H.
gracile, is the most abundant. The supposed occurrence of Pleis-
tocene forms, such as Rhinoceros tichorhinus, associated with the
Maragha Pliocene fossils, is probably an error.

The second part of the paper contains notes on specimens of
Elephas primigenius, chiefly in the Museum of Tiflis. The third
part gives very briefly the principal results of the author’s exami-
nation of Pleistocene Proboscidea in the various museums of Kurope,
especially in those of Germany and Italy, and concludes with his
views with respect to Hlephas antiquus, H. melitee (which he con-
siders a dwarf form of H. antiquus), E. meridionalis, E. hysudricus
(which the author considers identical with E. meridionalis), H. prini-
genius, and a few other species, one of which is believed to be new.

3. “The Thames Valley Surface-deposits of the Ealing District
and their associated Paleolithic Floors.” By John Allen Brown,
Esq. Communicated by A. Ramsay, Esq., F.G.S.

he author stated that his paper might be regarded as in some
degree supplementary to that by Colonel Lane-Fox, published in
the Quarterly Journal of the Society in November, 1872. He re-
ferred to Mr. Whitaker’s division of the Thames-valley deposits
into three terraces, namely :—1. The lowest now seen in bends of
the river, 10-20 feet above O. D.; 2. The middle terrace, 20-40 feet ;
and 3. The high-terrace gravel, 50-100 feet, extending up to the
shoulders of the hills, and, according to the author, much higher.
The high-terrace gravels near Haling reach nearly to the top of the
hills forming the inner valley-ridge, the highest point in which is
the Mount at Haling, 204 feet. The summit of this, when excavated

136 Reports and Proceedings—

for a reservoir, was found to be occupied by thick beds of gravel of
different character from the valley-gravels, and not of fluviatile or
estuarine formation ; the same gravel occurs upon other elevations,
and patches of it, appearing here and there, show that it probably
once extended right along the ridge and over Hanger Hill. Similar
materials to those forming this gravel also occur scattered over the
surface of the ground. On the Mount these gravels filled a series
of furrows or channels, beneath which were horizontally stratified
deposits of white sand, loam, and loamy clay, which were pressed
out of the line of deposit where the jagged furrows occurred ; and
from all the characters presented the author inferred that these
deposits were due to the action of ice which had stranded and melted
here, and deposited its burthen of glacial detritus. The author
described the deposits of gravels, brick-earth, etc., at various points
in the district, and noticed that the high-terrace gravels between 60
and 125 feet contain seams of black matter, apparently due to the
decay of vegetable substances, which recur at more or less regular
intervals, and serve to indicate three or four lines of old land-
surfaces. In connexion with these land-surfaces, especially in some
pits excavated in the Creffield Road, about 100 feet above O. D.,
numerous worked flints were found, the characters and mode of
association of which led the author to think that we have here traces
of a regular manufactory of flint implements. He further indicated
the conditions under which he considered their preservation in this
locality had taken place.

II.—Feb. 10, 1886.— Prof. T. G. Bonney, D.Sc., LL.D., F.R.S.,
President, in the Chair.—The following communications were read :

1. “On a new species of Psilotites from the Lanarkshire Coal-
field.” By R. Kidston, Esq., F.G.S.

The specimen described, which was found by Mr. Walter Burns
in 1884, consists of three parallel branchlets with thorn-like projec-
tions on one side only. The author describes these as a form of
Goldenberg’s genus Psilotites, and points out that they have much
resemblance to Dawson’s Psilophyton.

2. “The Melbourn Rock and the Zone of Belemnitella plena, from
Cambridge to the Chiltern Hills.” By W. Hill, Esq., F.G.S., and
A. J. Jukes-Browne, Esq., F.G.S.

The ‘Melbourn Rock,” which was first defined by one of the
authors in 1880, is a band of rocky chalk which forms the base of
the Middle Chalk in Cambridgeshire, and occurs about 80 feet above
the “Totternhoe Stone.” In the present paper it was shown, as the
result of the mapping operations of the Geological Survey, to form
a well-marked and constant feature in the counties of Hertford,
Bedford, Buckingham, and Oxford. In the original description of
the Melbourn Rock it was confounded with the “Zone of Belem-
nitella plena in a remanié condition,” as described by Dr. Barrois ; but
it was now pointed out that the latter horizon is distinct from and un-
derlies the latter. Although the zone of Belmnitella plena has been
very largely removed by erosion in the district described, there is,

Geological Society of London. 137

nevertheless, evidence that this erosion has gone on to a different
extent in each of the localities which have been particularly studied ;
and in some places some of the lower portions of the rocks of that
horizon seem to have escaped denudation.

The microscopical characters of the several varieties of rock form-
ing the Lower and Middle Chalk of the district were described, and it
was shown that the beds containing nodules of a different variety of
chalk which occur below the Melbourn Rock, may have been
formed by the washing away of the finer particles from a disinte-
grating mass of chalk. This mottled chalk and the overlying
Melbourn Rock are very similar to the bed found on the same
horizon in the Richmond well. Somewhat similar beds occur,
however, at other horizons in the Chalk over the district described
in this paper.

3. “On the Beds between the Upper and Lower Chalk of Dover,
and their comparison with the Middle Chalk of Cambridgeshire.”
By W. Hill, Esq., F.G.S.

In introducing the subject of this paper, the author referred to the
divisions of the Upper Cretaceous series given in the ‘ Geology of the
Neighbourhood of Cambridge’ by Messrs. Penning and Jukes-
Browne. The Middle Chalk was there described as separated from
the Lower by the Melbourn Rock, which also appeared to coincide
with a marked paleontological break, and from the Upper Chalk by
the well-known Chalk Rock, this rocky bed, 10 feet in thickness,
being included in the Middle Chalk. The division thus made corre-
sponded exactly with the Turonian of French authors.

The author, giving a description of the Middle Chalk seen in the
cliffs east and west of Dover, stated that the grit bed of Mr. Price,
though much thicker, had all the appearance and structure of the
Melbourn Rock, and this, with less hard, but still nodular, chalk above,
appeared to be the equivalent of the zone of H. Cuvieri in Cambridge-
shire. The zone of Zerebratulina gracilis is well marked in the
Dover cliffs, and is equal in thickness to that zone as described in
the Cambr. Mem., viz. 150 feet. Above this zone the Chalk became
harder, weathered, with lumpy projections, and finally passed into a
series of rocky layers. separated by courses of softer chalk, containing,
however, hard crystalline lumps. The passage to this rocky chalk
was marked by the occurrence of Holaster planus (zone of H. planus).
The rocky layers, extending upward for 80 feet, were marked by the
presence of numbers of Micrasters, ‘‘ Chalk with many Micrasters ” of
the author. His division included all the nodular chalk of Dover,
the “ chalk with many organic remains ” of W. Phillips, and in it were
found the fossils recorded as peculiar to Chalk Rock in the Geol. of
Cambridgeshire. It appeared divisible into two zones; the lower,
15 feet, with Micraster breviporus (zone of M. breviporus), may be
considered by some to be an extension of the zone of A. planus, the
form which marks the passage from the soft to the hard chalk. In
the remainder M. cor-testudinarium was common (zone of M. cor-
testudinarium).

Seen in thin sections under the microscope, the structure of the

138 Highbury Microscopical and Scientific Society.

hard beds which mark the limits of the Middle Chalk was stated to
be very similar.

In conclusion, the author considered that the divisions of the
Middle Chalk, as set forth in the Cambr. Memoir, are well shown
in the cliffs of Dover; but the hard beds which appeared to him the
equivalent of the Chalk Rock, and mark the upper limit of Middle
Chalk, attaining a great development at Dover, it became necessary
to examine the paleontological position of that bed to which the name
“Chalk Rock” was given by Mr. Whitaker. Having studied Mr.
Whitaker’s description given in the “Geology of the London Basin,”
and having examined exposures of this rock between Cambridge and
the Thames, he came to the conclusion that there was probably more
than one bed to which the name Chalk Rock might be applied, and
that these, probably not all persistent, may occur at different paleeon-
tological horizons. He therefore proposed to take the zone of
H. planus as the top of the Middle Chalk; although this zone was
difficult to identify inland, from the paucity of its fossils, the base of
the overlying zone was well marked by the abundance of Micrasters
and other forms, which appear to him more closely allied to Upper
than to Lower Chalk.

He believed that while the Chalk Rock seen at Henley may be
considered the summit of the Middle Chalk, the Chalk Rock of Cam-
bridgeshire, though convenient for marking the summit of the Middle
Chalk of that county, included that which was really the upper part
of the zone of H. planus and the base of the true Upper Chalk, the
equivalent of Chalk with many Micrasters of Dover.

He would therefore consider the Middle Chalk of Dover to be that
included from the base of the grit-bed to the summit of the zone of
H. planus. Its thickness was 242 feet at Shakespeare’s cliff. He was
indebted to M. Curry, Exsq., of Dover, for this accurate measurement.

IV.—Hieupury Microscorican anp Screntiric Socrery.—At a
numerously attended meeting of the members of this Society, held
on Thursday, the 28th January, at Mr. EH. P. Sell’s, 63, Highbury
Hill, the President, James Smith, Hsq., F.L.S., F.R.A.S., moved,
and Mr. Fitch seconded, the following resolution :—

“That the Members of the Highbury Microscopical and
Scientific Society having heard with the most sincere regret
of the death of their Vice-President, Mr. J. B. Jeaffreson,
M.R.C.8., desire to place upon record their deep sense of the loss
they have sustained, and to express their appreciation and
admiration, not only of his attainments as a scientific man, and
the able manner in which he discharged the duties of Presi-
dent, but more especially of his character as a kind and
sympathetic friend; and they furthermore desire that the
Secretary do, in a suitable manner, convey to Mrs. Jeaffreson
and the family the assurance of their heartfelt sympathy with
them in their sorrow.”

Correspondence—Mr. John Young. 139

CORRESPONDENCE.

“ CONE-IN-CONE.”’

Str,—I am glad to observe in the short article on ‘“Cone-in-cone,”
by Professor Newberry, M.D., in the December Number of the
GeoLocicaL Macazrne for 1885, that he at one time was inclined to
look upon that structure as due to ‘the escape of gases through
a pasty medium.” JI think that if he had the opportunity of studying
the large series of specimens that I have now assembled, and the
transparent sections of the cone structure that I have prepared, he
would still be inclined to favour that view as an explanation of the
phenomena that they present, rather than the one he now adopts,
viz. ‘an imperfect crystallization” of the deposit in which it is
found. Professor Newberry, after referring to a number of cases
of cone-in-cone structure that had come under his observation (some
of which apparently differ from what I have described), concludes
by stating that these examples ‘‘seem to me to be incompatible with
the theory that cone-in-cone is caused by pressure, or the escape of
gases, and appear rather to confirm the conclusion that it is due
to an impeded tendency to crystallization.” He, however, in the
article in question, offers no evidence in support of this crystallization
theory, nor does he explain in any way the peculiar structure and
arrangement of the cone layers. Those supporting a crystallization
theory have not referred to any known law of crystallization, which
would account for a structure agreeing with what is seen in the best-
preserved specimens of our Scottish cone-in-cone, or which would
satisfactorily explain all that is represented in the external structure
of the cones, and their terminations on the surface of the bed, as is
briefly noted in the short abstract of the paper I read to our Glasgow
Geol. Soc., and printed in the June Number of the Grou. Mac.
for 1885. In the abstract, to which I would refer your readers,
I have endeavoured to indicate what is seen in both the internal and
external structure of the cones, but which I explain more fully in
my paper, and I do not think that in either I have ventured
to hazard any explanation that is not fully warranted by what
the specimens reveal.

During the progress of my investigations, I have not wholly
relied upon my own judgment in coming to the conclusion that the
cone-in-cone structure was due to the escape of gases generated in
the sediment, but that from time to time I have had the opportunity
of submitting specimens and sections of the structure to Dr. Young,
Prof. of Geology ; Prof. Sir William Thomson, President of the
Glasgow Geol. Soc., and his brother Prof. James Thomson, who has
paid some mieatod to rock structures; likewise to Mr. Ferguson,
Prof. of Chemistry in this University, and to others, on whose

opinion I could rely, and I am pleased to be able to state, that they
are all inclined—so far as the specimens noticed in my paper are
concerned—to agree to the explanation I have given as to the pro-
bable origin of the structure. They also agree with me in thinking
that none of the agencies to which cone-in-cone structure has been

140 = Correspondence—Sir R. Owen—Mr. W. J. Black.

usually ascribed—such as crystallization, pressure acting on con-
cretions in the process of formation, or chemical deposition of
sediment—will ever explain the points of structure and other
characters seen in the specimens that I have selected for description.

Hunrerr1an Museum, JoHN YOUNG.
University, Guascow, Jan. 5th, 1886.

ON A NEW PERISSODACTYLE UNGULATE FROM WYOMING.

Str,—In the GerorogicaAL Magazine for February, 1886, it is
stated, p. 50, that no Perissodactyle mammal was known “ to possess
tubercular teeth.” Professor Cope does not supply the characters to
which his term ‘tubercular’ is applicable. If he would kindly
refer to p. 362 of my <“ Paleontology” (2nd ed. 1861), enlarged
views of the molars of both jaws of a genus of Perissodactyles
(Pliolophus), from Eocene, will be found. A still earlier example
of ‘tubercular’ molars, in the genus Hyracotherium, is described and
figured in “ British Fossil Mammals and Birds,” 8vo., 1846, p. 422,
cut 166: also from the ‘ London Clay.’

Permit me to add that my estimate of the claims of Elephants and
Mastodonts to rank as an ‘Order’ rests upon the multilamellate
structure, size and succession of their ‘ grinders,’ subordinate to
which dental character may be cited a vertebral one, necessitating
their special instrument the proboscis. The pentadactyle character
is common to Proboscidia with many Rodent genera, as well as with
the older Hocene members of the Coryphodont family, characterized
by Lophiodontoid modifications of the true molars. These teeth
afford the truest indications of affinity in the Ungulate series. The
diminutive Rhinocerontoid represented by the genus Hyraaw as little
determines by molar characters an ordinal distinction form Acero-
therium as do the modifications of teeth and limbs in Bradypus
support an ordinal distinction in the Megatherioid family.

RicwarpD OWEN.

THE “ALASKA GLACIER.”

Str,—In reference to the description of the Great Glacier in
Alaska, in “Nature” (Jan. 28th, 1886), 1 may draw attention to
the letter of Mr. J. Melvin in the same number, which would appear
to throw light on the subject of the progressive changes in it. The
ridges delineated in the diagram of the Glacier as lying between the
body of the Ice and the hill-side would seem to be analogous to the
Parallel Roads in Norway valleys, only they are formed on the flat
instead of the slope.

The body of the Glacier seems evidently to have contracted itself
in consequence of loss of substance by melting underneath, and
withdrawn itself by these decided starts from the hill-side, and left
the ridges as relics of its foundations on the bottom of the valley.

Probably the Glacier ages ago was quite flat on the top, and
reached across to the top of the morainic slope on the hill-side, and
it has since lost great bulk below by ground melting, which by
overstretching has caused the cracks or crevasses on the upper

Correspondence—Prof. E. D. Cope—Mr. W. Davies. 141

surface by consequence of change of shape from the level to the
convex.

The tunnel, opening out at the butt of the Glacier on to the sea-
beach, has doubtless been the main owélet for the ground melting, and
its arched shape may also be deemed significant of the process of
convexity adopted by the contraction of the Glacier from side to side.

The mechanism may be likened to the curling in of the sides of a
piece of wood or paper when the flat side is exposed to the fire,-~
and it would be all the greater if the other surface were damped,
just as the upper surface of the Glacier would be by the rainfall or
snowfall of the season. Mr. Melvin’s explanation of the formation
of the Parallel Roads in Norway valleys may therefore be pro-
visionally proposed to be applied to the phenomena of other Glacier
actions, but there are many of these probably that have not convex
roofs, nor ground tunnels like the Alaska Glacier. W. J. Brack.

Unirep Service Crus, Epinpurcu, February, 1886.

EDESTUS AND PELECOPTERUS, ETC.

Srr,—I observe in your interesting article on the Edestus Davisii,
in the January Number of the GronocicaL Macazine, that you refer
to the genus Pelecopterus, Cope, as identical with Ptychodus, Agass. ;
the pectoral spines representing the former being supposed to belong
to the animal whose teeth have given origin to the second name.

My studies of these fishes have led me to entertain a different
opinion from the above. Ptychodus, being a shark, is not likely to
have a pectoral arch and fin like that of Pelecopterus. Moreover,
these pectoral spines have been frequently found associated with the
jaws and teeth of the “ snout-fishes ” of the Kansas Chalk, which
have been described under the generic head of Hrisichthe, Cope.
Several species are known (see Bulletin U.S. Geol. Survey Terrs.
ili. 1877), and one of them is probably the Xiphias Dixoni of Agassiz,
from the Chalk of Sussex, England. These genera cannot be re-
ferred to any of the existing orders of fishes, on account of the
peculiar structure of the pectoral arch. I have therefore placed
them in an especial one, the Actinopteri (see Proceedings Amer.
Assoc. Ady. Science, 1877(78), p. 299). H. D. Core.

PHILADELPHIA, Jan. 26, 1886.

NOTE ON THE ABOVE, BY MR. W. DAVIES, F.G:S.

Professor Cope is, I think, mistaken in assigning Xiphias Dixoni
to Agassiz. The name first appears in a paper by Dr. Leidy “On
Saurocephalus and its Allies,” in the Trans. Am. Phil. Soe. vol. xi.
p- 91, where the name was given to the prolonged ethmoid bone
referred by Sir Philip Egerton to Saurocephalus lanciformis, as then
understood.

In that paper Dr. Leidy proves that the teeth assigned by Agassiz
to the Saurocephalus of Harlan had no relation to that genus, and he
refers the jaws and teeth from the English Chalk to a new genus;
under the name of Protosphyrena, Leidy. 'The “rostral” bones
described by Sir Philip Egerton, he contended did not belong to

142 Correspondence—W. Alphonse Favre.

Protosphyrena, but to a species of Xiphias to which he gave the
trivial name of X. Dixoni. Subsequently, Prof. Cope described his
genus Hrisichthe, which certainly embodies both of Leidy’s species.
I may mention here that the prolonged ethmoids are found in our
Chalk, Upper Greensand, and Gault; and here also are found (and
in no other deposit) the peculiar fin-rays referred to Ptychodus by
Agassiz. From this association the inference is natural, that the
ethmoids and fins belong to the same species of fish, viz. the
Protosphyrena of Leidy, Erisichthe, Cope. (See paper by W. Davies,
F.G.8., on Saurocephalus lanciformis of the British Cretaceous
Deposits, with description of a new species, Guoxt. Mac. 1878,
Decade II. Vol. V. p. 254, Pl. VIII.)—W. D.

A MONUMENT TO HORACE-BENEDICT DE SAUSSURE.!
(Born at Geneva, 1740; Diep 1799.)

Sir,—Chamounix is preparing to erect a monument in memory of
our fellow-citizen H. B. pz Saussure,

This memorial will be placed at the foot of Mont Blanc, whose
lofty summit the illustrious savant indefatigably reached, not far
distant from the Col du Géant, where, in pursuit of science, he
encamped amidst snow and ice for sixteen days. In short, it will
adorn the central position from which all the Alpine excursions of
this intrepid explorer originated.

It is impossible to enumerate here all the titles acquired by De
Saussure in the scientific world. Let us only remember that he was
an eminent physician, a distinguished meteorologist, a charming
writer, who devoted thirty of the best years of his life to the study of
those Alps whose beauties he revealed with precision and poetic
feeling, and as a conscientious and indefatigable investigator he
became one of the founders of modern geology by placing that
science on its true basis—observation.

The proposal to raise a monument naturally met with the most —
sympathetic support when it was presented to the members of the
Alpine Clubs of all countries, who met at Chamounix in August,
1883, and at Turin in August, 1885.

Since then an Executive Committee has been formed, composed of
Messrs. Folliguet (Mayor of Chamounix), Tairrez Payot, Thévenet,
President, and Maillot, Secretary of the Mount Blanc section of the
French Alpine Club, soliciting them to assist with their subscriptions
the erection of a monument.

Switzerland and Geneva in particular would wish to be associated
with the homage rendered to the merits of our eminent citizen.
Above all, the people of Geneva ought to be interested in a monu-
ment designed to preserve the memory of a man who shed such
lustre on our city and our ancient Academy. One knows, in fact,
that in spite of his numerous travels and his absorbing scientific
studies, he found time during many years to occupy a modest

1 Among various writings, his most important work is the record of his Alpine
observations: ‘‘ Voyages dans les Alpes,” im 4 vols. 1779-96.

Correspondence—A Bust to Prof. O. Heer. 143

philosophical chair in his native town, where he exhibited all the
high qualities of his exalted intellect.

It is equally well known that he interested himself all his life in
our scientific and literary institutions as well as the intellectual and
material development of our ancient Republic. Many of his
writings, unknown doubtless elsewhere, were received here, and the
Society for the Advancement of Art founded by him still continues
a work to which he was devoted.

Even when this monument to his memory shall have been raised
on foreign soil, Geneva will show its gratitude towards those who
have taken the initiative in this demonstration, and will honour those
who take part in it.

It is with this firm assurance that the Committee at Geneva is
formed to collect subscriptions.

The inauguration of the memorial is projected for the 38rd of
August, 1887, that being the centenary of H. B. de Saussure’s
ascent of Mont Blanc. There is therefore no time to be lost that it
may be finished by that date. It is important that the Initiative
Committee at Chamounix should know as soon as possible the sum ~
they have at their disposal, in order to decide what form the monu-

ment should take. ALPHONSE FAvRe,
6, Ruz pes Grances, GENEVA, President of the Swiss
20th December, 1885. Geological Commission.

A MONUMENT FOR PROFESSOR OSWALD HEER OF ZURICH.

Str,—Two years have passed since Death carried off one of the
most eminent naturalists of our age—Oswald Heer. He died on the
27th of September, 1883. he fitting moment seems to have arisen
to render Dr. Heer a public acknowledgment and to raise a lasting
monument tohis memory. Weare glad to be able to inform you that
a sculptor of Zurich, M. Hérbst, has modelled a bust in clay, which
gives the naturalist’s expression in the most pleasing manner.

The work of Heer was wide-spread. Although truly Swiss at
heart, and studying with delight the primitive history and flora of
his native land, his researches extended far beyond the limits of his
own country. He had become one of the highest authorities on the
domain of vegetable paleontology, and from all parts of the world,
from the islands of Sunda and from “hyperborean” lands, from
Portugal and Eastern Siberia, from the New World as well as the
Old, he gathered materials for his researches, and specimens came
for identification. The works of Heer on the fossil flora of the
Polar regions have placed him among the foremost ranks as one of
the founders of modern botanical geography ; for to him, and him
alone, is due the merit of having discovered, by studying the mar-
vellous Tertiary flora of Greenland, Spitzbergen, and Arctic America,
facts of the utmost importance to science. His name will perpetu-
ally remain united with those who have explored Arctic regions,
his researches will long form the basis of our knowledge of pre-
historic climates.

Feeling assured of the eminently international character of Heer’s

144 Obituary—Prof. A. von Lasaulx.

work, we confidently appeal to all to raise a worthy monument to
his memory.

It is proposed that this monument should consist of a marble bust
on a stone pedestal, protected in a suitable manner from the in-
clemencies of the weather, to be placed in the Botanical Gardens at
Zurich, on the spot where Heer’s energy was so well displayed.
The price of the memorial would reach about 5000 franes.

Besides which, the sculptor, M. Horbst, is prepared to execute, for
150 franes each, plaster casts of the original. If you desire one of
these copies, have the goodness to inform us, when sending your
contribution. Subscriptions will be gratefully received by Dr. C.
Schroter at Hottingen, Zurich. They may be sent direct, or through
the medium of the undersigned.

Prof. Dr. A. Mousson, Polytechnikum, Zurich.
Prof. Dr. C. Cramer, A i

@iSt Ee OEAS Ea

PROFESSOR A. VON LASAULX Pu.D.

We deeply regret to have received tidings of the death of this
distinguished German Geologist and Mineralogist, which took place
at Bonn, on the 25th January last, after a short illness. Dr. Von
Lasaulx was only in his 47th year; yet he had been the author of
a remarkably large number of Memoirs on petrological subjects, as
well as of more solid works, of which, perhaps, the joint work on
Ktna of Sartorius von Waltershausen and himself is the most
splendid example. In 1876 Dr. von Lasaulx, in company with his
friend Dr. Ferdinand Roemer, of Breslau, visited the British Isles ;
and was present at the meeting of the British Association in Glasgow
in that year. On his return to Bonn, he published an account of
his wanderings, in the form of a handsome hook, “ Aus Irland,
Reiseskizzen und Studien,” in which the physical features and
geological structure of the districts visited are closely noted and
graphically described, together with the mineral characters and
composition of many of the rocks as determined under the micro-
scope; of these, the most important was the discovery of tridymite
in the trachytic rocks of Antrim (Petrographische skizze aus Irland ;
mineralogischen und petrographischen Mittheilungen, Wien, 1878,
p. 410). The volcanic rocks of Bonn and the neighbourhood
afforded a rich field for the petrological investigations of this lamented
naturalist, of which he made abundant use. (opal.

We regret to record the death (on the 16th February, from heart-
disease) of Mr. W. W. Leighton, who, since the year 1867, has
filled the office of Clerk to the Geological Society of London, and
has during 19 years been a most faithful and valued servant to the
Society.

Geol.Mag.1886. | Decade III Vol. III. PI. IV.

#.C.Knight del etlith. West, Newman & Comp.

Fossil Ostracoda from Colorado.

THE

GEOLOGICAL MAGAZINE.

NEWS ERIESE DECADES iia VO Lay aiil:

No. IV.—APRIL, 1886.

Ore eG pENEAwE) -Asry ans Canara Ss

—_+>—__

T.—On Some Fosstn OstracopA FROM COLORADO.
By Prof. T. Rupert Jonss, F.R.S., etc.
(PLATE IV.)!

N December last Dr. C. A. White, Palezeontologist to the U.S.
Geological Survey, sent me a small packet of siliceous Ostracoda,
obtained by dissolving in dilute acid some pieces of an impure lime-
stone from the Jurassic “‘Ailantosaurus. Beds” near Canon City,
Colorado. These strata are of freshwater origin; and, besides the
wonderful Dinosaurian and Mammalian fauna, which Prof. O. C.
Marsh has published, they contain, Dr. White informs me, Unio,
Limnea, Planorbis, and Valvata, all of modern types. In the impure
limestone with Ostracods, and in associated layers, these Gasteropods
are found also in a silicified state, and the Dinosaurian fossils occur
both above and below them.

In January of this year I received also from the U.S. Geological
Survey, through Dr. A. C. White’s kind agency, a piece of the hard
limestone itself, for the examination of the microzoa not treated with
acid. Some fragments, carefully crushed, yielded free specimens,
but not so many nor so perfect as those obtained by acid-solution of
similar pieces. By careful manipulation my friend Mr. C. D. Sherborn
succeeded in finding some that showed traces of ornament by the
presence of the whitish matrix (siliceous) in rows of little pits and
in slight furrows similar to those on the Purbeck Metacypris Forbesii.
Consequently these little siliceous organisms are not all internal casts,
but some are perfect carapaces.

On the examination of thin sections and decalcified slices, many
sections of Ostracodous bivalved carapaces are recognized, also
crushed valves and numerous fragments. The test is often apparent,
replaced by silica. No limbs nor internal organs are visible within
the whole (bivalve) tests; only groups of brown granules, arranged
somewhat concentrically, as also in the neighbouring siliceous in-
fillings of Limnea, and other Gasteropods, and in the chalcedonic
(agate-like) infillings of rifts and other spaces in the matrix. In
some instances the carapace-valves are absent, and the first inside
layer of chalcedony imitates the shell. On being decalcified, a slice

1 This Plate was drawn with aid of a grant from the Royal Society for the illus-
tration of fossil Ostracoda,

DECADE II,—VOL, UI.—No. IY. 10

146 Prof. T. Rupert Jones—Fossil Ostracoda, Colorado.

loses much of its brownness; but some of the silica still retains a
brown tint.

1. Meracypris Forzest, Jones. Plate IV. Figs. 1a, 16, 1e.

M. Forbesii, Jones, Quart. Journ. Geol. Soc., vol. xli. 1885, p. 345, pl. 8,
figs. 11-16 (including var. verrucosa); M. Forbesii, Jones, in Bullet. U.S. Geol.
Surv. February (?), 1886.

Comparing our Figs. la, 1b, 1c, of the American Metacypris with
figs. 18 and 15 of plate 8 referred to above, we see no special
difference except that the antero-dorsal (nuchal) constriction is
stronger in the former two figures, and the valves are rather more
swollen in their posterior moiety.’ The siliceous specimens figured
do not show the ornament seen in their English representatives; but
some that have been beaten out (not separated by acid) show the
characteristic ornament, as stated above. Not rare.

For the proportions of this and the other species, see the Table at
the end.

2. Meracypris Bpapyt, sp. nov. Pl. IV. Figs. 2a, 2b, 2c.

M. Forbesit [var.], Jones, in Bullet. U.S. Geol. Survey, February (?), 1886.

“This is even longer in proportion than our most oblong form,”
such as fig. 11, pl. 8, Q.J.G.S. vol. xli.; and the constriction is very
strong, being deep, curving forward, and reaching quite across the
valve.” The posterior moiety of each valve is relatively less swollen
than in M. Forbesii; but the convexity of the anterior portion is
more pronounced, and more markedly defined by the transverse
sulcus ; and, owing to the curve of the furrow, the hinder portion
has an almost round convexity. A pimple on the centre of this
part, and some few elsewhere, show an analogy to the warty con-
dition of M. Forbesii, var. verrucosa, op. cit. pl. 8, figs. 12 and 15,
Not rare. ;

I propose to name this, as a distinct species, after my friend Dr.
G. 8. Brady, F.R.8., who first recognized the genus Metacypris (op.
cit. p. 344). ;

3. Meracypris Wuiret, sp. nov. Pl. IV. Figs. 3a, 30, 8¢.

Metacypris, sp. Jones, in Bullet. U.S. Geol. Survey, February (?), 1886.

“This form is narrow [relatively ], oblong, and compressed ; and
bears a distant resemblance to ‘ Oypris (?) conculcata,’ Jones, Quart.
Journ. Geol. Soc., vol. xvi. 1860, p. 266, pl. 16, figs. 3a and 3b”
(Se, young?). Valves oblong, nearly straight above and below,
almost equally rounded at the ends; compressed in front, thicker
behind. Impressed at the anterior third with a shallow sulcus, and
with a faint hollow near the anterior hinge. Hdge-view narrow-
ovate, sharp in front, obtuse behind, and somewhat undulate at the
sides by reason of the slight depressions. Not rare.

1 Some of the English specimens are more constricted than shown in the figures
and descriptions, op. cit. p. 845.

* The transverse sulcus impressed on or near the mid-dorsal region of each valve
is characteristic also of Limnicythere and occurs in some other recent Ostracods of
estuarine and freshwater habitats, namely, Cyprideis (Cytheridea), and one Cypris
(C. gibba, Ramdohr).

Prof. T. Rupert Jones—Fossil Ostracoda, Colorado. 147

This species is named after Dr. A. C. White, Paleontologist of
the U.S. Geological Survey, Washington, who kindly submitted
these interesting Colorado specimens for my examination.

Another fossil Metacypris was described and figured some years
azo as Cypris strangulata, Jones (Quart. Journ. Geol. Soc. vol. xvi.
1860, p. 187, pl. 10, figs. 73a, 6, c, d, comprising probably two
species), from the Tertiary beds of Central India, at Pahadsingha
and Butara, both in the Province of Nagpur (op. cit. pp. 165, 166).

4, DARWINULA LEGUMINELLA (HE. Forbes). Pl. IV. Figs. 4a, 4b, 4c.

D. leguminelia (E. Forbes), Jones, Q. J. G. S. vol. xli. 1885, p. 346, pl. 8,
figs. 30 and 31; and in Bullet. U. S. Geol. Surv. February (?), 1886.

It is evident that, judging from the shape and size of the carapace,
we must refer these American specimens, which are not rare, to the
same genus and species as determined for the similar little Purbeck-
Wealden Ostracods of England and Hanover.

Darwinula Stevensoni, Brady and Robertson, lives at present in the
brackish water of tidal rivers, and has been found fossil in late
Tertiary deposits belonging to the Forest-bed series of Suffolk.
D. Berniciana, Jones (Proceed. Berwicksh. Nat. Club, 1884, vol. x.
p- 325), is a Lower-Carboniferous form in Northumberland, and
D.? pungens, J. and K., occurs in the Coal-measures of Scotland.
Another probable Darwinula is the Cypris (?) Allportiana, Jones, from
the Neocomian ! freshwater beds near Bahia, in Brazil; seeQ. J. G.S.
1860, vol. xvi. p. 267, pl. 16, fig. 16.

5. Cypris Purseckensts, E. Forbes. PI. IV. Figs. 5a, 5b, 5e.

m Cypris Purbeckensis, E. Forbes. Jones, Q. J. G. S. 1885, vol. xli. p. 347, pl. 9,
gs. 1-6.

The figured carapace, Fig. 5a, corresponds with fig. 5, in pl. 9,
Q. J. G.S.; and Fig. 5b nearly with fig. 4 of that plate, in which
various forms of this species are given. It is common in the English
Purbeck beds, but rare and smaller in the sample from Colorado.

6. CytueripEIs Marsutt, sp. nov. Pl. 1V. Fig. 6a, 60, 6c.

This carapace, apparently perfect (showing the translucent edges
of the closed valves), approaches very near to Cytherideis trigonalis,
Jones, Monogr. Tertiary Entom., Pal. Soc. 1856, p. 47, pl. 2, figs.
2a-2h; but the curve and slope of the front margin differ, this end
being slightly blunter in the American form. The greatest con-
vexity, also, is rather ventral than along the middle. Rare.

This species is named after the eminent paleontologist who has
worked so enthusiastically and successfully in these highly interesting
fossiliferous deposits of the Far West.

7. CYTHERIDEA? ATLANTOSAURICA, sp. nov. Pl. IV. Figs. 7a, 7b, Te.

An oblong, convex carapace, round-ended, with the anterior rather
higher (broader) than the other end, and slightly oblique. _ Valves
somewhat undulate, being faintly impressed in the postero-dorsal

' Referred to the Neocomian by Dr. A, .C, White in a work prepared by him for
publication by the Brazilian Government.

148 J. W. Davis—Carboniferous Fish-remains.

region. The convexity is greatest along the ventral region, causing
this part to swell out a little beyond the ventral margin. Edge view
oval with sharp ends; end view short-ovate, acute above, broad
below. Rare.

This distantly resembles the smooth variety of Cytheridea torosa
(Jones), Monogr. Tert. Entom. 1856, p. 21, pl. 2, fiz. le; var. teres,
Brady (Trans. Linn. Soc. 1868, vol. xxvi. p. 425, pl. 28, figs. 7-12 ;
Aun. Mag. Nat. Hist. 1870, ser. 4, vol. vi. pp. 21, 22, note; Monogr.
Post-Tert. Entom., Pal. Soc. 1874, p. 178, pl. 7, figs. 1 & 2). The
anterior hinge, however, is more definite, though not prominent, the
shape is rather more truly oblong, and the sub-medial impression is
not so strong. As I have not seen an interior of a valve, I cannot
say if this American species belongs to Oytheridea or to Cytherideis.

TABLE OF PROPORTIONS.
Length. Height. Thickness,

Metacypris Forbesit, Fig. 1 .......cecceccsceseneene 15 9 11
MeBrad ye MEN O' Die are seenee eee ee cE ae eee 18 10 10
SUES UY OGUGES IONE S} eccoaccedbooeuoscousdenoneodacdsoose 18 9 8
Darwinula leguminella, Fig. 4......cceccceeceeeees 14 6 5
Cypris Purbeckensis, Fig. 5 .......... a eauaseentar 13 6 5
Cytherideis Marshii, Big. 6 .........000 4 weeceeeee 13 7 5
Cytheridea ? atlantosaurica, Fig. 7 ..........0000 12 6 6

If these proportional numbers be divided by 15, the result will
be linear dimensions in a millimétre and parts of a millimétre; the
figures being magnified 15 diameters.

As the anterior extremity is placed upwards in the figures, the
height of the valves appears as width on the plate.

The species Figs. 1, 2, 3, 4 are abundant; those shown by Figs. 5,
6, and 7 are rare.

EXPLANATION OF PLATE IV.
(The figures are magnified 15 diam.)
Throughout a is the side view; 4, edge view; c, end view of the bivalved carapace.
Fic. 1. Metacypris Forbesii, Jones; a, right valve outwards.
. M. Bradyi, Jones; a, right valve outwards.
. M. Whitet, Joues;,a, left valve, outwards.
. Darwinula leguminelia (K. Forbes) ; a, right valve outwards.
. Cypris Purbeckensis, KE. Forbes ; a, left valve outwards.
. Cytheridets Marshii, Jones; a, left valve outwards.
. Cytheridea ? atlantosaurica, Jones; a, left valve outwards.

NIADOFowhbWr

II.—Nortes on A Coutection or Fossitz Fiso-Remains FROM THE
Mountain Limestone or DERBYSHIRE.

By James W. Davis, F.G.S.

AM indebted to Thos. Parker, Esq., of Oldham, for the oppor-
tunity he has afforded me of examining his large collection of
fish-remains from the Carboniferous Limestone of Derbyshire. The
specimens have been obtained from quarries near Chapel-en-le-Frith,
in the N.W. of the county. They are for the most part in a beautiful
state of preservation, though some of the more fragile specimens are
only obtained with the most careful manipulation on account of their
liability to fracture. The fossils are creamy-white in a light-coloured
crystalline limestone matrix.

J. W. Davis—Carboniferous Fish-remains. 149

The fauna of this district affords some features of peculiar interest.
There is an entire absence of fin-rays, and of the sharply-pointed
conical teeth like Cladodus, a negative evidence of their intimate
relationship where present. There are two genera of Petalodontide,
three of the Copodontide, five of the Cochliodontide, one of Pleu-
rodus and one of Psammodus. Of all these only one species, Psephodus
magnus, Agass., has been previously recorded from Derbyshire.
Besides P. magnus, the following fish-remains have been chronicled
either in M‘Coy’s British Palaeozoic Fossils, or in the Fossil Fishes
of the Carboniferous Limestone series of Great Britai, in the Trans-
actions of the Royal Dublin Society, by the present writer :—

Acondylacanthus (Leptacanthus, M‘Coy) Deltodus aliformis, Agass.
junceus, M‘Coy. Deltoptychius acutus, Agass.
Cladodus mirabilis, Agass. - Pecilodus foveolatus, M‘Coy.
Cladodus striatus, Agass. Petalodus acuminatus, Agass.
Pristicladodus dentatus, M‘Coy. Cheirodus pes-rane, M‘Coy.

Petrodus patelliformis, M‘Coy.

To this list is now added twelve species, five of which have not
previously been described; they are comprised in the following
descriptions, to which are added such observations as appear necessary
to indicate peculiarities of form or structure.

Family Peratopontipm, Newberry and Worthen.
Genus Petalodus, Owen.
Owen, Odontography, p. 61 (1840).
Davis, Trans. Roy. Dublin Soe., n.s. vol. i. p. 429 (1883).
Petalodus Hastingsie, Owen.
Odontography, p. 61, pl. xxii. figs. 3, 4, 5.
Davis, /.c. p. 493, pl. lix. figs. 16-21.

A considerable number of the teeth of this species have been found
varying in size as well as in form. An average tooth apparently of
full size is 0°35 inch across the crown ; the height of the latter being
0-15 inch. The base is nearly double the height of the crown.
Whilst agreeing generally in form with the species from the Mountain
Limestone of Armagh, it differs in the greater area occupied by the
imbricating ridges at the base of the crown; whilst the former
possess five or six folds or ridges, the specimens from Derbyshire
have nine. Some of the examples are broader across the crown,
than the average tooth already named, and the height of the crown
is less, very thin, and almost straight. This may be due to greater
wear, the coronal surface being reduced from the normal convexity
to a more or less straight edge ; or, it may indicate a different species.
The broad form closely resembles in some particulars the specimens
of Petalodus inequilateralis from the Limestone of Wensleydale.

Genus Petalorhynchus, Agass. MS.
Davis, Trans. Roy. Dublin Soe. n.s. vol. i. p. 516 (1883).
Petalorhynchus psittacinus, Agass. MS.
Davis, /.c. p. 516, pl. lxi. figs. 12-16.
Hitherto the teeth of this species have been found only in the’
Mountain Limestone at Armagh and the Carboniferous Series near

150 J. W. Davis—Carboniferous Fish-remains.

Glasgow. The specimens from Derbyshire present as great a variety
in form as those from Armagh so far as the series extend, and there
can be little doubt that the species is the same. In one or two of
the best-preserved examples, the depth of the tooth only exceeds the
breadth by one-fifth, and consequently is probably from the posterior
part of the mouth; the sigmoidally curved folds of the ganoine,
extending across the external surface at the base of the crown, are
only three in number. In the species found at Armagh there are
four or five imbricating folds. The beak-like cutting-edge of the
crown is somewhat deeply and broadly serrated along each lateral
margin in some of the specimens; in this it also diverges from the
types and offers a superficial resemblance to the teeth of the genus
Ctenopetalus. Minute vertical furrows extend from the cutting
margin downwards over the anterior surface of the crown.

Palatal Teeth of Fishes from the Carboniferous Limestone, Chapel-en-le-Frith,
Derbyshire. Coll. Thos. Parker, Esq.

Family Cocuttopontipm, R. Owen.
Streblodus oblongus, Agass. MS.
Davis, Trans. Roy. Dublin Soc. n.s. vol. i. p. 424, pl. lui. figs, 1-4 (1883).

Remains of the teeth of this species are not uncommon. They
are usually detached, and owing to their extreme brittleness, and the

J. W. Davis—Carboniferous Fish-remains. 151

difficulty with which they are developed from the matrix, they are
often fragmentary. An example exhibiting the series of three teeth
covering a ramus of the jaw has not yet been discovered. The large
posterior teeth are most commonly met with. They are much smaller
in size than those of the same species from the Mountain Limestone
of Armagh, generally about 0:5 inch in length and 0:3 in breadth.
They possess the characteristic convolution of the genus. The
enamelled surface of the crown is exquisitely and perfectly pre-
served, and in most instances does not exhibit much trace of being
worn by attrition, from which it may perhaps be reasonably inferred
that they are the teeth of a young individual.

Genus Psephodus, Agass, MS.
Davis, Trans. Roy. Dub. Soe. ns. vol. i. p. 4388 (1883).

Psephodus magnus, Ag.
Trans. of the Royal Dublin Society, ser. ii. vol. i, p. 439, pl. lv. fig. 1-14,

Several examples of this species have been found. They do not
materially differ from the specimens described from the Carboniferous
Limestone of Armagh. The largest tooth, probably occupying a
median position on the jaw, is 0-85 inch in greatest diameter, more
or less pentagonal in outline, the upper surface highly convex, and
the under one correspondingly concave.

A second specimen consists of two teeth joined together similarly
to those represented in the memoir named above, pl. lv. fig. 4, the
two upper and larger teeth; the Derbyshire ones are about two-
thirds the size of those from Armagh.

Teeth occur which differ from the types in some particulars. They
are almost circular in form, and equally convex from all sides; their
diameter across the crown is slightly less than half an inch. They
may represent a different species of this genus of fossil fishes, but
until a larger number of specimens have been found affording more
complete evidence of its peculiar characters, it appears advisable to
retain them under the above title as a variety of the old type.

A number of small helodont teeth are scattered over some of the
pieces of limestone. They are small and elongated, smooth and even
on the surface of the crown, without median or other prominence.
They were probably connected with this or the following species of
Psephodus.

Psephodus simplex, Davis, sp. nov. (Figs. 1, 2, p. 150).

Teeth trapezoidal in outline, longest diameter 0-8 inch. Two
longest sides forming an acute angle at the apex. ‘The two shorter
ones, half the length of the longer, inclosing an obtuse angle. The
surface of the crown is convex (Fig. 1), its enamelled surface covered
with small punctures. The margins of the tooth are thick. The
under surface (Fig. 2) forms a channel extending parallel with the
long axis of the tooth, which like the under side of Psephodus magnus,
Ag., was attached to one of the cartilaginous jaws of the fish.

The teeth comprised in this species, of which several specimens have
been found, are almost identical in shape. They differ from those

152 J. W. Davis—Carboniferous Fish-remains.

of P. magnus in form; the latter are more or less pentagonal or
rounded, whilst this species is four-sided, two being so much longer
than the others as to assume almost a triangular appearance. I have
ventured to distinguish the species by giving it the name Psephodus
simplex.
Genus Deltoptychius, Agass. MS.
Davis, Trans. Roy. Dublin Soe. n.s. vol. i. p. 432 (1888).
Deltoptychius plicatus, Davis.
Quart. Journ. Geol. Soc. vol. xl. p. 628, pl. xxvi. figs. 13, 14 (1884).

Several teeth of this species have been obtained. They do not
materially differ from those described in the paper referred to above,
from the Yoredale Series of Wensleydale, in the possession of Mr.
Horne; like them, they are readily distinguished from the type
species of Agassiz, D. acutus, by the greater prominence of the ridges
occupying the surface of the crown; the more regular and broader
form; and more widely expanded outer margin. The Derbyshire
specimens are slightly larger than those found at Wensleydale. They
are delicately and beautifully punctate on the surface.

Genus Pecilodus, Agass. MS.
Davis, Trans. Roy. Dublin Soe. n.s. vol. i. p. 441 (1883).
Pecilodus Jonesii, Agass. MS.
Davis, Trans. Roy. Dublin Soc. n.s. vol. 1. p. 442, pl. lui. fig. 20-23.

Teeth of this genus have been found. ‘They correspond with
those of the same species found at Armagh in essential characters.
They are of two forms, the larger posterior tooth is about 0-5 inch in
breadth, the length equalling half the breadth. 'The posterior por-
tion of the tooth is broadest and is free from ridges. Its surface is
considerably worn and forms a concave depression. The remainder
of the crown is traversed by 7 or 8 parallel ridges. The whole is
enamelled and punctate. The second tooth is smaller, sub-triangular
in outline; its length is the same as that of the larger tooth, 0:25
inch; the greatest breadth is 0:lin., diminishing towards the opposite
extremity. Five ridges are exposed, extending transversely across
the surface, separated by somewhat deep grooves. It is similarly
enamelled and punctate to the posterior tooth.

The only species of the genus Pecilodus hitherto recorded from
the Mountain Limestone of Derbyshire is P. foveolatus, M‘Coy
(British Paleozoic Fossils, p. 639, pl. 3e). The type is in the
Woodwardian Museum, Cambridge, and is unique. It is readily
distinguished from the specimens in Mr. Parker’s collection by its
large size, narrow, elongate form, more numerous and diagonally
disposed ridges, and the regular rows of puncta which run parallel
with the ridges. The species, Pacilodus Jonesii, named by the late
Prof. Agassiz, and described in the memoir cited above, has hitherto
been found only in the Limestone of Ireland. Jt comprises teeth of
two forms originally considered by Agassiz to represent two species,
but proved by specimens in the collection of the Earl of Enniskillen,
now transferred to the Natural History Museum, Cromwell Road, to

J. W. Davis—Carboniferous Fish-remains. 153

belong to the same species, and to be the anterior tooth of P. Jonesii.
In this, as in others of its principal features, the species from Derby-
shire agrees; and whilst in one or two minor points it is dissimilar—
as, for instance, in the greater expansion of the smooth posterior part
of the larger tooth, and the fewer number of the ridges on the small
one—there can be no hesitation in considering those differences as
not more than varietal, and including it in the same species with the
examples from Armagh.

Genus Xystrodus, Agass. MS.
Davis, Trans. Roy. Dublin Soe. n.s. vol. i. p. 447 (1883).
Xystrodus Parkeri, Davis, sp. nov. (Figs. 3 and 4, p. 150).

Several exquisitely beautiful little teeth have been found belong-
ing to this genus. They are 0:3 to 0-4 inch in length, and 0°15 to
0-2 inch in width, sub-triangular in outline, rounded anteriorly, and
expanding towards the posterior margin. Surface of the crown con-
cavo-convex, rising on one side in the form of a ridge, depressed
along the opposite one, forming a broad concave channel extending
the whole of the length of the tooth, and expanding into a somewhat
aliform margin, more or less sinuous in outline. The surface is
enamelled, and a number of minute punctures, arranged so as to
form a series of sinuously parallel ridges, extend across the tooth.

This species resembles most nearly that of Xystrodus pulchellus,
Davis (Trans. R. Dublin Soe. n.s. vol. i. p. 450, pl. lv. fig. 24), from
the Yoredale Series of Wensleydale, but may be readily distinguished
by its rounded anterior extremity, less acutely triangular form, and
the aliform character of the concave margin. The convex margin is
rounded in this species, in X. pulchellus it is straight.

Xystrodus simplex, St. J.and W. (Geol. Survey of Illinois, vol. vil.
p- 178, pl. viii. figs. 4, 5, 1883), is a larger tooth than the one now
described, but is similar in form. It may be distinguished by the
more acute angle formed by the lateral margins and its point of
inrolment being more distinctly developed. The puncte on the
surface are without arrangement into ridges. Messrs. St. John and
Worthen consider that the genus Xystrodus is closely allied if not
identical with that of Tomodus, Agass. They remark, ‘‘ While we
have not the data necessary for carrying the comparisons to a final
conclusion, we are much impressed by the intimate resemblances
which subsist between the present genus and Tomodus, Agass. A
series of careful sketches of authentic examples of Tomodus convexus,
Agass., from the Mountain Limestone of Bristol, England, and which
were kindly submitted to us by Lord Enniskillen, show this rela-
tionship in a striking manner. The genus T’omodus, indeed, appears
to be a Xystrodus in all save the arrangement of the puncte in
parallel transverse lines; and in the latter respect we find a close,
though not absolute agreement, in the initial species occurring in the
American Carboniferous species X. simplex” (op. cit. p. 177). It was
in 1859 that the late Professor Agassiz, whilst visiting the Harl of
Enniskillen, took the opportunity to examine and arrange the mag-
nificent collection of Carboniferous Limestone fish-remains which

154 J. W. Davis—Carboniferous Fish-remains.

were then located in the Florence Court Museum. Amongst others,
the large, thick, massive, triangular and convolute teeth from Bristol.
They are one and a quarter inch in length and nearly half an inch
in thickness; the surface, convex from back to front, as well from
side to side, almost globose. These were named Tomodus convewus.
The type specimens are figured in the Trans. Roy. Dublin Society
(ns. vol. i. pl. lv. figs. 15-18). The teeth assigned to the genus
Xystrodus are medium or small in size, of a triangular form, much
elongated, slightly convoluted, and more or less acutely pointed
anteriorly. The crown does not present the bold convexity charac-
teristic of Tomodus, but is comparatively flat, one side of the crown
being raised, the other depressed. Xystrodus striatus and X. angustus,
the Agassizian types, are also figured in the memoir cited above
(pls. lv. figs. 7-10 and pl. lv. figs. 19-21). The former was de-
scribed by Prof. M‘Coy under the name Cochliodus striatus (Brit.
Paleozoic Fossils, p. 624, pl. 31, fig. 27). The group described by
Messrs. St. John and Worthen, of which Xystrodus simplex, already
mentioned, may be taken as the type, have all the characters of that
genus, and appear to be closely related to the British species ; but
there is no evidence with which the writer is acquainted which
demonstrates that either the British or American representatives of
the genus are generically related to Tomodus.

In recognition of the services rendered to paleeontological science
by Mr. Parker, I have ventured to distinguish this species by

appending to it his name.

Family Coropontipm, Davis.

Genus Mylacodus, Agass.
Davis, Trans. Roy. Dublin Soc. n.s. vol. i. p. 480 (1883).

Mylacodus variabilis, Davis, sp. nov. (Figs. 5, 6, p. 150).

Teeth trapeziform, length 0-7 inch, breadth 0-9 inch. Crown of
at least two different forms, in each the surface is more or less level,
slightly convex in central part between the sides, with a sigmoidal
curvature in the opposite direction, the posterior and lateral margins
are a little raised, inclosing a shallow depression, enamelled, and
covered with minute, and in some cases scarcely distinguishable, pustu-
lations. Anterior margin of first tooth straight, laterally more or less
straight, slightly diverging to the rounded posterior margin. Angles
rounded. Second tooth, anterior margin concave; may have been
attached to the posterior margin of the first; antero-lateral angles
acute, not rounded; lateral margins straight or slightly concave,
posterior margin slightly convex, postero-lateral angles slightly
rounded. Base not well exposed, mostly hidden in the matrix.
Part exposed 0:15 inch in thickness, porous, thinning out towards the
margin of the crown, with the upper surface of which it forms an
acute angle.

Two species of Mylacodus have been described in the Trans. of the
Royal Dublin Society, both from the Carboniferous Limestone of
Armagh, in Ireland ; the types are in the Enniskillen Collection at

J. W. Davis—Carboniferous Fish-remains. 155

the new Natural History Museum. From M. quadratus, Agass., this
species may be distinguished by its greater breadth, straight anterior,
and rounded posterior margins. The second tooth is readily distin-
guished by its form; and both are less distinctly punctate than in
M. quadratus. The coronal surface of Mylacodus sesamini, Agass.,
is uniformly rugose, and the lateral depressions near the margin are
deeper and more extensive. The form of the crown is that of a
truncated cone as compared with the broad expansion of the species
now described, which it is proposed to distinguish as Mylacodus
variabilis.
Genus Ruymopus, Agass. MS.
Davis, Trans. Roy. Dublin Society, n.s. vol. i. p. 473.
Rhymodus convexus, Davis, sp. nov. (Fig. 7, p. 150).

Teeth: length 0-25 inch, breadth 0:45 inch. Crown, median portion
uniformly convex, with depression on each side, lateral extremities
raised into prominent ridges; surface enamelled; central part con-
siderably worn by attrition, beautifully punctate, without definite
arrangement. Anterior and posterior margins similar; central part
rounded, with a depression, corresponding to the one across the
surface, on each side. Antero-lateral angles produced, slightly
rounded ; opposite ones similar. Base not exposed.

This species differs from Rhymodus transversus, Agass., and Rhy-
modus oblongus, Davis, in the form of the coronal surface. In each
of the species named there is a decided concavity in the median part
of the anterior margin. In this species the anterior margin is convex.
The aliform processes of the crown as well as the root, which are
prominent in the two forms previously described, are not largely
developed in this species. Whilst differing in specific details from
the forms of Rhymodus, the transversely oblong form, prominent
convex crown with lateral depressions and raised margins, are generic
characters sufficiently distinct to leave no doubt as to its relation-
ship with that genus. Having reference to its especially rotund
coronal surface, the name Rhymodus convexus is suggested to dis-
tinguish the species.

Genus Characodus, Agass. MS.
Davis, Trans. Roy. Dublin Soe. n.s. vol. i. p. 474.
Characodus minimus, Davis, sp. nov. (Fig. 8, p. 150).

Teeth trapezoidal in outline, small size; anterior margin 0-2 inch
in length, posterior one 0°25 inch; length 0:12 inch. Crown from
front to back convex ; laterally, slightly convex, the middle portion
worn by attrition and somewhat depressed. The surface is covered
with enamel, and minutely punctate where unworn. All the margins
are straight. The base is hidden by the matrix, but appears to be the
same size as the crown.

This tooth approaches most nearly to the generic characters
possessed by the genus Characodus; it differs from the species
hitherto described as C. angulatus, Ag., and C. cuneatus, Ag. (Fossil
Fishes of the Carb. Limestone Series of Great Britain, Trans. Royal

156 J. W. Davis—Carboniferous Fish-remains.

Dublin Society, ser. ii. vol. i. p. 475, pl. Iviii. figs. 19, 20, and 21),
in the absence of a prominent lateral border on each side of the
coronal surface. In the place of this the borders are more or less
depressed, except midway between the anterior and posterior angles,
where a minute projection forms an angular prominence. This
species in its form appears to hold an intermediate position between
the two named above; whilst its margin and angles are equally
regular with those of C. cuneatus, it possesses the elongated form
of C. angulatus.

Family Psammopontipa, L..G. de Koninck.
Genus Psammodus, Agass.
Davis, Trans. Roy. Dublin Soc. n.s. vol. i. p. 459 (1883).

Psammodus rugosus, Agass.
Poissons Fossiles, vol. iii. p. 111, pl. xii. figs. 14-18; pl. xix. fig. 15 (1833).

Several teeth of this species have been found: they do not differ
from those of other localities, examples of large size are not un-
common. A specimen, of which only a portion is preserved, is 1-1
inch in breadth, a portion of the length only remains. It differs
from the ordinary form in the sigmoidal curvature of the surface of
the crown from back to front, one portion being depressed and con-
cave, whilst the other is broadly convex, the latter much worn by
attrition. The margin of the convex side forms an acute angle with
the under surface of the base.

Genus Pleurodus, Agass. MS.
Davis, Trans. Roy. Dublin Soe. n.s. vol. i. p. 458 (1888).

Pleurodus Woodi, Davis.
Davis, /.c. p. 458, pl. lix. figs. 12-15.

About a score of teeth of this species have been found. They are
extremely interesting because they extend the vertical distribution
of the genus downwards from the Yoredale beds of Wensleydale to
the thick-bedded Lower Limestone of Derbyshire. The type-species,
P. affinis, was obtained from the Coal-measures, and named, but not
described, by M. Louis Agassiz. The same author also named a
second species, P. Rankinii, from the Coal-shales of Northumberland.
In 1870 a specimen was discovered at Newsham, near Neweastle-on-
Tyne, which was described by Messrs. Hancock and Atthey in the
Trans. of Northumberland and Durham, vol. iv. pt. ii. p. 408, pl. xv.
Sv much of the fish was preserved that its form could be identified.
The length of the head and body was 3 inches, the breadth across
the thorax 2 inches. The body was covered with mosaic-like tubercles,
the tail was not preserved ; a spine was inserted immediately behind
the thorax, five-eighths of an inch in length, laterally compressed,
straight, broad at the base, tapering rapidly to a point. The mouth
was large, and there were apparently three or four teeth on each
ramus of the jaws. The bones were cartilaginous throughout.

The teeth of Plewrodus Woodi indicate a fish about double the size
of the one from the Newsham Coal-shales; and, judging from a

Charles Davison—Earthquake Phenomena. 157

comparison of the size of the teeth, about half the size of the Pleurodus
affinis, Agass., also from the Coal-measures. The teeth may be
distinguished by the deep transverse ridges and the absence of
widely expanded lateral margins, as well as their elongate form. The
specimens described in the Transactions of the Royal Dublin Society
from the collection of the late Mr. Wood, of Richmond, were tabulated
as having been found in the Mountain Limestone of Richmond, in
Yorkshire. I have since found that they were from the Upper Yoredale
beds near Leyburn, the same locality from whence the collection of
Mr. Horne was obtained ; consequently Mr. Parker’s specimens from
Derbyshire are the only ones which have been found in the Lower
Limestone. Anexample of the spine of the fish has not been found ;
the teeth do not differ in any appreciable degree from the types, and
they are probably the same species.

INSERT SEDIS.

A large number of small palatal teeth have been found associated
with those already described. They are of varied forms, usually
more or less elongated, sometimes of uniform width and even and
smooth on the surface; in others, the median portion is raised and
gibbous, the lateral extremities depressed and attenuated in width.
The under-surface is devoid of basal or root-like extension, and is
frequently more or less concave, thus conforming to the convexity of
the crown. They are enamelled and covered with pustulations or
punctations where the surface has been worn.

Many of these small teeth are probably immature examples of
species already described ; others may have been associated with
them in different portions of the jaws, whilst it is possible that some
may be distinct and independent species. It is considered advisable
for the present to await the advent of other examples which shall
render the determination of their affinities and relationships some-
what less problematical.

II].—On THE OccurRRENCE OF UNDISTURBED Spots IN HARTHQUAKE-
SHAKEN ARnmas.!

By Cuartzs Davison, M.A.,
Mathematical Master at King Edward’s High School, Birmingham.

NE of the most important discoveries in Seismology is that
which proved the close connexion in position between earth-
quake-centres and lines of fault, leading up to the view that the
earthquake is an effect and not a cause of fault-formation. It may be
the momentary result either (1) of the sudden fracturing of the
earth’s crust, or (2) of the impulsive friction that must accompany
the relative displacement of the rock-masses adjoining the fissure.
Now, earthquakes are frequent at places where faults are already
advanced in the process of formation. They also recur continually
at one and the same place along a line of fault, the number felt in

1 A note read before the Birmingham Philosophical Society on March 11, 1886.

158 Charles Davison—Earthquake Phenomena.

any area being often greatly in excess of the number of faults
beneath that area. Hence, it follows that the majority of non-volcanic
earthquakes must be due rather to the individual slips which are
the elements of a great displacement than to the repeated fissuring
of the earth’s crust. On this view, then, the earthquake is but an
incident in terrestrial evolution, and has no further connexion with
the formation of mountain-chains and continents than the creaking
of an unoiled wheel with the motion of a railway train.

First, let us take the case of an earth-crust homogeneous and of
equal elasticity in all directions. Let HF represent a section of
a fault or fissure, and C’ D the sur-
face of the earth, and let us call E
the rock-masses on either side the C———____________D
fissure A and B. Now suppose
B to be slightly, but suddenly, B A
lowered relatively to A. Then the
particles of A at the surface of
the fissure will by impulsive fric-
tion be drawn sharply downwards.
Similarly, those of B at the surface
of the fissure will be drawn up-
wards. Hence, the earth-waves in
the two rock-masses will start in opposite phases of vibration. At
a distance from the fault this difference will not much affect the
character of the earthquake-motion; but along the line of fault,
every particle, being urged upwards and downwards equally, will
remain at rest; and in the immediate neighbourhood of the line
of fault, or its continuation, the disturbance will be less violent,
than it otherwise would be, owing to partial interference by the
spreading of either earth-wave in the adjoining rock-mass.

Returning to the case of the earth-crust as it actually is, hetero-
geneous and discontinuous in all directions, we find the problem
somewhat less simple. We have here to guide us the numerous
observations of earthquakes in Japan and other places, and, to a
certain extent, the seismic experiments of Prof. Milne and Mr.
Gray. These lead us to infer that absolute rest along a line of
fault must be a most.improbable occurrence, owing to the great
irregularity of the surface rocks. Still, we may believe that, in
many earthquakes, the disturbances will be less violent along, and
in the neighbourhood of, the line of fault, than in other parts of
the disturbed area; and that in earthquakes of moderate intensity,
the motion may be so slight as to be imperceptible to observers
unpractised or without instrumental assistance. Evidently, also,
the further away a place is from the spot where the fault-slip
occurs, the less likely will it be for the earthquake-waves to
interfere there.

The Scottish earthquake of November 28, 1880, furnishes a good
example of these considerations. It occurred at 5-40 p.m., after
the hour of sunset, and therefore at a time when all the lighthouse-
keepers must have been on watch. Mr. C. A. Stevenson, who has

aff

W. Whitaker—Brighton Water- Works. 159

studied this earthquake,! mainly from the reports of lighthouse-
keepers, shows that its epicentrum was in the neighbourhood of the
island and lighthouse of Phladda, and therefore at a place on or
close to the great fault which traverses Scotland in a south-westerly
direction from Inverness. In all probability, the shock was caused
by a slip of this fault, some distance below Phladda. On the map
illustrating Mr. Stevenson’s paper are marked, not only the places
where the shock was distinctly felt, but also those where it is ex-
pressly stated that no shock or tremor was observed. A glance at
this map suffices to show that, along the line of fault, no shock was
noticed at the five places nearest the epicentrum, while at two more
distant places in Scotland, and again, in the opposite direction on
the coast of Ireland, the earthquake was distinctly felt.’

In the same manner, the following well-known instances may
perhaps be accounted for, though the facts are too few to admit of
circumstantial proof*—the sparing of a solitary house at Radicina
during the Calabrian earthquake of 1788, while the rest of the town
was entirely levelled; the phenomenon described by Humboldt, when
the earthquake is said by the Andean natives to “form a bridge,”
being felt in two near but separated areas, and hardly at all in that
between; and, lastly, a somewhat similar instance mentioned by
Darwin as occurring during the Concepcion earthquake of 1836.

LV.—On tHe WaTERWORES AT GoLpsToNE Bottom, BRIGHTON.

By W. Wuiraxer, B.A., F.G.S., Assoc. Inst. C.E.
Communicated by permission of the Director-General of the Geological Survey.

HESE works were at first only supplementary to the Lewes Road
Works, on the east; but now are the chief source of supply.
They were begun in 1865, and are placed in a hollow in the Chalk,
in open ground at the north-western edge of Brighton. This
hollow, the bottom of which, I am told, is 30 feet below the lowest
part of its rim, is perhaps in itself an evidence of the existence of
underground water, being due, most likely, as is usually the case in
limestone-districts, to the dissolving away of the rock by under-
ground water and to the consequent sinking-in of the surface. It is
an analogous occurrence to the Meres of Norfolk, except that these
are generally more or less filled with water, whilst Goldstone Bottom
is quite dry at the surface. I may mention that at the time of my
visit there was so thick a fog that it was impossible to see the hollow.
The Brighton Waterworks are perhaps the best example of the
method to be employed in getting a very large supply from the

1 <The Earthquake of 28th November, 1880, in Scotland and Ireland,” Edin-
burgh Roy. Soc. Proc., vol. xi. pp. 176-187.

2 It should be mentioned that at two other places near Phladda, and not on the line
of fault, the earthquake passed unnoticed,

3 Dolomieu, ‘‘A dissertation on the Karthquakes in Calabria Ultra, which
happened in the year 1783,’’ Pinkerton’s Voyages and Travels, vol. v. p. 290.—
Humboldt’s Personal Narrative, vol. iv. p. 21.—C. Darwin, “ On the Connexion of
certain Voleanic Phenomena in South America, etc.,’ Geol. Trans. second series,
vol. vy. pp. 605-6.

160 W. Whitaker—Brighton Water- Works.

Chalk, and I was therefore glad to be able to accept the invitation
of the Chairman of the Waterworks Committees and of the Engineer,
Mr. Edward Easton, to visit the Goldstone Bottom Station on
December 6th, 1884, when, under circumstances not likely to occur
again for some time, the party, of which I was one, was able to go
down into the actual source of supply and to examine it thoroughly.

For the history, engineering details, and general account of the
waterworks, the reader is referred to the papers by Mr. Haston in
the Report of the British Association for 1872, pp. 895—400, and in
the Transactions of the Brighton Health Congress, 1881, pp. 48-56,
with three plates.

At Brighton the water is got from the Upper Chalk by sinking
shafts down to about low-water-level, and by then driving galleries,
or small tunnels, more less at right angles to the dip of the beds, so
as to cut the fissures along which water flows in its passage from
the higher ground on the north to the sea. The present supply is
plentiful ; but the Corporation have looked well ahead, and took
advantage of a late dry season, to extend these tunnels and so to
get a future increase (at the Goldstone Works).

The depth of the shafts varies of course as the level of their sites.
At Goldstone Bottom there are four, and their depth is 150 feet and
more. ‘The tunnels vary somewhat in size, up to a height of 18 feet
and a width of 12 feet. Under ordinary circumstances these tun-
nels are filled with water; but, in order to extend them, they were
practically pumped dry (except for small channels by the side), and
about 2,000,000 gallons of water were run to waste daily, after
enough had been taken for the supply of the town and neighbour-
hood. By the skilful management of the resident engineer, Mr.
Baker, the chalky water, that comes from the parts where work was
going on, was kept separate from the ordinarily clear water of the
springs cut ; so that the supply was still got whilst the work went on.

The tunnels are in white chalk, with but few flints in the flat
planes of bedding; but with many oblique layers of thin flint
filling joint-planes. These, it should be remarked, are evidence of
water-flow, having probably been formed by slow deposit from
water along the joints. Some joint-fissures on the other hand are
filled with a soft calcareous and sandy deposit, the sand brought
down from above by the sinking water. Though some of the chalk
seemed fairly soft, yet I am told by Mr. Easton, that much of it was
found to be very hard, needing, almost constantly, chisels and
sledge-hammers to break it, picks being often of no use. __

At Goldstone Bottom the length of the tunnel was 1800 feet in
1881, to which there had since been added (or would be added by the
work in progress) 2600 feet.

The supply comes chiefly from three or four springs yielding from
4000 to 5000 gallons a minute, a long way apart. Though there
are many small additions between these, yet it is noteworthy how
far, in these works, a tunnel has been driven before cutting a fissure
yielding a large supply, as this points to the need, in some cases, of
great lateral extension to get the required supply from the Chalk.

J. Starkie Gardner—Teredo in the Eocene. 161

Had recourse been made to boring, or even to a shaft, only, failure
would almost certainly have ensued, where now the most successful
result has followed from driving galleries. At the Lewes Road
Works a different state of things occurs: the springs are very much
smaller and nearer together, in the 2400 feet of tunnel.

It has occurred to me that the concentration of the underground
water at Goldstone Bottom may perhaps tend to explain the occur-
rence of the basin there, the water having a freer course there than
elsewhere, and therefore escaping more readily to the sea, and
carrying away more chalk in solution.

At the time of my visit the tunnels were brilliantly lit up, by
means of candles fastened to the sides, so that we could see the
length of the tunnels (in one case about 800 feet) and all the springs
issuing from the bottom. The large springs were seen to be in
connection with joint-planes, which, though for the most part closed,
or nearly so, yet, I was assured (by Mr. Baker, who accompanied
me), were open where the water came out, so that a man’s arm
could be thrust in the opening.

Some small inflows of water from the upper part of a tunnel
seemed to communicate nearly directly with the ground above, as,
though running, or rather gently trickling g, at the time (after some
wet weather), “they had not been seen before, in the dry weather.
It was strange indeed to see the great extent of side that was quite
dry, damp being the exception, and to think that, were pumping
stopped, the whole would be filled with water in 6 or 8 hours.

In the North-eastern tunnel the roof is throughout of one bed,
rarely needing support. At the bottom of this bed of chalk there
was a thin, but continuous, layer of flint, which, being brittle, had
been cleared away. It is curious that the end of this tunnel has
struck on an old well, probably one that was made in the early part
of the century, when a number of French prisoners of war were
encamped on the site of the works.

Some weak places in the tunnels had been strengthened by brick-
work ; but for the most part the chalk is firm enough to stand.

To conclude, the visit to these important works, so liberally
opened for us by the Corporation of Brighton, could not fail to be of
the greatest interest to those present, and to be a source of instruction

to all interested in the important question of water-supply from the
Chalk.

YV.—InQUIRY CONCERNING THE DistTRIBUTION OF 'TEREDO-BORED
Woop 1n THE KoceENE.

By J. Srarxre Garpyer, F.G.S.

HE habits and distribution of this marine molluscan pest chiefly
concern the engineer and ship-builder at the present day, but in

the past their presence is a considerable guide to the geologist as to the
conditions under which many of the Eocene beds were deposited. It
does not seem to have existed in the Gault sea, for though the drift-
wood of this period is riddled by some of its destructive ancestors, such
as Teredina, Lamarck, and perhaps Xylophaga, it is far less completely

DECADE III.—vVOL. II.—NO. ly. 11

162 J. Starkie Gardner—Teredo in the Eocene.

destroyed than when the true ship-worm has been at work. Some-
thing very like it is present in the Chalk; but when we come to the
Kocenes, there is no longer any possibility of doubt as to the animal
which has made its home in the drifting logs, for they are riddled in
the way peculiar to the true ship-worm, and its shell is frequently
left in the bore-holes. The distribution of such bored wood in our
EKocenes must prove very instructive in many ways, when the habits
of the living animal are more thoroughly known. As far as my
own observations go, it occurs in the following beds, but I trust many
of our numerous local observers will contribute additional and more
precise information.

Thanet Beds.—A good deal of the silicified wood from the Thanet
series of Herne Bay is bored by Teredo. Mr. Dowker, F.G.S.,
observes that most of the pentoreibeme are Duals. with the grain of
the wood, and mostly range from 3%; to 75; of an inch in cameron
though there are many smaller bores: associated with them.

Reading Beds.—1 have no recollection of meeting with Teredo-
bored wood in this formation.

Woolwich Beds.—Teredo has been recorded from Charlton and
Sunderidge. It is probable that all wood from these deposits will
prove to be bored by the ship-worm.

Oldhaven Beds.—Teredo is recorded by Mr. Whitaker from Charlton,
Sunderidge, and Reculvers,

London Clay.—In reply to my inquiry, Mr. W. H. Shrubsole, F.G.S.,
has very kindly sent me a response which I cannot do better than
quote :—

‘“‘Of the very large number of fossil trunks that I have observed,
in nearly every case, if not in all, it has been evident that the Teredo
borings were on one side of the ovally compressed stem, and in
every instance where I have examined these trunks én situ, either in
the cliff or on the undisturbed clay floor of the foreshore, I have
found the borings only on the underside. This seems to show that
the Teredo attacked the log when it was floating at the surface, and
that it was silted up very soon after becoming water-logged and
going to the bottom.

“The upper surface generally has a limestone covering some
inches in thickness. The trunks are nearly always cracked up into
lengths varying from two to four feet. It is extremely rare
to find a log, large or small, that has not been bored. I have just
examined a segment of a large fossil trunk which I selected and
brought home as being less mutilated by Teredo than any I had seen
for a long time, and I find that its appearance quite supports the
statement made above.

“Another segment of the same trunk J had cut up transversely
into slabs. One of these slabs (polished) is at Jermyn Street, and
another, J think, at Cromwell Road Museum. Reference to them
will probably show that owing to destructive action on one side the
natural axis is eccentric.

1 Teredo has been recorded from the Jurassics, but the generic identity is, I think,
doubtiful,

J. Starkie Gardner—Teredo in the Eocene. 163

“T have found living Teredo in wreckage and other timber that
had been drifting about for some time in the same relative position
as in the fossil trunks. Welle:

Some of the logs at Sheppey must have been entire trunks of large
trees, and they seem to have become water-logged and sunk before
the Teredo had penetrated through even to the core, but in the
vicinity of London, where wood in a calcified state is found in smaller
pieces, it is invariably completely riddled. I only recollect observ-
ing it elsewhere at Harwich and Herne Bay, but there is no doubt
that most of the wood, except small twigs, is universally bored by
Teredo in this formation.

Lower Bagshot Formation.—I cannot trace the occurrence of any
bored wood in these beds at Corfe, Studland, Alum Bay, or elsewhere
in Dorset and the adjoining borders of Hampshire, neither does Mr.
Keeping recollect any at Whitecliff Bay. I have found it, however,
in company with Mr. Hudleston, in the cutting near Walton.

Middle Bagshot Formation.—'The wood throughout this great
formation is invariably completely riddled, except in the lowest beds
overlying the Lower Bagshot in the neighbourhood of Poole Har-
bour and inland to the N.W. of Bournemouth. There is frequently
so little of the substance of the wood left that it appears as a mere
dark stain in the sand separating the casts of the tubes. The logs in
the Bournemouth beds are never large, seldom exceeding three or four
feet, and are riddled quite through and through. In a higher part of
the series, at Hengistbury, the logs are larger, sometimes five feet long
and two or more feet in width, and the bores are relatively gigantic,
being upwards of an inch in diameter, sparsely scattered, and
obviously the work of a different animal. Wood from the true
Bracklesham beds, wherever met with, is invariably bored by
Teredo.

Upper Bagshot Formation.—Wood is always more or less bored in
these beds, though less extensively so perhaps in the Barton series
than in the Bracklesham beds just noticed, for solid pieces occur in
the former, but not in the latter. J am indebted to Mr. Keeping for
corroborating this observation, and extending it to the same series in
Whitecliff Bay, where I had not noticed any wood.

Lower Headon Beds.— Neither Mr. Keeping nor myself have
noticed bored wood, at Hordle and in the Isle of Wight, in this
formation.

Middle Headon Beds.—Mr. Keeping tells me that wood is in-
variably bored in the Brockenhurst beds, but I have no notes regard-
ing wood in the beds at Colwell and Totland Bays.

Upper Headon Beds.—No bored wood occurs in these.

Bembridge Series.—Mr. Keeping and myself are confident that no
Teredo-bored wood occurs in any part of this series, unless in the
brackish series near Whitecliff Bay, where none however has yet
been observed. Mr. E. A’Court Smith writes, “I have never noticed
Teredo-boring in any of the wood here, though some of the wood is
apparently perforated by a species of beetle (or White-Ant?). So
great is the perforation in some cases that the wood drops to

164 J. Starkie Gardner—Teredo in the Eocene.

_ fragments on being released from the matrix.” I find no record of
Teredo from the Hempstead beds.

I have never met with any Teredo-bored wood in the Antrim and
other northern Hocenes, nor at Bovey Tracey. Additional informa-
tion would be of importance, especially with regard to the London
Basin, where the tubes often remain as hard cores of pyrites, when
the wood itself is soft and perishing. They are rounded and blunt
and closed at the thick end and open at the thinner end, and in this
state are often mistaken for plant-remains such as roots or stems.
On one occasion I was sent for to Bournemouth on account of the
supposed discovery of fossil canes or reeds in situ, these being
nothing more than casts of Teredo-boring in a vertical position.

With regard to the habits of the living Teredo, it was, I believe,
for a long time assumed to be a purely marine mollusc, and its oc-
currence in Kocene deposits that were quite obviously of fresh-water
origin was a serious stumbling-block. It has gradually been ascer-
tained, however, to ascend very far up tidal rivers; but whether it
ever passes up completely beyond the influence of saline water, is
a question that appears to be unsettled. It is one, however, which
must be set at rest, if we are ever to understand, and be in a position
to restore, the physiography of the great river to which the deposi-
tion of the entire English Hocene basin is due.

The late Dr. Gwyn-Jeffreys appears to have collected more infor-
mation bearing on this point than any previous writer, and the
following is an extract from his British Conchology, p. 147 :—

“TT. Senegalensis, de Blainv., was discovered by Adanson in the
roots of the Mangrove and another kind of tree lining the banks of
the Niger, Gambier, and other rivers on the W. coast of Africa,
which were only subject to an influx of sea-water for a few months
in the year. According to Adanson, the water of these rivers is
quite fresh or sweet during the remaining months; and T. Sene-
galensis not only exists, but retains its full vigour throughout the
whole year. This statement, however, must be received with some
qualification. JI was assured by Dr. Welwitsch, the great botanical
traveller, that in the tidal rivers of South Africa, the water in the
middle stream is fresh, while that of the sides is brackish, and that
no kind of Mangrove has been known to live in fresh water.
Another sort of ship-worm (Nausitora Dunlopei of Perceval Wright)
has lately been found in India, inhabiting the river Comer, one of
the branches of the Ganges, and a perfectly freshwater stream, that
joins the main river at a distance of about 70 miles from the
sea. Dr. Kirk, the friend and companion of Livingstone, informs
me that he picked up a piece of ebony (Dalbergia melanoxylon) on a
sandbank in the Zambesi river, the water of which was there always
fresh and drinkable 100 miles from the sea—very far beyond the
influence of the tide, which never comes more than 10 miles up the
creeks of the delta. This piece of ebony was pierced in all direc-
tions by a species of Teredo having a calcareous sheath. The kind
of wood mentioned by Dr. Kirk resembles the ebony of commerce,
but is utterly worthless except as fire-wood; and therefore it is not

J. Starkie Gardner—Teredo in the Eocene. 165

at all likely that the piece in question could have been accidentally
brought inland, after being perforated in the sea by Teredo. It sinks
in water, is rather brittle, much harder and far more compact than
either mahogany or teak, and is full of some mineral matter that
quickly deadens the edge of any tool. It does not grow on the coast,
nor within 50 miles of it on the Zambesi. Dr. Kirk adds that in
the bottom planks of the pinnace belonging to the expedition, the
ship-worm was also found, with its soft parts attached to the finely
sculptured valves. The boat was so riddled that the quartermaster
pushed a paint brush through her double planks. This was at Tete,
250 miles from the sea, after the pinnace had remained there six
months at anchor. IJ regret not having space to give in eatenso Dr.
Kirk’s interesting account of all the circumstances connected with
this discovery. There is not the slightest doubt that the Teredo ©
observed by him inhabits water which is at all times perfectly sweet and
Sresh.”

With regard to its occurrence in fresh water in India, a letter
from a member of the Survey appeared in ‘“‘ Nature” of April 19th,
1877: “That the delta of the Irawadi, a tangled maze of creeks, the
waters of which are brackish or salt for about half the year, and
slightly so, and even potable during the other months. The large
canoes which traverse these creeks are much infested by ship-worm,
and are fired to get rid of them. I cannot recall any instances of
bored wood well above the tide-way, but wherever the water is .
occasionally brackish, thus far the worms seem capable of settling.
Perceval Wright has described Nausitoria Dunlopei from the rivers of
Hastern Bengal as Novaculina gangetica. The two Burmese species
of Scaphula are both estuary forms, whereas the type of the genus
in the Ganges is found a thousand miles from the sea.”

Dr. W. T. Blanford, F.R.S., in reply to my question, almost dis-
poses of the contention that Teredo actually becomes a bona-fide fresh-
water mollusc, so far as India is concerned. He writes: ‘I know
nothing of any occurrence of Zeredo in Indian freshwater, and as I
for many years paid a good deal of attention to Indian freshwater
shells, 1 should be much surprised if Teredo were really found in
fresh water there. The genus, however, abounds in the salt and
brackish water of estuaries; all dead wood and even dead branches
of living trees being riddled with borings of several different forms.
I have seen them abundantly in the deltas of the Ganges and
Irawadi rivers. The estuarine molluscan fauna is very rich and
peculiar in India. At times of flood the quantity of water pouring
down the rivers is so great that estuaries become temporarily fresh,
and in this case estuarine forms may be found living in what is for
the time freshwater.”

There is still, however, considerable doubt as to the limits to
which the ship-worm penetrates in Australian rivers, and naturalists
with whom I have conversed seemed under the impression that it
might be met with above rapids, and altogether out of reach of even
an occasional mixture of brackish water. The only further infor-
mation I have, is contained in a letter to “Nature,” May 8rd, 1877,

166 Notices of Memoirs—Geology of Kimberley, W. Australia.

in which Mr. Arthur Nicols, speaking from recollection, says that
“ Teredo navalis is certainly able to endure a long continuance of
freshwater. At Brisbane the river is subject to freshes, one of
which lasted ten days, when the flood was so powerful that ocean
steamers could not get up. Salt-water is said at floods to ascend
thirty miles beyond the town, which is itself twenty-five miles from
the Pacific,—but the ebbs are more fresh than salt. Piles have to
be protected with Muntz metal.”

It will be seen that more definite information is required on all
the points raised. There is said to be a freshwater Carcharias in
the rivers of Fiji, and it would be interesting to learn whether it
also ever lives wholly beyond the tidal reaches, or merely ascends
rivers, as seals will, in search of food.

It thus appears, so far as we can go at present, that Teredo
chiefly flourished during our Hocene time in waters that were clearly
estuarine. ‘The purely salt water reaches of the great river, such as
those in which the London Clay and Bracklesham beds were
deposited, were less favourable to its development than the almost
fresh-water reaches in which the Bournemouth fresh-water beds and
the Lower Bagshot of the London Basin were formed. In this last
class of deposits there is no other sign whatever of aquatic life, either
fresh or salt, and we are forced to conjecture that perhaps frequent
change from quite fresh to quite salt water was the excluding
cause. In what were perhaps more littoral marine beds, out of the
influence of the river, such as those of Herne Bay and Highcliff, the
Teredo seemed comparatively to languish, and it is quite excluded
from the higher reaches of the river in which the Lower Bagshots
of Studland and Corfe were formed, and which from the presence of
Unio would appear to have been wholly freshwater. It had no place
in the lacustrine deposits of Headon and Bembridge, and even the
brackish and salt waters of these formations seem to have been quite
unfavourable to it, being, it appears, from their teeming life, too
permanently either fresh or salt. Without its presence we might
never have suspected that many important masses of sediment
containing terrestrial vegetation had ever been formed within the
influence of the tides of the sea. Sufficient has been said to
illustrate the peculiar local significance that the record of this
destructive mollusc may possess with regard to the origin of a
formation. It is noteworthy that the Hocenes possess three distinct
types of Teredo which have not as yet been distinguished.

IN CMR CAa Ss) (Oi IMME OilisysS)-

I.—Report on tHE GerotocGy or tHE KimpertEy District,
Western AvsTRaALia. By Epwarp T. Harpmay, etc., of H. M.
Geological Survey of Ireland. Feap. pp. 22, 16 Plates, Map.
(Perth, W.A., 1884.)

a country described in this very excellent report comprises that
portion of Western Australia extending from Roebuck Bay

Notices of Memoirs—Geology of Kimberley, W. Australia. 167

inland to the Leopold Ranges, and between Port Usborne, and a line
running eastward to the south of the Fitzroy River (lat. 16° 35’ and
18° 30’ S., long. 122° 10’ and 126° 50’ E.), including in all 12,800
square miles.

It may be generally described as a vast undulating plain, rising
gradually from the sea-coast to a height of 200 ft., broken by isolated
hills and some extensive mountain ranges, the highest reaching
2000 ft. above the sea-level. The district is unusually well watered,
The geological formations represented over this immense tract of
country consist of Recent accumulations, Pliocene sand and gravels,
Carboniferous sandstones, grits, and limestone, and Metamorphic
rocks.

The Recent accumulations are—(a.) Wide sand-flats locally termed
“‘ Marshes,” along the sea-coast, and extending inland for miles, the
most striking instance being the great plain from Roebuck Bay to
Barlee Spring. The contained fossils are of recent species. (b.)
Alluvium deposited by successive floodings of the rivers, estimated
as equal to 3355 square miles, or 2,147,200 acres. But taking into
consideration an average thickness of 30 ft., we have the “enormous
weight of 103,924,480,000 tons of silt and mud carried down by
these rivers” of the Kimberley District. (¢.) River-gravels accu-
mulated in the upper reaches of many of the streams (notably in the
Usborne district), the pebbles often reaching six to nine inches in
diameter. These subdivisions comprise the ‘“‘ Recent” formations
described by Mr. Hardman.

Certain deposits of reddish sand, with small pea-like nodules of
ironstone, and other rocks, with beds of red and yellow-ochreous
earth, are provisionally classed as Pliocene. They are termed the
«« Pindan ” sands and gravels, and occupy a very large area, and have
been proved to be at least 30ft. in thickness. They are unfossiliferous,
“but there can be little question that they are of comparatively
recent age.”

The Carboniferous rocks appear to be separable into an upper and
lower series. The upper consists of sandstones, and forms the chief
mountain ranges, extending as much as 190 miles into the interior,
and are over 1000 ft. in thickness. Lepidodendron, Calamites, and
Sigillaria are said to occur in these beds, but no traces of coal have
been met with. The apparently overlying Carboniferous Limestone
extends in a line N.W. and §.H. directly across the Kimberley district,
with a maximum breadth of thirty miles, and an estimated thick-
ness of 1000ft. “It is a light-coloured, compact, brittle, splintery,
more or less Magnesian Limestone,” and bears a strong resemblance
to the Upper Carboniferous Limestone of Ireland. It is in places
very cavernous. Fossils were met with abundantly at certain
localities, and the list of species given by Mr. Hardman clearly bears
out the age assigned to the beds.

The Metamorphic rocks are divided into two classes—the schistose,
including gneiss schist and metamorphic granite, and quartzites and
altered grits. The former are widely developed along the base of
the Leopold Range, and contain quartz veins, and the common garnet

168 Notices of Memoirs—Lias of Fenny Compton.

in great abundance. The quartzites and altered grits constitute the
mountainous country in Kimberley, and are interstratified with red
and yellow sandstones, conglomerates, and grits.

Dykes of felstone, of later age than the Metamorphic rocks, are
also met with. No precious metals were discovered, but Mr. Hard-
man believes in their discovery being probable in this series.

The Report is accompanied by sixteen geological views, and a very
good map.

IJ.—Tue Lias or Fenny Compton, WARWICKSHIRE.

R. THOMAS BEESLEY, F-.C.S., has just issued this paper
with additions and corrections to the end of 1885. The author
describes the situation of Fenny Compton as a little station on the
Great Western and Hast and West Junction Railways, on the War-
wickshire side of the boundary between that county and those of
Oxford and Northampton, eight miles from Banbury and twelve
from Leamington, and at an elevation of nearly 400 feet above the
sea. He points to the Burton Hills, whose bold escarpment forms so
pleasing a feature in the landscape, as the extremity of the Marlstone
promontory which stretches from the Cherwell valley into the Lower
Lias bay of Warwickshire. He then directs attention to the sources
of the Leam, the Cherwell, and the Nene, flowing respectively to
the Severn, Thames, and Ouse, which sources are all within a circle
of one mile radius, in the high ground above the Marlstone escarp-
ment of Northamptonshire, a short distance east of the Burton Hills.
The railway at Fenny Compton passes for nearly three-quarters of
a mile through a cutting which exposes a section of the lowest zone
of the Middle Lias, which, with the exception of those on the Dorset-
shire and Yorkshire coasts, is probably the most extensive to be met
with in England. The zone of Ammonites Jamesoni which occurs
at Fenny Compton is, with the two others next above it, referred to
the Lower Lias in the maps and memoirs of the Geological Survey
of England; but, under the circumstances, the author prefers the con-
tinental arrangement. Proceeding southwards upon the Hast and
West Junction line, the banks rise rapidly, exposing a bluish-black
shale, fine in texture and rather marly. With one doubtful exception,
none of the Ammonites of the Lower Lias have been found there.
Some geologists have attributed this bed, and a good deal above it, to
the “ Raricostatus zone” of the Lower Lias, but Professor T'ate, who
had carefully examined it, agreed with the author that there was an
error in the conclusion.

The bed soon presents unmistakable Middle Lias characteristics in
the form of parallel lines of pale grey or reddish flattened nodules.
They are much more calcareous than the clay in which they are
embedded, and contain a notable amount of phosphoric acid, chiefly
combined with lime. ‘There are five lines of conspicuous nodules
in the 40 feet of shale. The lower ‘nodules, like the shale in which
they lie, are rather poor in fossils, though both become richer in
higher ground. The author possesses a small one containing on its
surface 50 specimens belonging to more than 20 species, one of which

Notices of Memoirs—The Vienna Museum. 169

is a Discina. About a quarter of a mile from the station, two
noticeable bands of stone occur about 40 feet above the base of the
section. The upper stone is separated from the lower by 4 ft. 6 in.
of dark blue clay with many fossils. It is of the same mineral
character and appearance as the lower; but contains corals of the
genus Monitlivaltia, while corals are no longer present in the lower.
The Spiriferine, which play so important a part in the fauna of the
upper stone band, as well as the corals and Waldheimia numismalis,
are absent from the Yorkshire Lias. The dip of the beds is dis-
tinctly to the south, as the stone bands sink below the surface, at
a distance of about a third of a mile beyond the spot where they
first appear. The true dip is about three-fourths of a degree.
Above the stone bands, the shale gradually becomes greyer, rougher,
and more lumpy, many of the lumps containing impressions of
fucoids.

The following is a detailed section of the Fenny Compton beds:—

Ft. in.
OMe Esha acl avenue see liseli suse dy) col ussideh voetupecoiisesy) osm uiysson a0 gO
Band of calcareo-argillaceous nodules 6 008) Gen ado"! "i508" 0061" 606 2
Sial cement see RAL) ortho Nh ern ere” nN nota trace’ oes gee LON VO
Hand of nodules with Am. Henleyi, A. Ibex, A. Maugenetii, A. Valdani ... 3
Nal CMBR te save cacti saa) ani oNeder aiaein ie Siindas. Messi nl tech hceriet ress 0
Band of nodules with Am. Maugenetii, and Fucoids NG Raion RUscOee pod 2
Sihalla, wiitiin Telveunmnies aesas 7 soa 8 BaSe eee ged age feces Heol ida daa, ea)
Rough, shelly, argillaceous limestone, with Am. Valdani, and A. Jamesont,
Spiriferina verrucosa, Belemnites clavatus, Lima Hettangiensis, Waldheimia
numismalis, Rhynchonella rvmosa seu ne sneer 1
Single, witin, Byellewamntiig="* shoe OREM SSUM aac Gao”, eee econ Pose. Bde ooo eda «es
Rough, shelly, argillaceous limestones with Am. armatus (young), Pecten
priscus, Limea acuticosta, Gryphea obliquata, Cardinia attenuata,
Rhynchonella rimosa. Corals ... ws 9
Shale Soares 1 8
Band of nodules ... 3
Shale Ee ecm ce Nicely | cons Mosee! Memen vsas: gene 3 0
Band of nodules with Pecten calvus, Terebratula subovoides ... ... 0» eve 3
Spite MRD N RUC ye: Shwe raues epi) ei) cae: cbip re detonn ale Videantizeeabbeelly odaili Ary
Band of nodules ... SOC MPECAT | OCCT ECENY PELE PDUCREEECOR Nord eRCOI pacaare cD 2
SURES cca: dg! SRR EGS ec a Ae sat tea Se)
Band of nodules ... MRP Soas Love ese) ciieon dicta’ eiugretslu Reset gcse. cee 2
Smee te eee mar eco eee RUC e TAME NY Poe sire Te eeG
Band of nodules ... LeU Pera ital Bese Weasel both alee acme cacw last: please) Mees 2
SLGI@ 15” ORE UNE ate len (meen tin car mnrineo sR ESPRD Oreos ltr Meaney ne orem ReeCER EEE aE Ee), 1)
97 0

II].—AnNALEN Dues kK. K. NATURHISTORISCHEN HOFMUSEUMS ; REDIGIRT
von Dr. Franz Rirrer von Haver. Band I. No.1. Jahresbericht
fiir 1885, von Dr. F. von Hauer. (Wien: 1886.)

ANNALS oF THE Roya Narurat History Museum. Edited by

Dr. F. von Haver. Vol. I. No.1. Annual Report for 1885, by
Dr. F. von Haver. (Vienna: 1886.)

ite. report contains a review of the progress made in the organi-

zation of the New Natural History Museum of Vienna under

the superintendence of the well-known mineralogist, Dr. von Hauer,

the successor of the late Dr. F. von Hochstetter. Until lately, the

170 Notices of Memoirs—A. von Kenen, U. Devonian Crinoids.

various Natural History collections of the Austrian capital were
deposited in different buildings, under independent management, but
they have now been brought together in a magnificent edifice ex-
pressly constructed to receive them. The Museum ineludes the
following five divisions: (1) Zoological; (2) Botanical; (8)
Mineralogical and Petrographical; (4) Geological and Palzeonto-
logical; (5) Anthropological and Ethnographical. Dr. A. Brezina
and Theodor Fuchs are the keepers of the third and fourth depart-
ments respectively. The mineralogical collection is noted more
particularly for its meteorites, of which there are 1207 specimens
from 365 different localities; and the special forte of the paleonto-
logical division is the splendid collection of Tertiary mollusca.

“A special library is being formed in connection with the museum,
and we notice with pleasure the facilities provided for carrying
forward original research whether by the museum officials or by
voluntary independent investigators.

The present number is intended as the first of a series in which it
is proposed to publish, together with the museum report, original
memoirs on various natural history subjects.

LTV.—Dir CrinoipEN DES NORDDEUTSCHEN Oxper-Devons. Von A.
von Kenen, in Gottingen. Neues Jahrbuch fiir Mineralogie,
etc., 1886, Bd. I. p. 99-116, Plates I.—II.

WING to their defective state of preservation, very little has
hitherto been known of the Crinoids of the Upper Devonian
strata of North Germany. Prof. von Koenen in this paper gives the
results of a critical examination of specimens which he has for many
years been collecting, as well as of those preserved in the Museums
of Bonn, Berlin, and Aix-la-Chapelle. From a comparison with the
forms from the Famennien group of Senzeille in Belgium, described
by Fraipont, the author has been able to determine the position of
the anal plate and the composition of the ventral roof of the calyx
of the different species; characters, which the author regards as
of special: value in the determination of species. The following
species are described and figured :—Melocrinus gibbosus, Goldf., M.
hieroglyphicus, Goldf., M. Chapuisi, Dewalque, M. Dewalquei, un. sp.,
M. Benedini, Dew.-Fraipont, Hexacrinus infundibulum, n. sp., A.
angulosus, n. sp., H. verrucosus, Dewalque, H. tuberculatus, n. sp., and
Storthingocrinus sphericus, sp. n. (Ge dla Jats

V.—Recorps oF THE GroLocican Survey or Inpra, Vol. XIX.
Part 1, 1886.

HIS part contains, with other papers, the Annual Report of the
Geological Survey of India by Mr. H. B. Medlicott, in which
attention is more particularly called to the discovery, by Dr. Warth,
of Paleozoic fossils in the Salt Range of the Punjab, in strata, asso-
ciated with a noted Boulder-bed, which have hitherto been regarded
as belonging to the Cretaceous series. The fossils, which have been
determined by Dr. Waagen, include several species of Conularia,
Bucania, Nucula, Atomodesma, Aviculopecten, Discina and Serpulites,

Notices of Memoirs—Dr. J. Lorié—Geology of the Pays-Bas. 171

some of which occur in Carboniferous strata in Australia, and others
are related to species from the Carboniferous Limestone of Belgium.
A further interest attaches to this discovery of Carboniferous fossils
in connection with the Boulder-bed in the Salt Range, from the
probability that this bed may be identical with the Talchir boulder
glacial deposits found almost everywhere at the base of the Gond-
wana rocks of Peninsular India. These in turn have been correlated
with remarkable Boulder-beds, believed to be due to ice-action, occur-
ring in the Carboniferous series of Australia. Mr. R. D. Oldham has
lately visited Australia, and contributes, in this part, a highly im-
portant memorandum on the subject. This further evidence strongly
supports the original views of Dr. Blanford as to the Palaeozoic age
of the Lower Gondwana deposits, and, as Mr. Medlicott remarks,
“it would be the first clear and broad case to confirm the assertion,
made twenty-five years ago by Prof. Huxley, when introducing the
term ‘homotaxis,’ for it shows that a full-blown Mesozoic flora in
one region of the earth was contemporaneous with a full-blown
Paleozoic flora in another region.”

Under “ Afghan and Persian Field Notes,’ Mr. C. L. Griesbach,
who accompanied the Afghan Boundary Commission as geologist,
gives an outline sketch of the various geological formations, which
range from the Post-Tertiary to the older Paleozoics, occurring in
the Herat Valley and Khorassan.

The other papers in this part are “Notes on the Section from
Simla to Wangtu,” by Col. McMahon, and an excellent ‘Report
on the International Geological Congress of Berlin,” by Dr. W. T.
Blanford, F.R.S. G. J. H.

VI.—Conrrisutions A ta Géonocie pres Pays-Bas. Par Dr. J.

Lorté. Résutrats GoLogiquEs ET PALONTOLOGIQUES DES

- Foraces DE Purrs A Urrecut, Gores et Gorkum. Extrait des

Archives Teyler, Series II. tom. ii. Large 8vo. pp. 182, and 5
lithographic plates. (Haarlem, 1885.)

ae opportunities of studying the structure of the earth’s crust

in a flat country like the Netherlands are indeed few and far
between. ‘There are no coast or valley sections, and owing to the
general level character of the country, scarcely any artificial cuttings
are required for the railways. Under such circumstances, well-
sinkings afford the best, and almost the only means of ascertaining the
stratigraphical succession. In the course of the last few years, three
important sinkings have been made in this country, at Utrecht, at
Goes on the island of South Beveland, and at Gorkum in South
Holland. The first of these was carried to the depth of 869 meétres,
that at Goes to 223-9 m., and that at Gorkum to 182 m. beneath the
surface, which, in each case, did not exceed 5 m. above the sea-level.
The distribution and the characters of the fossils met with in these
well-borings have been carefully investigated by Dr. Lorié, and this
memoir contains critical descriptions and figures of the different
species and tabular lists of their occurrence in the beds at different

172 Reviews— United States Geological Survey.

depths, and a comparison with those in strata of corresponding age
in Belgium and Hast-Anglia.

The strata pierced in these well-borings consist entirely of beds
of gravel, sand and clay, of Tertiary and Quaternary age, some
barren of fossils, others with shells, bryozoa and other fossils. There
are 131 species enumerated, all of which have been previously
described. In the Goes boring the entire thickness of the Pliocene
is penetrated. The Lower Pliocene or Diestien, the equivalent of
the Coralline Crag, has a thickness of 87 métres. It contains a certain
proportion of Polyzoa and appears to have been deposited in a
tolerably deep sea. It rests upon the Rupélien clay of Middle
Oligocene age. The Upper Pliocene or Scaldisien, the equivalent
of the Red Crag of Hast-Anglia, has a thickness at Goes of between
25 and 29 métres. Above this comes the so-called Diluvial beds,
about 47 métres in thickness. At Utrecht the Diestien beds have
a minimum thickness of 125 m. and their base is not reached. They
are principally greyish-green sands with intervening bands of clay,
and the absence of Polyzoa and the broken condition of the shells
indicate a shallower sea than at Goes. The Scaldisien or Red Crag
has a thickness of 82 m., and there are above it beds of Quaternary
and Recent age 162 m. in thickness. At Gorkum the base of the
Scaldisien or Red Crag was not reached at the depth of 182 m.
This deposit has thus a minimum thickness of 62 m., and from the
fragmentary and triturated shells therein, it appears to be of littoral
origin. Above this are freshwater beds, 28m. in thickness, of
Quaternary age. With the exception of the first 12m. of recent
deposits, the intervening strata 80m. in thickness are also of
Quaternary age.

This memoir is a valuable contribution to the history of the later
fossiliferous strata in a new area, and it has a special interest to the
student of the corresponding beds in Hast-Anglia. G. J. H.

D152) aT WA 2D Eh WW Se

—-——

J.—Bubuetins oF THE Unirep States GroLtogicaL Survey. Nos.
1-19. (Government Printing Office, Washington, 1884-6.)

N addition to the large volumes of the Annual Reports, and the
magnificent Monographs, the United States Geological Survey

are also issuing a series of Bulletins, each on a special subject and
complete by itself. Nineteen of these papers have already been
published. Some of them, it is true, treat of subjects which are but
remotely connected with geological research, as, for instance, “ Gold
and Silver Conversion Tables,” giving the coining value of Troy
ounces of fine metal, etc., and “ Boundaries of the United States and
of the several States and Territories ;” others, though not directly
geological, are of great practical value to all geologists working in
the United States and Canada, as, for example, “A Dictionary of
Altitudes in the United States’ and “ Elevations in the Dominion of

Reviews—Paleontologia Indica. 173
Canada ;”’ whilst others are of interest to geologists generally. We
regret that space does not permit us to mention more than the titles
of the Bulletins of this latter description ; it may suffice to state
that their respective authors are all well-recognized authorities on
the subjects of which they write. The following are on paleonto-
logical matters:—‘“ On Mesozoic Fossils,” by Dr. C. A. White, who
also contributes papers ‘On the Mesozoic and Cenozoic Palzontology
of California,” and “On Marine Eocene, Freshwater Miocene, and
other Fossil Mollusca of Western North America.” “On the Fossil
Faunas of the Upper Devonian along the Meridian of 76° 380’,” by
Prof. H.S. Williams. ‘On the Cambrian Faunas of North America,”
by C. D. Walcott. ‘On the Quaternary and Recent Mollusca of the
Great Basin,” by R. H. Call; and “On the higher Devonian Faunas
of Ontario County, New York,” by J. M. Clarke.

The following treat of petrological and mineralogical subjects :—
“On Hypersthene-Andesite and on Triclinic Pyroxene in Augitic
Rocks,” by Whitman Cross, with a geological sketch of Buffalo
Peaks, Colorado, by S. F. Emmons; ‘On Secondary Enlargements
of Mineral Fragments in certain Rocks,” by R. D. Irving and C. R.
Vanhise; “A Crystallographic Study of the Thinolite of Lake
Lahontan,” by EH. 8. Dana; and “On the Development of Crystal-
lization, etc.,” by Arnold Hague and J. P. Iddings.

Besides the above, Mr. George F. Becker contributes “ Notes on
the Stratigraphy of California,” and MM. Jules Marcou and J. B.
Marcou, “‘ A Catalogue of Geological Maps of America (North and
South) 1752-1881.”

These Bulletins, in all cases where the subject-matter requires
illustration, are furnished with well-executed plates, in one instance
these are beautifully coloured. Further, these papers will not be less
appreciated on account of the fact that they are published at such
moderate prices as to bring them within the means of all geologists.

Garon ble

T]l.—Memorrs oF tHe GrontocicaL Survey oF Inpra. PanmonTo-
nogia InpicaA. Ser. X. Inpran Tertiary anpd Post-TERTIARY
VERTEBRATA, Vol. III. Parts 7 and 8. Srwanik Crocopiria,
LacErTILIA AND OpHtpIA; AND TrerRTIARY Fisnes. By Ricnarp
Lyperker, B.A., F.G.S., with ten plates, xxvili-xxxvii. (Lon-
don, Triibner & Co.)

E noticed the previous issue of this important serial of Indian

Paleontology in August last (see Grou. Mac. 1885, Dec. IIT.

Vol. II. p. 371). The present part, which completes vol. iii., contains

the Crocodilia, which occupy seven plates, some fragmentary remains
of Lacertilia and Ophidia, Sharks, Siluroid fishes, etc.

The Crocodilia comprise only two species of true Crocodile,
namely, C. sivalensis, Lyd.,and C. paleindicus, Fale. ; five species are
referred to Geoffroy’s genus Gharialis, namely, G. gangeticus, G.
hysudricus, G. curvirostris, G. leptodus, G. pachyrhynchus, and a single
Species toa new genus, Lhamphosuchus, viz. kh. crassidens. Some

174 Reviews—Paleontologia Indica.

of these old Gharials attained to enormous size, judging by the pro-
portions of the parts preserved in the Falconer and Cautley Collec-
tion in the British Museum (Natural History), Cromwell Road, and
in the Geological Survey Museum, Calcutta. Thus, “ G. pachyrhyn-
chus, from the Lower Siwaliks of Sind, was between two and a half
and three times the size of full-grown existing specimens of G. gange-
ticus, which attains a total length of twenty feet. If the same pro-
portions obtained in this fossil species, its total length would have
been from fifty to sixty feet.” (p. 21.)

A portion of a humerus of a Varanus indicates in a similar manner
a lizard perhaps twice the size of the largest existing species (V.
salvator), which, according to Mr. Theobald, attains a length of nearly
seven feet; so that V. stvalensis, Falconer, may have been as much as
from 12 to 14 feet long.

This Memoir also makes us acquainted with a series of ophidian
vertebre referred by the author to Python, and probably identical
with the Python molurus, Linn. sp.

Many of the remains here described and figured were collected
thirty years ago or more by the late Sir Proby T. Cautley, and a few
have been described already by Dr. Hugh Falconer, F.R.S.

The fish-remains described embrace teeth of sharks, referred to
Carcharias, sp.; and Carcharodon, sp., from the Siwaliks ; palatal
teeth of Rays, Myliobatis, from the Eocene of Kach; teeth of
Sparide (Capitodus) ; Ophiocephalida, cranium of Ophiocephalus, and
numerous cranial plates of Siluride, ete., very like, or identical with
living Indian forms, This part also includes the Title-page, Index,
and some Introductory Observations to complete Vol. III. of Series
X. Some excellent figures of Mustodon-molars accompany and
illustrate the Introductory Chapter, with which, when bound, the
volume will commence.

This great work, carried out under the able administration of the
Superintendent of the Geological Survey of India, Mr. Henry B.
Medlicott, M.A., F.R.S., has of late years been wholly prepared by
Mr. Lydekker, and printed, and illustrated, in England, and has thus
had the best possible care and every advantage in its production ; yet,
nevertheless, it is sold at a lower price than any similar publication
in Europe or America. We wish the publications of the Indian
Survey the success they so richly and honourably deserve, and we
compliment Mr. Lydekker, the author of the present volume, upon
‘the completion of this section of his very excellent Indian Mono-

raph.

: It is interesting to mention, for the information of English
Palontologists, that a large number of the type-specimens figured
in the volumes of the “ Palzontologia Indica” are to be seen in the
cases of the Geological Gallery of the British Museum (Natural
History) ; so that this magnificent work is in a measure an illustrated
and descriptive catalogue, not only of the Calcutta Museum, but in
part also of our own Indian collections at home.

Reviews—R. Lydekker’s Catalogue, Fossil Mammalia. 175

I1J.—Cartatoeus or THE Fossit Mammatta In THE British Museum
(Naturat History), CRomwEetL Roap, §8.W. Parr II.’ Con-
TAINING THE ORDER UNGULATA, SUB-ORDER ARTIODACTYLA. By
Ricwarp LyprexKer, B.A. 8vo. pp. i—xxii. and 38241, illus-
trated by 39 Woodcuts. (London, 1885, printed by Order of
the Trustees.)

ITH praiseworthy zeal Mr. Lydekker has finished another

volume of the Catalogue of Fossil Mammalia in the Geolo-

gical Department of our National Museum; indeed we are assured

a third part is now actually passing through the press and will be
issued this Spring.

The present section is a very large one (nearly 350 pages in
extent), and is illustrated by thirty-nine woodcuts. It is confined
entirely to one sub-order of the Ungulata, or hoofed-animals, the
ARTIODACTYLA, or even-toed Herbivora. In this sub-order are in-
cluded the Bovide, Girafide, Cervide, Camelide, Tragulide, the
Suide, Phacocheride, and Hippopotamide, all of which families have
living representative species; also the families Dichodontide, Coeno-
theriide, Anoplothertide, Oreodontide, Merycopotamide, Anthraco-
theriide, Cheropotamide, and Listriodontide, all the species of which
are extinct. The following definition of the Artiodactyla may be
acceptable.” In this sub-order the premolar and molar teeth are not
alike, the former being single, and the latter two-lobed. The last
lower molar of both the first and second dentition is almost in-
variably three-lobed. The nasal bones are not expanded posteriorly.
They have no alisphenoid canal. The dorsal and lumbar vertebree
together are always nineteen, though the former may vary from
twelve to fifteen. The femur is without a third trochanter. The
third and fourth digits of both feet are almost equally developed and
their ungual phalanges are flattened on their inner or contiguous
surfaces, so that each is not symmetrical in itself; but when the two
are placed together, they form a figure symmetrically disposed to a
line drawn between them. In other words, the axis or median line
of the whole foot is a line drawn between the third and fourth digits,
while in the Perissodactyles (uneven-toed Ungulates) it is a line
drawn down the centre of the third digit. The distal articular sur-
face of the astragalus is divided into two nearly equal facets, one for
the navicular and one for the cuboid bone. The calcaneum has an
articular facet for the lower end of the fibula.

The Artiodactyla are naturally separable into two very well marked
subdivisions, namely :—

A, The SrLEnoponta—including the numerous extinct genera and
also the existing types of true Ruminants, and

B. The Bunoponra—containing the families of the Hippopo-
tamide and the Suide.

Both these divisions are very well characterized by their dentition.

1 Part I. of this Catalogue—containing the Orders Primates, Cheiroptera, Insecti-
vora, Carnivora, and Rodentia—was noticed in the Grou. Mac. 1885, Decade III,
Vol. II. p. 321.

* See Prof. Flower’s Article ‘“‘ Mammalia,’ Encyclop. Britannica, 9th. edit. vol. xy,

176 =Reviews—R. Lydekker’s Catalogue, Fossil Mammalia.

The Selenodont (crescent-shaped) type of dentition is closely asso-
ciated with the Ruminants and evidently has a direct relation with
the cud-chewing habit of the Artiodactyle; whilst the Bunodont (or
hill-toothed type) are well exemplified in the molar teeth of both
the pig and river-horse, a pattern of tooth not met with out of this
division save in certain Mastodons and in the teeth of Halitherium.

With regard to a large number of extinct forms, their true affini-
ties are of course somewhat conjectural ; nevertheless we may pretty
safely infer that they were very near to, if not actually to be classed
with the Ruminants proper (where the teeth are known). Mr.
Lydekker commences his catalogue with the Bovide, under which
section are included the Oxen, Bisons, Sheep, Goats, Antelopes and
Giraffes. Following Boyd Dawkins and other authors, Mr. Lydekker
sinks the great Bos primiyenius into a mere gigantic ancestor of Bos
taurus, and he does the same with the little Bos longifrons.

The other bovine species which remain are all foreign and Indian
forms. The Bison retains its distinctness, and the Buffalo with its
various Indian species. Then follows the Musk-sheep, which appears
to have two extinct Pleistocene relatives in North America (probably
only local varieties), about which little is known.

Succeeding these are the Sheep, Goats, Gazelles, Antelopes, com-
pleting the hollow-horned ruminants. Next after these are placed
the Giraftidee, with which are included the extinct genera Sivatherium,
Bramatherium, Helladotherium; this last was formerly considered
as the hornless female of Sivatherium, but it is now established as a
distinct genus by Gaudry and Lartet, and also by Riitimeyer. Re-
mains of the true Giraffe are also found fossil in India and elsewhere.

The solid-horned Deer-tribe follow next in order, with rugged
branching antlers of true bone without a horny sheath, but covered
during their growth with vascular integument coated with short
hair. When their growth is finished, the supply of blood is cut off,
the skin dies and peels off, leaving the bone bare and insensible, and
after a time, by a process of absorption near the base, it becomes
detached from the skull and is “shed,” an event which occurs
annually. After a time a new pair of horns are developed from the
peduncles or base of the original pair. The collection affords ex-
amples of 38 species of Corvide—ineluding the Roebuck, Elk, Rein-
deer, Gigantic Irish-deer, Fallow-deer, Red-deer, and a long series
of extinct species, among which Cervus tetraceros from the Pliocene
of France, and the Cervus giganteus from Ireland, are the most in-
teresting and uncommon forms of simple straight-tined, and broadly
palmate types.

The Camels offer no interest to the paleontologist, as they appear
to have undergone scarcely any modification from existing species ;
but many of the ten extinct families which follow date back to the
Kocene, such as the mnaplodhentde, the Anthracotheriide, the Cono-
thertide, etc.

If we except the Uiveiledicaenis the Dorcatherium and some few
others, the greater number of these species are founded merely on
teeth, jaws, bie. and but seldom upon associated skeleton remains ;

Reviews—R. Kidston’s Catalogue, Fossil Plants. ne Ui

from what we do know, however, concerning these earlier species,
they are seen to be of the greatest interest, as offering forms inter-
mediate in dentition, by which the ruminants and non-ruminants can
in a measure be connected together, and also the Perissodactyla and
Artiodactyla.

The Suid@ are a very remarkable group, being connected by the
Chevrotains with the Deer-tribe (and possibly also with the Perisso-
dactyla and Proboscidea, if not with the Sirenia also in past times).

The principal sources whence these early types of Mammalia have
been obtained are from the Eocene freshwater beds of Hempstead
in the Isle of Wight, the Headon beds, Hordwell, Hampshire ;
Vaucluse, Débruge, Montmartre, Caylux and many other localities
in France; Hesse-Darmstadt in Germany, Pikermi in Greece, and
the Siwalik Hills, India.

Some of the most ancient progenitors of the pig-tribe (Hlotherium)
also date back to the Hocene of Hempstead and the Lower Miocene
of France. The Hyotherium is also regarded as an ancestral form
of Sus or Dicotyles.

Sus giganteus and Sus titan, both from the Indian Siwaliks, were
amongst the very largest ancestral forms of the Pig family.

The Hippopotamide, of which a short notice was given in the
March Number of the GroLtocicaL MaGazine (p. 114), appear at a
less early date than the pigs, but are of extreme interest. They are
confined to the old world, over which they seem to have been very
widely distributed in Pliocene and Quaternary times, but they are
restricted now to the rivers and coasts of the African continent.

It is hardly possible to over-estimate the advantage derived by the
publication of these Catalogues. They are an embodiment of all the
(too-frequently) unwritten traditions concerning specimens in our
grand National Collection, and Mr. William Davies has largely con-
tributed, by his unostentatious, but earnest labours, to bring the
remains of the fossil Mammalia in the Geological Collection into
such a state as to enable them to be catalogued by Mr. Lydekker,
a task too, in which, as stated in the preface, he has taken no small
share. It is gratifying to be able to state that this portion of the
geological galleries is in a highly satisfactory state, and reflects the
greatest credit on the staff who have arranged it in so admirable
a manner.

TV.—CatTaLoGuE OF THE PaLmozoric PLANTS IN THE DEPARTMENT
oF GroLocy aNnD PatmonToLocy, British Museum (Naturan
History). By Roserr Kinston, F.G.8. 8vo. pp. vill. and 288.
(London, 1886, printed by Order of the Trustees.)

R. ROBERT KIDSTON has been favourably known for some
time past as a diligent worker in fossil Botany, and he has
confined his attention mainly to the plant-remains of the Coal-
formation.
Having named and catalogued the Coal-plants in the Museum of
Science and Art, Edinburgh, and also contributed several papers to
DECADE III.—VOL. I1I.—NO. Iv. 12

178 Reviews—R. Kidston’s Catalogue, Fossil Plants.

scientific journals on paleeobotanical subjects, he was entrusted in
1883 with the task of naming and cataloguing the Paleozoic
plants in the Geological Department.

The present work, which was only completed at the end of 1885,
is the result.

The plants catalogued are divided into Permian, Carboniferous,
Devonian, and Silurian, of which the Carboniferous form by far the
largest group.

The Permian contains 39 species.
», Carboniferous contains 218 ,,
», Devonian Ab Be} 55

», Silurian on) yl is
The total number of recognized species represented in the Collection being 305.

It is probable that this number might be greatly increased, and
that it does not represent more than a quarter of the total number of
fossil plants described from the Paleozoic rocks of the whole world.

The method adopted by the author has been to give a complete
bibliography of each species; this has entailed an enormous amount
of labour, and largely serves to increase the bulk of the present
catalogue. Should a new Edition be prepared, we would recommend
the author to eliminate all but the important and essential references,
and so thereby to greatly reduce the number of pages, whilst largely
increasing the real usefulness of the work for purposes of reference.

Another feature of this work consists in the critical remarks, often
extending to essays of from one to five pages in length, on questions
bearing upon the structure or interpretation put by various authors
on the fossil plant-remains recorded in the Catalogue.

Here is an example of one of Mr. Kidston’s dissertations taken at
random from the Catalogue :—

Lerprorutotios, Sternberg, 1825.

Versuch eines geognostisch-botanischen Darstellung der Flora der Vorwelt, vol. i.
fase. iv. p. 13.

Lepidophloios laricinus, Sternberg.

Lepidophtoios laricinus.
Boulay, Terr. Houil. du Nord de la France, p. 38.

[Here follow 41 references to works by various authors in’ which
this genus is quoted. These we omit. |

(2) Ulodendron tumidum.
Carruthers, Monthly Micro. Journ. p. 154, pl. xliii. figs. 5, 6, 7, 1870.

Remarks.—It has been shown by Feistmantel, in his Steinkohlen-Flora von
Kralup in Bohmen,! that Ha/onia, Lindley and Hutton, is only a fruiting branch of
Lepidophloios laricinus, Sternberg, and later the same relationship of Halonia to
Lepidophioios has been further explained by Dr. Macfarlane (Trans. Bot. Soc.
Edinb. vol. xiv. p. 181, pls. vii. and viii.2). These figures alone, one would think,
were sufficient to place the affinities of Ha/onia outside the circle of discussion, but
notwithstanding the conclusive evidence they afford on this point, the view held by
these writers has not been universally accepted.*

1 Abhandl. der k. Bohm. Gesellschaft der Wissensch. vi. Folge, vol. v. 1871.

2 Dr. Macfarlane’s Lepidophioios is not L. laricinus, Sternberg, but a new species
for which I propose the name of Lepidophioios Scoticus.

3 See Renault, Cours d, Bot. Foss, p. 53, 1882.

Reviews—R. Kidston’s Catalogue, Fossil Plants. 79

Mr. Carruthers has also figured a specimen of Halonia attached to Lepidophloios,"
which is in the Collection. The conclusion arrived at by him was very similar to
that mentioned by Feistmantel, that Halonia was only a condition of Lepidvphioios.
Both on the Halonian-branch and the main stem of this example some of the
characteristic leaf-scars of Lepidophloios are shown. ‘Those on the Halonia portion
are normal in form and point downwards, but on the main stem from some cause,
perhaps pressure or distortion during or aiter mineralization, the leat-scars are
arranged at right angles to the direction they ordinarily hold on the stem ; hence the
two lateral angles of the leaf-scar lie parallel to the direction of growth, and the scar
of the vascular bundle so twisted round, occupies one of the lateral angles.

In his last memoir on the ‘‘ Organization of Fossil Plants of the Coal Measures,” #
Dr. Williamson gives a figure (pl. xxxiv.) of Halonia attached to a Lycopodiaceous
stem. He says,® ‘‘ In my second memoir (Phil. Trans. 1872, p. 222), read in June,
1871, I said, ‘I have little doubt but that Hadonia was a fruiting branch of a
Lepidodendron ;’ and in a note added in April, 1872. I affirmed absolutely, ‘ First, that
Halonia belongs to the upper branches of a Lepidodendroid tree, consequently it
cannot be a root;’ ‘secondly, we learn that Halonia is a specialized branch of a
Lepidodendroid tree that is not itself a Halonia.’’? . . . ‘The specimen now
described is unquestionably not a Lomatophloios, but a true Lepidodendron,” In
describing his specimen, he says further (p. 468), that at the lower portion of the
branch the leaf-scars have exactly the same form as those of L. selaginoides and L.
elegans, Lindley and Hutton. I have already mentioned that the leaf-scars on the
specimen described by Mr. Carruthers are so turned round on the stem that instead of
their greater diameter being transverse to the stem, as is normally the case in
Lepidophloios, it is vertical. Dr. Williamson’s figure does not show clearly the form
of the scars further than that the vertical diameter of those on the lower part of the
stem seems greater than their transverse breadth. The leaf-scars towards the upper
portions of the specimen are rhomboidal. I am inclined to think there is here a case
of distorted leaf-scars on the lower part of the fossil. similar to that occurring in
Mr. Carruthers’ specimen, where, notwithstanding this peculiarity, the fossil is
clearly identifiable as Lep:dophloios laricinus.

With such an imperfectly preserved example as Dr. Williamson’s appears to be,
any conclusion derived from it is of doubtful value, and though from an examination
of his plate one cannot affirm his fossil is a Lepidophloios, equally one cannot say it
is a Lepidodendron.

‘The figures given by Feistmantel and Dr. Macfarlane are conclusively affirmative
that at least some Ha/onia specimens belong to Lepidvphioios, whereas we have no
example which shows in an undoubted manner that any Halonia fossil can be referred
to Lepidodendron. My own opinion is that Ha/onia is exclusively related to Lepido-
phioios as its fruiting branch. Of course, those authors who place Lepidophioios
laricinus, Sternberg, in Lepidodendron, may consistently say that Halonia is the fruit-
ing branch of Lepidodendron, but I am not aware that any recent writer has followed
this classification.

Lepidophtoios and Lepidodendron I regard as essentially distinct genera. Lomato-
pihloios is now united with Lepidophloios, hence I understand Dr. Williamson's state-
ment that ‘The specimen now described is unquestionably not a Lomatvphlotos, but
a true Lepidodendron,” which is equivalent to saying that it is nota Lepidophiotos, but
a Lepidodendron.

Sigillaria Menardi, Goldenberg (Flora Sareep. Foss. pl. vil. fig. 1), appears to be
referable to Z. daricinus. The central point of the leaf-scars of this figure is
probably the tubercle with which the leaf-supporting pedicels of this plant are
frequently provided, as pointed out by Weiss. U. twmidum, Carr., the type of
which is in the Collection, is, I think, also referable to LZ. daricinus. 'The leaf-scars
are not well preserved on his type, but it probably finds its place here. It is not, at
any rate, a Ulodendron as defined by Lindley and Hutton, for it shows more than two
rows of the larger scars on the circumference of the stem, a third row appearing on
the side not shown in Mr. Carruthers’ figure.

Halonia tubereulata, Eichwald (Letheea Rossica, vol. i. p. 148, pl. xi.), is another
instructive example as illustrating the affinities of Halonia. The core out of this
specimen is atypical Ha/onia, the impression Lepidophioios. In such examples as

1 Grou. Maa. Vol. X. April, 1873. ? Phil. Trans. 1883, clxxiv. p. 459. ° le. p. 469.

180 Reports and Proceedings—

these a layer of cortical tissue from between the core and the impression has evidently
been removed by decay, after the cortical cylinder had been filled with sediment and
the impression of the outer surface of the bark had been imparted to the surrounding
matrix. An example in the Collection shows the same conditions—a removable
Halonia core from a Lepidophioios impression.

The plant figured as Anorria Sellonii, by Lindley and Hutton (Fossil Flora, vol.
u. pl xevii.), appears to be a compressed specimen of ZLepidophioios. 1 have
examined this type in the ‘‘ Hutton Collection,’’ of which their plate does not give a
very correct idea.

I am unable to discover from what evidence Renault has restored his Lepidophloios,
as represented in his Cours d. Botan. Foss. 1882, pl. xi. fig. 1. It appears to
possess the large scars of one genus and the leaf-scars of another.

Horizon.—Coal Measures.

Localities.— British. Staffordshire: Ipstones.

Foreign. Bohemia: Radnitz. Silesia: Waldenbure.

Space precludes our giving a fuller notice of this Catalogue. An
index and list of works quoted completes the book.

Mr. Kidston has visited numerous localities in search of species,
and has added by his exertions nearly 250 specimens to the
collection; it is hoped that other gaps which at present exist will
ere long be filled by further donations.

SaaS OissalsS) LIND) 12154{O\C saa DAN ES

5 4
Groxtocicat Soorrty oF Lonpon.

J.—Annvat Generat Meeting, February 19, 1886.—Prof. T. G.
Bonney, D.Sc., F.R.S., President, in the Chair.

The Secretary read the Reports of the Council and of the Library
and Museum Committee for the year 1885. In the former the
Council stated that they had the pleasure of congratulating the
Society upon an improvement in the state of its affairs, both from
a financial point of view and on account of an increase in the
number of Fellows. The number of Fellows elected during the year
was 04, and the total accession amounted to 51; while the losses by
death, resignation, etc., amounted to 46, making an increase of five in
the number of Fellows. The number of contributing Fellows was
increased by 15. The Balance-sheet showed an excess of Income
over Expenditure during the year of £347 18s. 2d. The Council’s
Report further announced the awards of the various Medals and of
the Proceeds of the Donation Funds in the gift of the Society.

In handing the Wollaston Gold Medal to Mr. Warington W. Smyth,
T.R.S., for transmission to Prof. A. L. O. Des Cloizeaux, the President
addressed him as follows :— ;

Mr. Warington Smyth,—In the absence, which we much regret, of Prof. Des
Cloizeaux, I must request you to transmit to him this Medal.

Geology is the child of two parents, — Mineralogy and Biology. If we look to the
latter to bid the dry bones and buried relies of organisms once more live, we appeal
to the former to disclose the nature and constitution of the earth’s framework whereon
they flourished. It is therefore only just that our Society should seek opportunities of
acknowledging the aid which we receive from mineralogists ; and it would be cifficult
to find one on whom this Wollaston Medal could be more fitly conferred than on

Prof. Des Cloizeaux. To enumerate the papers which he has written would be a
formidable task; they numbered 141, so long as fourteen years ago; what, then,

Geological Society of London. 181

must be the present total? I may, however, point, in passing, to his admirable
“* Manual de Minéralogie,’’ and allude, as more directly bearing on the work of this
Society, to his papers on the classification of hyperites and euphotides, on the geysers
of Iceland, on the action of heat upon the position of the optic axes in a mineral,
and the numerous memoirs on the distinction of minerals by their optical properties,
especially those relating to microcline, and to other species of felspar, of the importance
of which students of microscopic petrology are daily more sensible. I esteem it a
great honour to be the means of carrying into effect the award of the Council by
placing in your hands, to be transmitted to Prof. Des Cloizeaux, the Wollaston
Medal, founded “to promote researches concerning the mineral structure of the
earth.”’

Mr. Warineton W. Smyru, in reply, said:—Mr. President,—It is, Sir, with
more than ordinary satisfaction that I am privileged to receive for, and to transmit to,
Prof. Des Cloizeaux the Medal founded by Dr. Wollaston, No one can fail to ap-
preciate the appropriateness of this award when we consider the researches into the
physical characters of minerals which have contributed so much to the petrological
branch of our science, in which you, Sir, have taken so prominent a part. But it is
more especially in the wide and successful application of Wollaston’s invention of
the Reflection Goniometer that Des Cloizeaux has attained so deserved an eminence,
following closely upon the steps of Prof. Miller, to whom, in his admiral manual, he
paysso highacompliment. The Society will regret to learn that Prof. Des Cloizeaux
has been prevented by domestic anxieties from being present to-day.

The President then presented the Balance of the Proceeds of the
Wollaston Donation Fund to Mr. J. Starkie Gardner, F.G.S., and
addressed him as follows :—

Mr. Starkie Gardner,—The small number of students and the paucity of memoirs
seems to indicate that fossil botany is one of those subjects of which the difficulties
repel rather than fascinate the neophyte. If perhaps these are in some respects less
formidable in the plant-remains of the earlier Tertiary period, if, in studying them,
recent throws some light on fossil botany, yet the practical difficulties of obtaining,
developing and preserving specimens are so great that no little ardour and patience
are demanded from one who devotes himself to the subject. For years this has been
your special work : after thoroughly exploring the flora of the Eocene Tertiaries on
the coast of Hampshire and in the Isle of Wight, you are now, and have for some
time been, engaged in communicating to us the fruits of your labours through the
medium of the Paleontographical Society, thereby earning the thanks of students.
Your researches also of late years have been extended to Antrim, Mull, and even
Iceland, and their results cannot fail to be of the highest interest in regard to the
age of these floras, and their relation to those which occur in the Hampshire district.
In recognition of past and in aid of future work, the Council has awarded to you the
balance of the Wollaston Fund, which I have much pleasure in handing to you.

Mr. Garpner, in reply, said:—Mr. President,—I beg to return my thanks for
the honour the Council have done me in placing the balance of this fund at my
disposal. The amount of leisure 1 am able to command has not permitted me to
contribute towards the advancement of geology in this country in anything like the
same proportion as my professional brethren ; but I think I may fairly claim to
yield to none in my devotion to its pursuit. The subject I somewhat untortunately
monopolize is one of such magnitude that, at the best, very many years of such work
as 1 am able to devote to it must elapse before even a first general impression of the
composition of our Eocene flora can be published. I am, however, so deeply im-
pressed with the importance of the study that I am prepared to sacrifice much in
order that the time required may not be unduly prolonged. I am convinced that in
addition to the ordinary botanical, paleeontological, and evolutionary interest attach-
ing to it, it will be found to present the solution of many problems as to the former
relative positions of land and sea and the climatic changes accompanying their suc-
cessive redistribution. I need hardly add that I regard the award made me this day
as a direct encouragement to persevere in the line of research I have chosen.

The President next presented the Murchison Medal to Mr. William
Whitaker, B.A., F.G.S., and addressed him as follows :—
Mr. William Whitaker,—To many members of the Geological Survey of Great

182 Reports and Proceedings—

Britain since the date of its constitution we are indebted for work freely done—
beyond the sphere of their more strictly professional duties. Its chiefs, from the
days of Sir H. De la Beche to the present distinguished Director-General, Dr. A.
Geikie, have been among the most valued contributors to our Journal, and have en-
riched geological literature by their longer writings; while among its other members,
few have done more than yourself in following the example of its leaders. On the
present occasion I will only allude to the various Memoirs of the Geological Survey,
especially that on the London Basin, in which you have taken so large and im-
portant a share, and will dwell rather on your contributions to our own Journal and
to other publications. Your papers on the western end of the London Basin, and on
the Lower London Tertiaries of Kent, deserve to be ranked with the classic memoirs
of Prestwich as elucidating the geology of what I may call the Home District ; and
your last contribution to its deep-seated geology is still too fresh in our memories to
need more than a mention. We do not forget your varied and valuable contributions
to the GroLocicaL Magazine, especially those on the Red Chalk of Norfolk, on
the Water-supply from the Chalk, on the formation of the Chesil Bank (written
jointly with Mr. Bristow), a paper, as it seems to me, of remarkable suggestiveness,
and last, but by no means least, ‘On Subaerial Denudation,” in which, as remarked
by the late Mr. C. Darwin, you had ‘‘the good fortune to bring conviction to the
minds ”’ of your fellow-workers by means of ‘‘a single memoir.”

We are also greatly indebted to you for your labours in reference to the history of
the literature of geology, a task involving not a little labour, which, though of the
greatest value to students, is to all unremunerative and would be, to many, exception-
ally toilsome. Of this, your care for several years of the Geological Record, and the
lists of books and memoirs relating to the geology of various counties in England,
are conspicuous instances.

There is a peculiar appropriateness in the award to you of this Medal, founded by
Sir Roderick Murchison, one of the illustrious chiefs of your. Survey, and I have the
greatest pleasure, on behalf the Council of the Geological Society, in placing it in
your hands together with the customary grant from the Fund.

Mr. Wuiraxker, in reply, said that to workers in science the best reward was the
appreciation of their fellow-workers, and of this he had on various occasions received
testimonies ; but the award of this Medal was the crowning one, knowing, as he well
did, the care with which such awards were made. He expressed his interest in the
Geological Survey, to which he had for so many years belonged, and in the important
work done by his colleagues in that Survey. He had a particular pleasure in re-
ceiving this award from the hand of an old friend like the President, whom he
thanked most heartily for the very kind and flattering terms employed by him in
presenting the Medal. He also thanked the Fellows of the Society present for the
cordial manner in which they had received the announcement of the award.

In presenting the Balance of the Proceeds of the Murchison
Geological Fund to Mr. Clement Reid, F.G.8., the President said :—

Mr. Clement Reid,—The later Pliocene and the Pleistocene deposits of East Anglia
offer to geologists a series of problems as difficult as they are attractive. We are
indebted to you for much valuable information on the exact distribution and the fossil
contents of these varied deposits, which owing to peculiar local circumstances often
present exceptional difficulties, and demand exceptionally patient study on the part of
the investigators. Your memoir on the Forest Bed of Norfolk is a contribution of
especial value to students as affording them fuller and more precise information than
could previously be obtained, while the pages of our Journal and of the GroLoercaL
Maceazine testify to the zeal and thoroughness with which you have applied yourself
to these and kindred questions. In conferring upon you this award from the
Murchison Fund, which I have great pleasure in placing in your hands, the Council
of the Geological Society hopes that it may aid you in prosecuting your studies in
this department of geology and extending them to localities which could not be
visited by you in the discharge of your professional duties as a Member of the
Geological Survey of Great Britain.

Mr. Cirement Rein, in reply, said:—Mr. President,—I have sometimes felt dis-
couraged at the small results of my work. But this welcome and unexpected award
by the Council of the Geological Society is a recognition that the work is not con-
sidered altogether worthless, and will encourage me still to persevere. Though a
large portion of my observations have been made in the course of the Geological

Geological Society of London. 183

Survey, I have also devoted my leisure time to the study of various questions in
Pleistocene and Pliocene Natural History. This award of the Murchison Fund will
now enable me to undertake a more thorough examination of many of the less-known
deposits.

The President next presented the Lyell Medal to Mr. William
Pengelly, F.R.S., F.G.S., and addressed him as follows :—

Mr. Pengelly,—The Council of the Geological Society has awarded you the Lyell
Medal and a sum of twenty guineas from the Fund in recognition of your lifelong
labours in the cause of geology, and more especially of your investigations in those
caverns of the south-west of England by means of which our knowledge of the con-
dition of Britain during the latest epoch of geological history has been so largely
augmented. ‘To exhume the contents of a cavern, not only the lair of wild beasts,
but also an abode of men in those ages when, to quote the words of the old Greek
tragedian,

‘‘ Like tiny ants they dwelt in sunless caves,’’!

requires the exercise of unwearied patience and, in addition, of extensive knowledge
and critical acumen. By the labours of the Committee, of which you were the hands
and the eyes, and at least a fair proportion of the compound brain, Mr. MacEnery’s
long-neglected discovery in Kent’s Hole was placed beyond all dispute, and the con-
tents of that cavern, its succession of deposits, its relics of extinct animals, and its
tools of stone and bone, denoting more than one stage of civilization, have been made
known to the world.

In like way the virgin ground of the Brixham cave was investigated, and its
valuable contents have been rendered accessible to students. All this you have done,
not as the fruit of secured leisure, but in the intervals of a busy life, of which, in the
full sense of the words, time was money ; and you began this work at a period when,
owing to mistaken prejudices, you incurred no small risk of obloquy and personal loss.
Your work at Bovey Tracey and your papers on the later geology of Devonshire and
Cornwall are too well known to need more than a passing allusion; the Torquay
Museum and the Transactions of the local societies will be a lasting monument of
your zeal in stimulating scientific researches in the neighbourhood of your home.
‘There is a peculiar fitness in the award to you of this Medal. a memorial of the fearless
and illustrious author of the ‘‘ Principles of Geology ’’ and of the “ Antiquity of Man.”’
I esteem myself exceptionally fortunate in being commissioned to place it in your hands,
and being thus enabled to testify my regard for so valued and genial a friend.

Mr. Pencetty, in reply, said that he could not conceal from himself, and did not
wish to conceal from the Fellows, the gratification that he felt at receiving this award.
He had studied Geology for some fifty years, although he had appeared but little in
the rooms of the Geological Society, his publications on geological subjects having
been chiefly contributed to those local Societies in whose neighbourhood his researches
had been carried on. His gratification at this award compensated for much obloquy,
especially as it bore the name of an old and loved friend with whom he had worked
much and often. No doubt the founder of the Medal intended that its award should
serve not only as a reward for work done, but asa stimulant to further exertion. It came
to him so late in the day, however, that he could hardly hope to do very much more ;
but although he himself might not be urged by it to renewed efforts, the stimulus
might act vicariously, as the knowledge that he had received this recognition of such
services as he had rendered to science would doubtless get spread abroad in Devon-
shire, and would probably serve as an incitement to many local workers to persevere
in their studies.

In handing the Balance of the Proceeds of the Lyell Donation
Fund to Dr. Henry Woodward, F.R.S., F.G.S., for transmission to
Mr. D. Mackintosh, F.G.S., the President addressed him as follows :—

Dr. Woodward,—I have much pleasure in placing in your hands, as representing
Mr. Mackintosh, the balance of the Lyell Donation Fund awarded to him by the

Council of the Geological Society. In him we have a second instance of the way in
which, through an untiring zeal for science, the rare intervals of a hard-worked lite

1 ZEschylus, Prom. Vinct. 491,

184 Reports and Proceedings—

may bear fruit so largely augmenting the common stock of geological knowledge.
There are few problems more interesting than that of the physical condition of our
native land during the period commonly designated the Glacial Epoch ; but tor its
solution an exact knowledge of the distribution of erratics and an identification
of their points of departure is absolutely necessary. ‘Those who, like myself, have
attempted to adjust the rival claims of glacier and floe, of the ice-chariot versus the
ice-ship, as vehicles of boulder-transport, can hardly speak too highly of the value
of the papers on British erratics which he has contributed to our Journal and to
other publications. I trust that this award may not only be gratifying to him as a
mark of our appreciation, but also help him in continuing his labours in a field where,
notwithstanding them, much still remains to be done.

Dr. Woopwarp, in reply, said :—Mr. President, —The intelligence of the decision
of the Council has had a most cheering effect on Mr. Mackintosh, and will brighten
the remaining years he may have left to him. It is well known to Fellows of this
Society what has been the nature of Mr. Mackintosh’s work, and what good and
careful observations he has made, extending over long years of wandering up and
down through England and Wales, and carefully observing wherever he went. I
cannot do better than read the following letter trom Mr. Mackintosh, which, indeed,
is addressed to yourself. He says:—‘‘In thanking you for the honour conferred
upon me by the Award of the Lyell Donation Fund, I may mention the fact that
25 years ago I was elected a Fellow of this Society, and that Sir Charles Lyell was
one of those who signed my certificate. I am now seventy years of age; this is the
second occasion that my work has been so much honoured, for I am proud to be able
to state that I was presented with the Kingsley Medal of the Chester Society of
Natural Science in 1881.”

The President them handed the Award from the Barlow-Jameson
Fund to Dr. W. T. Blanford, F.R.S., for transmission to Dr. H. J.
Johnston-Lavis, F.G.S., and addressed him as follows :—

Dr. Blanford,—I will ask you to transmit this Award to Mr. Johnston-Lavis.
In this country happily the volcanic fires have long ceased to glow, and the earthquake
seldom causes more than a transient tremor. It is otherwise on the shores of the
Bay of Naples, where again and again during the last eighteen centuries Vesuvius
has rained down ruin; and of late years the earthquakes of Ischia have wrought
destruction on the works, and desolation in the homes, of men. It is true that these
phenomena of the darker side of nature have not been unobserved by the many illus-
trious men of science to whom Italy has given birth ; but ‘‘ the curse of Babel’’ has
debarred some of us from access to their works. ‘This alone gives an exceptional
value to the elaborate studies which Mr. Johnston-Lavis has undertaken of the various
eruptive-products of Vesuvius, and of the Ischian earthquakes. There is yet another
advantage, that natural phenomena should be studied by men of different nations,
diverse training, and varied habits of mind. In recognition of his past labours and
in furtherance of future work in the vicinity of Naples, the Council has awarded to
him a grant from the Barlow-Jameson Fund, which I have much pleasure in placing
in your hands.

Dr. Buanrorp, in reply, said that the best mode of replying to the kind remarks
made by the President would be to read a letter which he had received from Dr.
Johnston-Lavis. That gentleman said :—

“Tt was with a considerable amount of astonishment and pleasure that I received
your letter announcing the Grant from the Barlow-Jameson Fund, since the news
was so perfectly unexpected. The honour thus paid me for my attempts to clear up
some questions in vulcanology and seismology will stimulate me to further follow that
line of investigation, with the hope of adding something more to our knowledge of
those subjects.

‘«My professional work at this season prevents me from having the great pleasure
of being present in person to receive this mark of esteem from the hands of our
President. Will you kindly express my deep gratitude to the Society for so
generously conferring such an honour upon me.”’

The President then read his Anniversary Address, in which, after
giving obituary notices of some of the Members lost by the Society
during the year 1885, he referred to the principal contributions to

Geological Society of London. 185

geological knowledge which have been made during the past year,
both in the publications of the Society and elsewhere in Britain.
The remainder of the address was devoted to a discussion of the
principles of nomenclature which should be followed in regard to
the metamorphic rocks. After describing the nature and relations
of the various metamorphic rocks in certain parts of the Alps,
Canada, Scotland, etc., the effects of the intrusion of igneous rocks,
and the results of pressure in producing changes, both mechanical
and chemical, upon rocks originally crystalline, he pointed out that
these last could generally be distinguished from anterior foliation,
otherwise produced; that many rocks in the metamorphic series
appear to have originated in stratified deposits, but that the evidence
at present in our possession pointed to the very great antiquity of all
these, and to the probability of their having been produced under
conditions which have not recurred since the beginning of the
Paleeozoic period.

The ballot for the Council and Officers was taken, and the following were duly
elected for the ensuing year :—President: Prof. J. W. Judd, F.R.S. Vice-Pre-
sidents: H. Bauerman, Esq.; John Evans, D.C.L., LL.D., F.R.S.; A. Geikie,
LL.D., F.R.S.; and J. A. Phillips, Esq., F.R.S. Secretaries: W. T. Blanford,
LL.D., F.R.S.; and W. H. Hudleston, Esq., M.A., F.R.S. Foreign Secretary :
Warington W. Smyth, Esq, M.A., F.R.S. Zreaswrer: Prof. T. Wiltshire, M.A.,
F.L.S. Councid: H. Bauerman, Esq.; W. T. Blanford, LL.D., F.R.S. ; Prof. T.
G. Bonney, D.Sc., LL.D., F.R.S.; Thomas Davies, Esq. ; Prof. P. Martin Duncan,
M.B., F.R.S.; John Evans, D.C.L., LL.D., F.R.S.; A. Geikie, LL.D., F.R.S. ;
Henry Hicks, M.D., F.R.S.; G. J. Hinde, Ph.D.; J. Hopkinson, Esq.; W. H.
Hudleston, Esq., M.A., F.R.S.; Prof. T. M‘Kenny Hughes, M.A.; Prof. T.
Rupert Jones, F.R.S.; Prof. J. W. Judd, F.R.S.; R. Lydekker, Esq., B.A.; J. E.
Marr, Esq., M.A.; J. A. Phillips, Esq., F.R.S.; Prof. H. G. Seeley, F.R.S. ;
Warington W. Smyth, Esq., M.A., F.R.S.; J. J. H. Teall, Esq., M.A.; W.
Topley, Esq.; Prof. 'f. Wiltshire, M.A., F.L.S.; Henry Woodward, LL.D., F.R.S.

II.—Feb. 24, 1886.—Prof. J. W. Judd, F.R.S., President, in the
Chair.—The following communications were read :—

1. “On two Rhetic Sections in Warwickshire.” By Rev. P. B.
Brodie, M.A., F.G.S.

The sections noticed in this paper were (1) one exposed on a
railway at Summer Hill, near Binton, between Stratford and Alcester,
and (2) one, 15 miles further to the south-east, at Snitterfield, three
miles north of Stratford-on-Avon, in excavations for a tunnel con-
nected with a supply of water to that town.

At the first-named locality a bed with insect remains overlies the
firestone and Hstheria-bed, and this is succeeded in descending order
by a considerable thickness of black and grey shales with the usual
Rheetic fossils. The bone-bed is not exposed.

At the second locality, in borings and shafts, black Rheetic shales
were found in three places resting upon a denuded surface of new
Red Marl, and covered by between 40 and 50 feet of drift. Avicula
contorta and other typical fossils were obtained from the shales.
In other shafts the Rhetic beds were wanting. so that apparently
those met with were merely small portions remaining of a larger
mass which had been denuded away.

186 Reports and Proceedings—

2. “On the Basement-beds of the Inferior Oolite of Gloucester-
shire.” By E. Witchell, Esq., F.G.S.

The author observed that few papers have appeared lately on this
subject in the Quarterly Journal, and admitted that the work done
between 1847 and 1860 was of such excellent character that there
seemed to be but little left to do in the Cotteswolds. Still he con-
sidered, after twenty-five years of experience, that there is room for
another paper on the lower beds :—

(1) Because the Pea Grit of Leckhampton is made to include
too much.

(2) Because this use of the term has led to confusion.

(3) Because the Pea Grit proper has a greater extension than has
hitherto been supposed.

Thus has arisen the mistaken notion that the Oolitic limestone at
Frocester and Haresfield Hills is part of the freestone series above
the Pea Grit. The author proposed to call the beds underlying the
Pea Grit the “Lower Limestone,” and gave sections at Crickley Hill
and Ruscombe, near Stroud, in explanation of his views.

Summarizing the results—(1) The Pea Grit is well developed in the
Cheltenham area, thinning towards the south, is no more than from
three to five feet thick in the Stroud area, extending as far as Uley
Bury, where it occurs as a thin band, having lost its ferruginous
aspect. (2) Underlying this are several beds of white Oolitic Lime-
stone, having layers of freestone alternating with layers of shelly
detritus, and locally small quartz-pebbles, thickness from 20 to 80
feet. Attention was especially drawn to the contrast which these
beds present, both lithologically and paleontologically, to the Pea
Grit; and to their poverty in entire organic remains, limited chiefly
to a few very small and peculiar Gasteropods. (3) Brown sandy
limestones, locally coarse ferruginous gritty beds from 5 to 9 feet,
fossiliferous in the lower portion. These are within the Opalinus-
zone, and repose directly on the Cephalopod-beds.

3. “On the Pliocene Beds of St. Erth.” By Perey F. Kendall,
Esq., and Robert G. Bell, Hsq., F.G.S.

This paper consisted of a description of the beds exposed at St.
Erth, a list of the Molluscan fossils identified, and some preliminary
considerations of the evidence afforded by the Mollusca, and may be
considered a continuation of that by the late Mr. S. V. Wood, read
to the Society in November, 1884.

The beds consist of sand and clay dipping to about 5° to N.N.W.
The only important fossiliferous bed is a blue clay, and fossils have
only been obtained in one spot, though the beds have been traced
over an area of about 120 acres. The fossils are well preserved, and
with a few unimportant exceptions, are of invertebrate forms, chiefly
Mollusca, Polyzoa, Ostracoda, and Foraminifera ; remains of Crabs,
Cirripedes, Echinoderms, Annelida, Sponges, and even of Holothu-
rians and Tunicata (e.g. Leptoclinum tenue ?) have been detected.

The list of the Mollusca showed the range of each species in
Miocene and Pliocene beds and in the present seas. The authors
considered that the fossils agree in age with the middle or lower

Geological Society of London. 187

portion of the Red Crag, but that whilst many species having a
southern character are present at St. Erth, and wanting in the Crags
of the East coast, the Boreal and Arctic forms found so abundantly
in the Crag are absent at St. Hrth.

In explanation of this remarkable fact, it is suggested that when
the St.-Erth beds were deposited, although the North-Sea area was
in direct communication with the Arctic Ocean, the western part of
the British Channel was not, that the British Isles were joined to the
continent of Europe on one side and to Greenland on the other, the
Shetland and Faroe Islands and Iceland being the remnants of
the barrier that formerly divided the Atlantic from the Arctic Sea.
Evidence is given in support of this view from the present sub-
marine configuration of the North Atlantic. It was also shown to
be probable that the St.-Hrth area, in Pliocene times, was more
directly connected with the Mediterranean than at present, by a
marine channel that traversed France.

TII.—March 10, 1886.—Prof. J. W. Judd, F.R.S., President, in the
Chair.—The following communications were read :

1. “On the Alteration of coarsely spherulitic Rocks.” By Gren-
ville A. J. Cole, Hsq., F.G.S.

The author stated that the pitchstone of Zwickau, Saxony, contains
large spherulites, remarked on by Cotta in 1847, which are devoid
of radial structure, and are traversed by the fine lines of flow that
characterize the glassy matrix. The centre of each of these has been
hollowed out by decomposition along cracks, as may be seen at the
ends of the branches into which the cavity divides, and infiltration
of chalcedony and calcite has occurred. The lines of flow corre-
spond on opposite sides of this secondary mass, and do not bend
round as if the spherule had formed about some calcareous inclusion
or about avesicle. Similar excavation and infiltration have occurred
extensively among the coarsely spherulitic layers of the Precambrian
rhyolites of Lea Rock, Wrekin, and in these the cracks traversing
the rock are seen, under the microscope, as mere lines when passing
through the matrix, but widen out at once probably through more
ready decomposition along their walls, when they enter spherulitic
matter. In the white rock (Silurian rhyolite) of Digoed, near Pen-
machno, N. Wales, similar alteration has converted the closely set
spherulites (often three inches in diameter) into mere shells filled
with quartz and chlorite; while a black slate-like decomposition-
product, with a hardness of 2°5 and a specific gravity of 2°77, occurs
occasionally here, and very frequently in the less coarse but similar
rock of Conway Mountain. In the latter place spherulites may be
found containing this product in alternate concentric layers. Analysis
shows it to be allied to pinite; but the formation in it, when it tends
to become crystalline, of microlites of various kinds, opposes its
being regarded as a simple mineral. The rock of Digoed itself
contains 83 per cent. of silica, the black product only 50 per cent.
The great nodular masses of quartz and these contrasted soft, black,
cleavable layers form striking features of alteration, especially as

188 Reports and Proceedings—Geological Society of London.

the residual spherulitic matter closely resembles the matrix, and
may in time become undistinguishable from it. A consideration of
the pyromerides of the continent makes it appear probable that they
also are altered coarsely spherulitic rhyolites, and the comparisons
made by Delesse in 1852 strongly support this view.

2. “Account of a Well-sinking made by the Great Western
Railway Company at Swindon.” By Horace B. Woodward, Hsq.,
F.G.8. With Lists of Fossils, by E. T. Newton, Esq., F.G.S.

This well-sinking was made under the direction of Captain William
Dean, while fossils were collected and notes of the strata were made
by Messrs. W. H. Stanier and A. R. Elliott, to whom the authors
were greatly indebted. The object of sinking was to seek a supply
of water for use in the works at Swindon. ‘The strata proved were
as follows:—

ft. in.

Ma eE STON st iceiy oveRare nen west eh Men uau Cotati se une 8 0
Kammenidge: Clay: via, esc’ css, can dee sens coterie BO Leen
Corallian Beds ae SR ase ae TOOL
Oxford Clay and Kellaways Bockts.cuisutc shaken wens gO 7209
Cornbrash . vale ee Bak ect oaniey cla a utehrchan Pesce ial O mau
Forest Marble Seni vekit, Roe Srisesh Tete, tote ecsamer acess woo.
{a6 62

Unfortunately for the Company, saline waters were met with in
the Corallian roeks, and again in the Forest Marble.

Few fossils were obtained from the Kimmeridge and Corallian rocks ;
but those from the Oxford Clay and Kellaways Rock indicated the
upward succession of the Callovian ornatus- and cordatus-forms of
Ammonites. It was shown that at least 44 feet of clays, sands, and
sandstones might be assigned to the Kellaways Rock, which should
be regarded as an irregular and impersistent basement-bed of the
Oxford Clay. Turning to the subject of the saline waters, it was
shown from analyses by Mr. F. W. Harris that the Corallian water
contained 144 grains per imperial gallon, consisting chiefly of sodium
chloride and sodium carbonate. In the Forest-Marble water, which
had a temperature of 64°, the saline ingredients amounted to 2131
grains per gallon, consisting chiefly of sodium chloride, calcium
chloride, ete.

Attention was then drawn to the occurrence of saline waters in
the Jurassic rocks, at Melksham, Holt, Trowbridge, St. Clement’s,
Oxford, and other localities in the neighbourhood; and also to the
occurrence of saline waters in the Coal-measures and older rocks
of the Bristol Coal-basin, etc. It was shown that the occurrence of
saline waters was not necessarily connected with the proximity of
saliferous New Red rocks, and it was suggested that the saline waters
at Swindon escaped from a ridge of Paleozoic rocks against which
the Lower Jurassic rocks abutted, as they do on the Mendip Hills.

Mr. E. T. Newton said the fossils had been collected with great
care by Mr. Stanier and Mr. Elliott, an exact record of depths being
kept. He noticed some of the more important species that had been
met with and their distribution, especially mentioning that the Am-
monites from the Oxford Clay were nearly all from greater depths
than 400 feet.

Correspondence—Prof. Edward Hull. 189

COR EES Oia se zbae

THE GEOLOGICAL AGE OF THE NORTH ATLANTIC OCEAN.—REPLY
OF PROFESSOR HULL TO PROFESSOR LE CONTE.

Srr,—I have read with much pleasure Professor Le Conte’s views
on the question of the ‘‘ Permanence of Continents and Ocean-
Basins”; and especially with reference to the growth of the North
American Continent.’ I am glad that he does not carry his views
as far as some geologists on this question. As stated, they are
substantially the same as those supported in his ‘“ Hlements of
Geology ” (Edit. 1885). It seems to me, however, that Prof. Le
Conte scarcely realizes sufficiently what must have been the effect
of continued subsidence during the whole of the Paleozoic period
in extending the sea-area, and consequently in pushing the ad-
joining land-area further into that of the present North Atlantic
Ocean. In his ideal-section (Elem. p. 288) of the Paleeozoic rocks
from the Primordial downwards to the Carboniferous, which is
consistent with his statement that the whole of these rocks in the
United States are conformable, Prof. Le Conte makes it clear that
were these strata reduced to the original horizontal position, there
would be several thousand feet of marine sediments, which must
originally have overlapped on the flanks of the lands formed of
Archean rocks. This will, probably, explain to him why in my
sketch-map No. 2 I have carried the northern part of the continental
border westward so as to cut through Labrador, not in ‘“ Primordial
times,” as he supposes, but in Silurian times, when the land-area
was further depressed.’

I am gratified to find that on the question of the position of the
and and sea areas during Archean (or Laurentian) times Prof. Le
Conte is in accord with myself; on the other hand I fully agree with
him as to the immense duration of the ‘ Lost Interval” which
elapsed between the Archean and Primordial eras, and the extent of
the denudation of the raised sea-beds over the American and Kuropean
continents. But, I cannot concur with him in supposing that the
small tracts of land which were (at least partially) maintained in
the North, as the Laurentian ‘‘ Nucleus,” or along the Hast of the
Appalachians (even with a considerable margin including some now
ocean-covered tracts), were sufficient to supply the amount of Palzo-
zoic sediment, which, when originally deposited (i.e. before denudation),
was the measure of the denudation of these tracts themselves. The
conformable relations of these beds throughout a vertical depth of
several thousands of feet imperatively involves the view of the con-
temporaneous existence of an extensive continental area, stretching
both to the north and east of the present margins of the Silurian
strata. Nor, as it appears to me, does Prof. Le Conte recognize
sufficiently (if at all) the significance, in reference to this question,
of that on which I have laid principal stress in my essay ; namely,

1 GrotocicaAL Macazine, March, 1886, p. 97.
* Scient. ‘rans. Roy. Dublin Soc. vol. iii. new ser. plate vii, p. 319.

190 Obituary—Charles Wiiliam Peach, A.L.S.

the increase in thickness of the sedimentary strata towards the north-
east and east of the N. American continent, and their attenuation
and replacement by limestones in opposite directions. In the case of
these sediments they are truncated along their thickest margins; and
the fact, which I have pointed out, that the British and Huropean
formations exhibit similar phenomena of attenuation and truncation,
only in an opposite direction, leads us to a similar conclusion with
reference to the position of the derivative lands. Prof. Le Conte
admits (p. 100) that the great thickness of Carboniferous strata
would require a large land-mass to the east of the Appalachian
region; but, he adds, ‘There is no reason why the eastern land-
mass, which sufficed to contribute 30,000 feet of Silurian and
Devonian sediments, should not have been sufficient to contribute the
much smaller amount of sediments of the Carboniferous period.”
This, however, allow me to say, is begging the question at issue
between us. I maintain in the first place, that the narrow strip of
land (comparatively speaking) allowed by Prof. Le Conte was quite
insufficient for the production of 80,000 feet of conformable sedi-
ments; and secondly, that this continuous accumulation of such
sediments must have caused the originating land-mass to recede
farther and farther eastwards into the Atlantic area, down to the
close of the Carboniferous (or Permian) epoch.

Prof. Le Conte is scarcely correct in stating, that in my map, fig.
3, Ihave completely abolished the Atlantic Ocean by converting it
into land during the Carboniferous epoch. As a matter of fact, I
have indicated the land as far south as lat. 88°—40°, making it in-
tentionally vague at this line. As will be seen, on referring to the
map itself, the main land-areas are represented as occupying the
Arctic regions ; and there is an interesting fact tending to corroborate
the view of the land connection between Europe and America during
both Devonian and Carboniferous times which should not be lost
sight of, viz. the general resemblance, and partial identity, of the
land floras of both regions during these epochs. Altogether it would
appear that there is cumulative evidence of the general correctness
of the views I have endeavoured to enunciate, whether we have
recourse to the organic or physical aspects of the question.

Epwarp Hutt.

@aS cs OeAsee yas

CHARLES WILLIAM PEACH, A.L.S.
Born 1800. Diep 1886.

Cuartes W. Pracn, Geologist and Naturalist, was born in 1800 at
Wansford in Northamptonshire. His father was a harness-maker.
He first went to a dame’s school in the village, and at the age of
twelve was sent to a school at Folkingham in Lincolnshire, where he
remained three years. He was appointed to a post in the Revenue
Coastguard in January, 1824, and sent first to Southrepps in Norfolk,
and afterwards to Weybourn, Cromer, etc. Here he first commenced

Olituary—Charles William Peach, A.L.S. 191

the study of Natural History, and began to make a collection. He
made the acquaintance of the Rev. J. Layton, then living at Catfield.
With this excellent geologist he explored the cliffs and the sub-
merged Forest-bed, and assisted him greatly in collecting the large
series of teeth and bones of elephants which are now preserved in
the British Museum.

From Norfolk Peach was sent to Lyme Regis and Charmouth in
Dorsetshire, and thence into Cornwall, where he worked at the
geological formations along the coasts, and found fossils where no
fossils had been found before. At the meeting of the British
Association held at Plymouth in 1841, he read his first paper entitled
«The Organic Fossils of Cornwall.” The following year at the
Manchester Meeting he read a paper before the Zoological Section, ‘‘On
the Marine Fauna of the Cornish Coast.” Charles Darwin, in his
monograph on the Balanide (Ray Society, 1854, p. 157), quotes Mr.
Peach’s observations on the exuviation of the integument of the
Balani on the Cornish coast. He was acknowledged to be one of
the most original observers in Geology and Zoology, and was taken
by the hand by Murchison, De la Beche, Buckland, Forbes, Daubeny
and Agassiz.

While residing at Fowey, he was made an Honorary Member of
all the local scientific Societies of the Duchy, and he added many
organic remains from the Devonian rocks to the collection of the
Royal Geological Society of Cornwall, and this collection seems to
have remained as he left it nearly 40 years ago.

One of Peach’s most important discoveries was the detecting
remains of Pteraspidian fish-shields, in the Lower Devonian Slates
of Polperro in Cornwall. These fossils were recognized as fish by
Mr. Peach in 1843. In 1851 Prof. Mc‘Coy determined the fossil to
be a Sponge! and named it Steganodictyum Cornubicum. Prof. Ferdi-
nand Roemer subsequently determined it to be the bone of a Cuttle-
fish, and named it Archeoteuthis Dunensis (1855) ; and in 1868 Prof.
Ray Lankester, in a note to the Geological Society, stated that
Huxley and Salter, as well as himself, had determined it to be the
cephalic plate of a Pteraspidian fish (Quart. Journ. Geol. Soc. 1868,
vol. xxiv. p. 546), which he described under the name of Scaphaspis
Cornubicus. He says, “The merit of first recognizing the fish-nature
of these remains belongs to Mr. Peach, who more than twenty years
since wrote of them as such” (op. cit. p. 547). -See also Gnou. Mag.
1868, Vol. V. pp. 247-248, and 1869, Vol. VI. pp. 77-78. Mr.
Pengelly, writing on the same subject, says:—‘“‘Mr. Peach’s judgment
has received the fullest justification, and we all congratulate him
heartily on the fact” (Trans. Devonshire Assoc. for 1868).

Having been transferred from the Coast-guard to the Customs,
Peach was removed from Cornwall to the north of Scotland, being
stationed first at Peterhead, and afterwards at Wick. It was whilst
at the latter place that he made the acquaintance of Robert Dick,
the Thurso Baker-Geologist and Botanist, and the account of their
friendship and mutual studies is contained in some of the most
interesting chapters in Dr. Smiles’ “ Life of Robert Dick,” part of

192 Obituary—Charles William Peach, A.L.S.

which book is devoted to a biographical sketch of Mr. Peach, to
which we are indebted for many of our facts. Here he con-
tinued his study of geology and zoology. Whilst travelling round
the coast of Caithness in search of wrecks, he made good use of
his spare time, hammering the rocks in search of fossil plants with
which the dark flagstones of the district abounded. He was the
first to find fossils in the limestones of Durness in Sutherland.
Obscure organic remains had been detected by Macculloch in the
quartz rocks of Sutherland ; but they passed out of mind, and their
organic nature was stoutly denied by Sedgwick and Murchison.
Peach, however, in 1854 brought to light a good series of shells !
and corals, which demonstrated the limestone containing them to
lie on the same geological horizon as some part of the Lower
Silurian of other regions. He also found a new fossil fish, which
was described in the Decades of the Geological Survey. At the
meeting of the British Association at Liverpool, 1854, Peach read a
paper on ‘‘The Remains of Land Plants and Shells in the Old Red
Sandstone of Caithness.” In August, 1858, Mr. Peach accompanied
Sir R. I. Murchison to the Orkney and Shetland Islands, and
finally the two geologists landed at Cape Wrath, and proceeded to
visit the Durness Limestone, where all that Peach had already
discovered was confirmed by the personal observation of Sir
Roderick, who, proceeding to Leeds, laid before the Geological
Section of the British Association, ‘The Results of his Re-
searches among the older rocks of the Scottish Highlands,”
doing full justice to Mr. Peach’s discovery of organic remains of
the Lower Silurian age in the Crystalline Limestone of Sutherland,
similar to those which occur in the Lower Silurian rocks of
North America.

He was a Fellow, and served the office of President of the Royal
Physical Society of Edinburgh.

In 1868 Peach was elected an Associate of the Linnzan Society
of London.

The “Neill Gold Medal” was awarded to Mr. C. W. Peach in
1874, by the Royal Society of Edinburgh, for the addition of about
20 species of Hchini, Meduse, and Sponges made by him to the
known fauna of the British seas.

Though his long and active life had entitled him to rest both from
official and scientific work, his vigorous mind and great love for
science urged him to further investigations, and in the plant-bearing
beds of Edinburgh, Falkirk, and Fife, he made important discoveries,
not only of new forms of plant-life, but of materials which increased
our knowledge of already described forms.

He died at 50, Haddington Place, Edinburgh, on February 28th,
in his 86th year. His son, Mr. B. N. Peach, F.R.S.E., F.G.8., has
for many years been attached to the Geological Survey of Scotland,
and is the author of several important geological and palzontological
memoirs.

1 Maclurea Peachii, which was named after Mr. Peach, and several other forms.

Decade Il. Vol. I. Pl V.

Geol Mag. 1886.

West,Newman & C® imp.

GM Woodward del.et lith.

Jurassic, Yorkshire.

2,Grass-hke leaf from the Purbeck, Swindon.

d

l,Supposed Monocotyledonous fruit

THE

GEOLOGICAL MAGAZINE.

NEW 7 SERIES.) DECADE. Tie V OE Iii:

No. V.—MAY, 1886.

(Gi viKeMbN (Asin? Js Svan OsiesayS)-

—_—_»—__

I.—On Mesozoic ANGIOSPERMS.
By J. Srarxre Garpner, F.L.S., F.G.S.
(PLATE V.)

HERE can scarcely at the present time be a problem more in-
teresting than that of the first appearance of Angiosperms, nor
one regarding which there is less trustworthy information at the
disposal of the geologist. In attempting to bring together a sum-
mary of what is known regarding the earlier forms of this most
important division of the vegetable kingdom, I make little claim to
originality ; nor are such criticisms as I may venture upon entitled
to the same weight as if put forward by a trained botanist.

It is quite unnecessary to recall the many supposed representatives
of Angiosperms that were formerly included in the Palzeozoic Floras,
for they have long since been dismissed from our lists of fossils and
forgotten. Though less fanciful in degree than some of the still
earlier geological fallacies, they are no less mythical, and at present
the names Yuccites, Palmacites, Antholites, Poacites, Culmites, etc.,
are no longer included among the plants of the Coal-measures. Now
that Pothocites has been shown to be part of a Sigillarian plant, there
is in fact no longer any Angiosperm remaining of Paleozoic age.
At the same time, it must not be overlooked that Corda described two
species of Carboniferous and Permian endogenous wood, while the
exhaustive studies of Prof. Williamson, extending over a great num-
ber of years, have brought to light the existence of some anomalous
woods and other plant-struetures from the Coal-measures, in the most
perfect preservation, so that it is certainly within the bounds of possi-
bility that we may some day come to a clearer appreciation as to the
lines through which Angiosperms were differentiated from the older
Cryptogams or Gymnosperms.

There are met with, however, in the Coal-measures, the exceed-
ingly problematical remains of a plant which is claimed in the
latest work of Saporta and Marion to be a “ pro-Angiosperm,” or, in
other words, an Angiosperm imperfectly differentiated from a Cryp-
togamic or Gymnospermic stock. The widely-distributed fossil,
known as Spirangium, consists of acutely-pointed spindle-shaped
bodies, which are believed to be composed of from five to ten linear
valves, supposed to envelope a central cavity. These valves usually
appear to be spirally twisted, but in some specimens, which seem to

DECADE Il1.— VOL. III.—NO. yY. 13

194 J. Starkie Gardner—Mesozoie Angiosperms.

be in more perfect preservation, there is no twist visible,’ so that
it is probable that either the spiral arrangement was confined to an
inner part of the structure, or that the purpose they had to serve
could be equally fulfilled without the twist. They seem to have
been seated on a pedicel, and according to Schimper, a number were
joined to form a sort of umbel; but in England at least they are
generally found detached. Examples were figured in the Trans-
actions of the Geological Society as long since as 1840,” under the
name of Carpolithes helicteroides. No better idea of their enigmati-
cal nature can be given than the bare enumeration of some of the
guesses that have been made as to their affinities. They were
thought to be allied to Helicteres, a genus of Sterculiacee, by Prest-
wich and Morris: they are Palgobromelia of Ettingshausen, allied
to the Pine-apple family ; the Palgouyris, of Brongniart, related to
Xyris,> a sedge-like Monocotyledon principally confined to the
Tropics; the radicular appendages of Hquisetwm according to Les-
quereux ; they were named Sporlederia by Stickler, who regarded
them as Bromeliads; and Spirangium by Schimper, who hazards
no opinion as to their position in the vegetable kingdom, beyond
such as is implied by placing them after the Monocotyledons. Finally,
they are claimed to be “ pro-Angiospermous” fruits by Saporta
and Marion, but it is almost superfluous to say that their affinities
remain to this day completely unknown. They are found in all
stages, from the Carboniferous up to and including the Wealden, and
any discovery tending to shed further light upon them would be of
very great importance.‘ |

Next in point of age comes a leaf with reticulated venation from
the Permian of Russia, and named Dichoneuron Hookeri, Sap. It is
stated to be of a firm consistence, with a long petiole, slightly dilated
at the base and detached naturally from the stem; and an engraving
shows it to be bipartite, indented, and lobed and cut laterally into
two segments. Saporta and Marion® claim that the venation re-
sembles that of Pistia (a tropical Duckweed), and that the leaves of
the aroideous Amormophyllum are similarly bilobed, and suggest the
association with it of a spathe-like body from the same formation.
Sir Joseph Hooker, however, to whom the specimen was shown,
thought that it was probably a cryptogam allied to Ceratopteris, a
genus of tropical and aquatic Ferns. It is in any case quite obvious
that very little importance can be attached to a mere leaf with such
undecided characters, when we reflect that leaves greatly resembling
each other with not dissimilar venation are common alike to Crypto-
gams, Gymnosperms, and both divisions of Angiosperms. Another

1 There is an admirable specimen showing this condition in the Museum at
Owens College.

2 Prestwich, Geology of Coalbrook Dale, Geol. Trans. vol. v. part iii. plate 38,
fig. 12, and explanation by Prof. Morris.

3 A view recently upheld by Nathorst.

4 The species described as Pale@ospathe by Unger from the Carboniferous and Per-
mian, may possibly also belong here. A list of them is given in Schimper, Pal.
végétale, vol. ii. p. 505.

° Evolution des Phanérogams, vol. i. p. 231.

J. Starkie Gardner—WMesozoic Angiosperms. 195

problematic plant, of which the outline at least is perfectly known,
is the Cithophyllum speciosum, Sch. and Moug., from the Trias of the
Vosges. It possessed linear leaves, with fine linear veins without
mid-rib, which are decurrent and grouped by threes on a woody and
branching stem. The branches are terminated by cylindrical and
more or less elongated spikes, whose scales or bracts bore smooth
shining seeds in their axils. These spikes were imperfectly articu-
lated at the base and furnished at that point by a ring of pales or
hairs, and were probably caducous.1 It has been suggested by
several writers that Cthophyllum may be allied to the Typhacee,
and though it is by no means even certain that they belong to the
Monocotyledons at all, it appears difficult to avoid regarding them
with interest as at least possible “ pro-angiospermic ” types. Certain
fruit-spikes from the same formation were named Eehinostachys by
Brongniart.

Synchronous with the last, and also common to the Jurassics, are
narrow ribbon-like leaves known as Yuccites, Sch. and Moug., five
species of which are described by Zigno.* They are broad or
narrow linear leaves, with entire margin, and without mid-rib, with
fine longitudinal veins united by transverse veinlets and sessile or
amplexicaul base. As stated by Schimper,* “It is useless to remark
that these fossils may proceed from very different types, and perhaps
without real analogy with the living type to which we compare
them.” They most resemble the leaves of Dracena or Fourcroya.

_ Inthe Rhetic we meet for the first time with the remarkable organism
known as Williamsonia, a fossil familiar to us from its not uncommon
occurrence in the Oolite of Yorkshire. It appears to have been
figured first as a flower‘ in Bird’s Yorkshire, pl. ii. fig. 6, associated
with Zamites, and later by Mantell in 1844, Medals of Creation,
vol. i. p. 161, as the fruit of Zamites lanceolata, in consequence of a
conjecture by Lindley that the supposed petals were scales and the
stamen and pistil the fractured axis. It was first described by Prof.
Williamson in a communication to the Linnean Society,’ in 1868, and
was named after the Professor by Carruthers; butat that time it was
considered that the Cycadean foliage associated with it, and known
as Zamites gigas, might very probably belong to the same plant.
The fructification is very rarely attached to stems with spirally arranged
leaves, and to such stems and the fruit the genus is now restricted.
It seems no longer possible to regard it as even an utterly abnormal
Cycad, and the question therefore arises as to whether Saporta and
Marion have sufficient grounds for ranking it among their “ pro-
Angiosperms.” Mr. Carruthers and Prof. Williamson appear uncer-
tain as to which section of the vegetable kingdom it should enrich,
while Dr. Nathorst advances the rather untenable proposal to place
it in Balanophoracee, a small natural order of succulent leaf-less,

Schimper and Mougeot, Monogr. d. pl. foss. du Grés bigarré, p. 39, pl. xix. xx.
Flora foss. forma. oolithice, i.-iv.

Pal. végétale, vol. ii. p. 427.

A closed bud is apparently figured as a nut, pl. iii. fig. 7.

Linn, Trans. p. 663, pls, 52 and 53.

af oO Ye

196 J. Starkie Gardner—Mesozoie Angiosperms.

parasitic Dicotyledons, to which Rafflesia belongs, while Newberry
appears to regard them as possible Composites.’

The branches of Williamsonia gigas, Carr., are stout, densely clothed,
with remarkably thick and short sheathing leaves, amplexicaul,
loosely imbricated, dorsally keeled or convex, inferiorly canaliculate,
and with lanceolate, stiff, and even spinous apex. They are coriaceous,
smooth, with entire margins and parallel veins, united by a delicate
network of oblique veinlets only visible with a lens. Many of
these stems are terminated by more or less developed globose
involucres, composed of at least one whorl of converging linear
bracts, bent inwards so as to form a chamber, which is sometimes
empty, showing the basal scar from which the interior organ had
become detached. The largest of these involucres are formed of
several rows of bracts enveloping a peculiar gourd-shaped body or
axis invested with a dense covering of compressed long narrow cells,
which Saporta regards as an investing mass of filaments and anthers,
such as that covering the spadix of Typha. Prof. Williamson calls
this a cortical layer, but has inferred that it possibly bore antheridial
organs: Saporta adds that these fell away after the pollen was shed,
. leaving the axis bare. Saporta asserts, and Williamson thinks it not
improbable, that this involucre represents the male organ of the
plant.

Associated with them are found verticils of incurved bracts united
at their bases into a cup-shaped organism, which Williamson on the
one hand is confident have never been found attached to any other,
but which Saporta maintains are sometimes present in the interior
moulds, in which condition all the English specimens are found,
adhering to the gourd-shaped axis which he says it surmounted.
The important collection of Mr. Yates is now in the Jardin des
Plantes, and I have not had the opportunity of examining it since I
became interested in the subject; but on the other hand Professor
Williamson certainly possesses a specimen in which each bract is
furnished with a pair of oblong depressions, which are clearly not
accidental markings as Saporta would believe, and are obviously
adapted for bearing a pair of ovules. The remarkable thing is that
none of the other numerous specimens, so far as I know, in our
public museums show any such marks. Moreover, the gourd-shaped
axis is sometimes prolonged into a peculiar point which can be most
readily described as in shape like a light-house, and which finds no
place in Saporta’s restoration.’

The rest of the description of Williamsonia is taken wholly from

1 Dr. Newberry describes a number of helianthoid flowers which he calls Palean-
thus, from the Cretaceous Amboy Clays, which are three to four inches in diameter
and greatly resemble Williamsonia. He remarks that though ‘‘so much like flowers
of Composit, we are not yet warranted in asserting that such is their character,” Bull.
Torrey Botanical Club, vol. xiii. p. 37, 1886.

2 The cup is described by Saporta and Marion, Evolution des Phanérog. vol. i.
p- 240, as a large cup or bell-shaped expansion with fringed or lobed margin, com-
posed of coriaceous and fibrous tissue, comparable to the spongy apex of the fleshy
spadix of Amoiphophaillus, and more remotely with the tutt of leaves crowning the
Pine-apple.

J. Starkie Gardner—-Mesozoie Angiosperms. 197

Saporta and Marion,’ as the specimens preserved in museums in this
country do not appear to reveal the characters claimed by these
distinguished French authors. They say that in addition to the
male involucres are others, smaller, less regularly globose, generally
empty, with a broad cicatrix at the base, corresponding to the in-
sertion of an organ which has evidently become detached in a
natural manner. Complete specimens, however, show a globular
receptacle or spadix, shrunk as if empty and surrounded by the
bracts forming the involucre. Sometimes this involucre appears to
have been detached entire, but more often the globular spadix with
the inner row only of bracts was disarticulated. The surface of
the spadix itself is areolate, the compartments irregularly polygonal,
either grouped in rosettes of five or six round central points, which
appear to be stigma of ripe pistils, or with these latter more irregu-
larly interspersed among them. The areolee are presumably barren
carpels. An Indian specimen shows the female spadix to have
possessed a fibrous covering which was shed in a single piece. A

A C

A, Fruiting organ of Williamsonia Morieri, Sap., naturally shed. The specimen is
preserved as carbonate of iron. Some of the bracts of the involucre remain, and
beneath the areol an accident has exposed some of the ripe seeds in their natural
position. The specimen, magnified twice, is from the Oxfordian of Vaches-
Noires. B. Areole formed of carpels grouped together and compressed, the
central points being the scars of the stigmas. C. A seed greatly magnified.
After Saporta and Marion,

1 Saporta has an exhaustive treatise on the subject in the press, which will be
superbly illustrated, in which he intends to demonstrate the absolute identity of
Williamsonia with Podocarya.

198 J. Starkie Gardner—Mesosoic Angiosperms..

very perfect specimen of Williamsonia Morieri, beautifully preserved
in carbonate of lime, is from the Oxfordian of Calvados. In this
species only the upper half of the spadix, which is ovate instead of
globose, is covered with areolz, in consequence of the fibres of
which the areolate covering is formed being directed upwards,
obliquely, instead of at right angles to the axis. This disposition
has fortunately enabled some of the ovules to be uncovered, and
shows that they are situated in the interior of the rosettes in which
the areole are arranged, each one corresponding to an entire rosette.
Thus most of the pistils were unfertilized, supposing there were as
many pistils as areole, and several of them became subsequently
united into synearps. Each areola when magnified is polygonal
and convex, with the facets culminating in a small button, an
arrangement exactly similar to that of Pandanus fragrans. The,
ovules or seeds were attached by the base, which was rounded,,
while the other end was more pointed.

The spadix was not a true inflorescence, or spike composed of a
number of flowers on one axis, as in the true Spadiciflore, but a
branch with every leaf metamorphosed into carpels, and thus the
morphological equivalent of the gyncecium of the Magnolia. Conse-
quently it represents a single flower composed of an indefinite
number of unisexual elements, a structure of a. kind that might
a priort have been expected to occurinan early type of pro-Angiosperm.

Small buds, as well as the more mature organisms, are met with in
the Yorkshire Oolites. Other and distinct species have been met
with in the Oolites of India,’ France, and some of the Baltic pro-
vinces, in some of these cases apart from any associated Cycadean
remains.” An organism found by Griffiths in the Grey Chalk
between Dover and Folkestone, in which the coaly substance of the
plant is preserved, was forwarded by me to Saporta, who pronounced
it without hesitation to be a Williamsonia. It would be interesting
to have this determination confirmed, as it strengthens the evidence
already in existence, tending to show that no great change took
place in the Flora of the British area, from the Jurassic to the Cre-
taceous, inclusive.®

The oldest definite Monocotyledons however are the well-marked
Pandanaceous fruits from the Oolites, which therefore take rank as
the earliest known Angiosperms. One of the most distinct of these
was figured by Buckland in 18386 from the Inferior Oolite of Char-
mouth,* to which, at R. Brown’s suggestion, he gave the name

1 Feistmantel lays great stress on their occurrence in the rocks of the Rajmahal
group as supporting his view that they are of Jurassic age. There are two species”
besides the one considered identical with the Yorkshire W. gigas, Pal. Indica, Flora
of Kach, p. 73, 1876.

2 Williamson, On some Anomalous Oolitic and Paleozoic Forms of Vegetation,
Proc. Roy. Institution of Great Britain, Feb. 16, 1883.

3 Saporta writes to me under date April 2nd, 1886, regarding this fossil :—‘‘ Je
crois bien que c’est un véritable Williamsonia, mais écrasé et méconnaissable et je
n’ose pas le décrire dans |’état ow il est, ne sachant méme si ce ne serait pas quelque
type spécial.”’ It appears, however, that it is to be figured in a forthcoming work.

* Geol. and Min. vol. i. p. 504; vol. ii. p. 101. Unger, Gen. et Spec. Plant.
Foss, p. 327. '

J. Starkie Gardner—WMesozoic Angiosperms. 199

Podocarya. Carruthers redescribed it! as of “the size of a large
orange, and composed of an indefinite number of cells, each con-
taining, near the surface, a single longish seed, about the size of a
grain of rice. The cells were separated from the spadix by long
fibrous footstalks, and were surmounted by hexagonal tubercles, in
the centre of which could be seen the remains of a stigma.” The
resemblance of this fruit to that of Williamsonia when deprived of
its involucre should not be overlooked.” Another Pandanaceous
fruit from the Great Oolite of Kingsthorpe, near Northampton, is
named Kaidacarpum by Carruthers and is thus described (p. 155, op.
cit.) : >—

“The fruit consists of a thick spadix,—not so thick, however, in
proportion to the drupes as in Bryantia butyrophora, Webb. The
drupes leave the spadix at a right angle about one-third from the
apex, those above have an ascending and those below a descending
direction, increasing as it reaches the fruit-stalk, which is seen in the
fossil, and shown in the drawing. This arrangement is precisely
that of Sussea conoidea, Gaud. The drupes are rhomboidal at the
base, spreading out laterally towards the apex, where their form is
a broad compressed rhomb two or three times longer than it is broad.
The cell containing the seed is near the base of the fruit, leaving
only a short pedicle or being really sessile, as in the recent species
with single-seeded drupes. Hach drupe contains a single seed ; and
although the whole structure is replaced by calcite, yet the details
are so beautifully shown that the connection of the seed by an
internal unilateral placenta adnate to the whole length of the cell is
in many cases obvious. The seed is ovoid and compressed and
the cicatrix at its base, by which it was attached to the placenta,
can be detected.” A comparison of the fossil with Sussea conoidea,
Gaud., places it beyond doubt, in the author’s opinion, “that it is
a true Pandanaceous fruit.” Another less perfectly preserved
species is in the Woodwardian Museum from the Potton Sands of
Cambridgeshire, and figured by Lindley and Hutton, but it is
certainly a derived fossil, and of Jurassic age. Another is recorded
from the Upper Greensand of Wiltshire. It was originally figured

1 Guot. Maa. Vol. V. April, 1868, Pl. IX. pp. 153-156.

2 See note ante. I was not in the least aware of Saporta’s conclusion when this was
written.

3 The mode of preservation is important, and is stated to be as follows :—‘“ The
matrix in which it is preserved is an amorphous cream-coloured limestone, which has
abounded in Molluscan remains, but the shells have been removed, and the spaces
they occupied, as well as the other larger cavities in the rock, are lined with or
entirely filled up by crystallized calcite. The fruit also is only a cast, in the same
material, of the cavity which originally contained it. The fine white mud had
insinuated itself into every crack and opening of the fruit, and filled the decayed
interior of the upper portion of the drupes. The walls of the seed cavity and the
seeds themselves, as well as the outer membrane of the drupes, resisted decay until
the matrix was somewhat compacted. These hard portions at length decayed, but the
insoluble carbon remained as a black amorphous substance, giving an external coloured
coating to the crystallized carbonate of lime, which in the end filled the cavity, pre-
serving in the most perfect manner the form of the fruit, and even some of the minute
details as to the relation of the different parts.” Guzou. Mag. lc.

200 J. Starkie Gardner—Mesozoic Angiosperms.

by Lindley and Hutton as Sérobilites Bucklandi, in their Fossil
Flora, vol. ii. pl. 129, published in 1833-35, from a drawing by
Miss E. Benett, made for Dr. Buckland, without the least clue as
to age or locality in the descriptive letterpress. In Miss Benett’s
*« Catalogue of the Organic Remains of Wiltshire,” published in 1831,
the only fossil referred to, which could possibly be the Strobilites in
question, is a Cycadeoidea ? from the Portland Beds, under the head-
ing “ Woods,” p. 9. In the first edition of Morris’s Catalogue, 1843,
it is put down as from “Gr. §. Wilts,” which cannot mean either
Lower or Upper Greensand, the abbreviations for which are “ L. G.
8.,” and “U.G.S.” but which looks like a misprint for “ Gr. O.,” the
sign for Great Oolite. In the second edition Morris, 1854, it
appears as from “U. G. 8. Wiltshire.” The question is whether in
correcting the printer's error of the first edition, due care to ascertain
the facts de novo was used. The circumstances are such as to leave
the age of the fossil in considerable doubt.

Part of a similar fruit is also described by Heer from the Cre-
taceous of Patoot in Greenland.

A not dissimilar but still smaller fruit has been found in the Coral-
line Oolite and the Kimmeridge Clay in France. These, named
Goniolina, are small ovoid, aggregated fruits, like those of Pandanus,
borne on a naked, cylindrical and relatively slender petiole. The
heads of the very numerous fruits are arranged in spirals and regular,
closely pressed together and barely a millimétre across. They are
of hexagonal shape, and six keels extend from the angles and meet
in a raised point in the centre. The interior axis is cylindrical, and
impressed with scars made by the bases of the fruits, completing its
likeness to Pandanus.

ro

Se

aya

8

UoGy, © Gee
©

Goniolina. Fruiting organ. From the Jurassic, in the Paris Museum, After Saporta
and Marion.

The Aroides Stutterdi, from the Great Oolite,! must, it appears on
the other hand, be expunged from the list of fossil plants, for Dr.
Woodward has well-nigh conclusive evidence proving that this
calcareous organism is part of an Echinoderm, Apiocrinus (Milleri-
crinus) Prattii. Poteriocrinus and Platycrinus are furnished with

1 See paper by W. Carruthers, F.R.S., Grou. Mac. 1867, Vol. IV.

J. Starkie Gardner—WMesozoic Angiosperms. 201

singular prolongations emerging from the calyx, known as the
“proboscis” (really the efferent orifice), which exactly resemble
externally the spadices of large Aroideous flowers.' Though the
calyx and “proboscis ” have not been found united in this particular
species, the fact that the supposed spadix is calcareous, and is far
from uncommon in a purely marine formation, renders it in the
highest degree improbable that it could be any portion of the flower
of an Aroid such as Xanthosoma. These singular crinoid probosces
were however not known when the determination was made. It is
a remarkable fact, that up to the present, there are no fossil representa-
tives of the Aroidee described, save a single fragment from the
Tertiary of Eriz, in Switzerland, named Aronites dubius by Heer, a
determination thought by Schimper to be doubtful. Our Eocene
Flora, however, contains several important representatives of the
group.

Several quite distinct types of Monocotyledons have been recorded
from the Lias, the principal of these being Bambusium liasinum,
Heer,’ a leaf very similar to those mentioned as Yuccites without
mid-rib and with two to four fine veins alternating with every more
decided one. Stems supposed to have been solid and cylindrical
and jointed are said to have been found associated with the leaves.
Some other fragments described as Cyperites protogeus, Heer, sup-
posed to be a species of Cyperacee, and Zosterites tenuistriatus,
Heer, possess no characters whatever on which any opinion should
have been expressed, and must certainly be expunged. The stems
of Endogenites erosa, so common in the Wealden and Neocomian, are
now known to be Cycadeous, and it is probable that the Dracena-like
stems from Tilgate Forest and elsewhere, so often referred to by
Mantell, are referable to the same group. There are also many
Jurassic-Cretaceous fruits which may quite conceivably prove to be
angiospermous, and which deserve careful study.

The remarkably fine stem I have figured is in the possession of
Prof. Williamson, who states that it is the Calamites Beanii of
Bunbury.’ Sir Charles, however, remarks on the tumid articula-
tions, “the stem being much thicker in those parts than in the
intermediate spaces,” so that he must have had specimens of
Equisetum columnare, which occur abundantly in the same beds,
in his mind. In speaking of it Prof. Williamson observes that
“so far as external appearances are concerned, it more closely
resembles the stem of one of the arborescent Graminee. But
such appearances have very little Taxonomic value. Nevertheless,
the plant stands out in prominent distinctness from amongst the
Ferns, Cycads, and Conifers that grew around it, forcibly suggesting
the idea of an arborescent Monocotyledon ; and if such has been
its character, its position amongst these older Oolites would make

1 Although this conclusion seems highly probable, it must be borne in mind that a¢
present we know of no Secondary stalked crinoid with a ‘“‘proboscis’’ like Potertocrinis
or Platycrinus. All the forms with this appendage being of Paleozoic age.—H. W.

* Heer, Flora Helvetie, p. 138, pl. 55.

3 Quart. Journ. Geol. Soc. vol. vii. p. 189, C. giganteus, Bean MS.

202 J. Starkie Gardner—WHesozoic Angiosperms.

it, if not the earliest, one of the earliest representatives of the
Monocolytedonous group.”! The stem is somewhat compressed,
and the piece preserved is evidently from near the base, the three
joints of which it is composed diminishing rapidly, the first
measuring 2 inches, the second 13, the third 14 inches in height.
The diameter of the middle joint is about 5 inches, but its crushed
condition has no doubt considerably added to the width, which
was probably nearer 34 inches before compression. The exterior
has a smooth and silky look, with fine longitudinal veins. The
nodes are depressed, about +45 of an inch wide, and bordered by
slight collars or thickenings. The stem seems to have been
hollow, though it may perhaps have been solid like the sugar-
cane ; it has an altogether different texture to that of Calamites
or Hquisetum. There are unfortunately no other organs in these
beds which can be even tentatively united with it. ;

Supposed Monocotyledonous stem from the Jurassic of Yorkshire.

[Owing to the unfortunate loss of the wood engraving in transit
by rail, the figure of Prof. Williamson’s specimen had at the last
moment to be omitted, but will be inserted in the June Number.—
Eprr. Grou. Mac. |

The specimen figured, Plate V. Fig. 1, a and 6, isnow in the Wood-
wardian Museum, and is also stated to have come from the York-
shire Oolites. As in all fossil vegetables from these deposits, there is
no internal structure preserved, and we are therefore only able to
deal with the exterior. This appears to represent on one side a ropy
ligneous stem, slightly twisted, and with a half-lunar section. On
the other side is a thick, closely adherent spathe, rather smoother
than the stem, but furrowed, very thick and leathery, acutely pointed
at the top, and narrowed and amplexicaul at the base. The spathe
or pod is 9 inches long, 2 broad, and 13 inches deep in its greatest
diameter. There is a slight swelling near the base, with two or three
projections, as if there were ovules under the spathe, then a contrac-
tion, and then the main swelling with apparent traces of more ovules
under it, especially towards the apex. The seeds or fruits would
appear to be oval and about half an inch in length. At the base,
where the spathe joins the stem, its substance is seen to be ysth of
an inch in thickness, and it is an inch across; the stem itself being
1+ inches wide, rather compressed and squarish. It increases upward.
with the spathe, becoming more crescentic in section, and again
diminishes as the spathe commences to taper to a point. Though
the transverse section reveals no structure, it shows clearly the
demarcation between spathe and fruit and the stem.

It forcibly reminds us of some palm spathes and fruits, and if it
should prove to be'merely concretionary, it would certainly be a case
of most extraordinary mimicry. Such a view seems however, quite
out of the question, and we cannot help regarding it as a mono-

1 On some Anomalous Oolitic and Paleozoic Forms of Vegetation, Ruyal Instituion,
Feb. 16, 1883.

J. Starkie Gardner—WMesozoic Angiosperms. 203

cotyledonous fruit of some kind, and greatly regret that its precise
locality and horizon cannot be fixed with greater precision.

The supposed Najadita, on the other hand, is quite certainly no
Angiosperm, but a Cryptogam.

These remains, which must obviously have belonged to a fresh-
water plant, occur in some profusion in the fissile limestone at the
base of the Lias or top of the Rhetics in the neighbourhood of
Bristol.!. The precise beds are called by the Rev. Mr. Brodie
“ Hstheria beds,” from the quantity of Estheria Brodieana, var. (T. R.
Jones), which they contain, while the valves of a species of Cyclas
are also very abundant with them.” The plant remains were deter-
mined by Prof. Buckman to belong to the Monocotyledons, and
named by him Wajadita on account of the relationship which he
believed they bore to the family of Najas or Pond-weeds, and were
described and figured in the Quarterly Journal of the Geological
Society, 1850, vol. vi. p. 415. The supposed early appearance of
this group of Monocotyledons has excited considerable interest, and
has frequently been quoted and referred to in works on paleontology
and botany. Wishing to re-examine them, I communicated with the
Rev. P. B. Brodie, in whose cabinet many of the original specimens
are preserved, with the result that a number of them were placed
at my disposal.

My first examination convinced me that far from being Monocoty-
ledons, they were cellular Cryptogams of some kind, the supposed
rectangular venation being nothing more than the cell walls of the
tissue forming the leaf-blades. I next took them to Manchester,
where Prof. Williamson kindly looked at them, and without a
moment’s hesitation pronounced them to be the remains of cellular
plants. Since then Mr. Carruthers has examined them, when Mr.
Ridley, who has charge of the Monocotyledons, and Mr. Murray, in
whose care the Cryptogamic section of the British Museum Herba-
rium is placed, were also invited to express their opinions, the result
being that all these botanists agreed in regarding them as Crypto-
gams resembling ontinalis in habit. They in fact bear the strongest
possible resemblance to these fresh-water mosses, and without wish-
ing to place them definitely in the genus Fontinalis, it does appear
to me to be useless to seek further among existing plants for their
affinities. This group of fresh-water mosses has not previously
been included in any fossil flora, and it would indicate a temperate
climate, thus corroborating the evidence of the insects associated
with it, and that the water was limpid, with a feeble current. I am
most pleased to be able to state that Mr. Brodie quite concurs in the
transfer of his specimens to the aquatic mosses.*

The Lilia, Bensonia, and other supposed Monocotyledons and

1 Q.J.G.S. vol. vi. p. 415, 1850.

2 Mr. Brodie informs me that he regards them as a junction bed between the two
formations.

® Mr. Brodie has since sent me a capsule from these beds, which appears to belong
to the same moss. .

204 J. Starkie Gardner—Mesozoic Angiosperms.

Dicotyledons of Buckman’ seem to be either Cycadaceous or too
indistinct to be determinable, and no importance whatever can be
attached to their supposed Angiospermous affinities.

Among many specimens lent me by Mr. Brodie, however, is one
undoubtedly Monocotyledonous fragment from the Purbeck of
Swindon (Plate V. Fig. 2), three millimétres wide, with nine
parallel equal longitudinal veins. It has a rush or grass-like
appearance, but may possibly belong to an aquatic plant.

The records of some of the supposed early Angiosperms may have
escaped me, but some have purposely not been included in this
notice, because they are not deserving of mention.

No new types come in during the Lower Cretaceous, and our
knowledge of the Angiosperms of this period remains in a most
imperfect state. There are still jointed stems and _ occasional
fragments of sword-like leaves, and the important Dracena-like
Kolirion, of Schenk. I have found rolled pellets of palm-like wood
in the Gault at Folkestone, and, as already stated, an organism in
the Grey Chalk which Saporta pronounced to be a Williamsonia.
The most remarkable thing is that not the smallest trace of an
Angiosperm has been found in the Wealden deposits, though these
appear to have been pre-eminently likely to have preserved such,
had they existed. A host of Dicotyledons as well as many of the
principal families of Monocotyledons, come in with the Upper
Cretaceous, but the relative ages of the beds in which they occur
are by no means satisfactorily determined. and, as Floras, they are
rather to be grouped with those of the Tertiaries than those of the
Wealden, Neocomian and Gault.

The mystery in which the early development of Angiosperms is
still shrouded is the more inexplicable, since the presence of a flower-
sucking moth in the Solenhofen beds is a well-ascertained fact.
From a remark made by Prof. Marsh, at Aberdeen, there is some
hope that welcome revelations regarding American Jurassic Angio-
sperms may reach us ere long. In the meantime I refrain from
encumbering this communication with any of the obvious speculations
that have oceurred to me, and probably to others, as possible
explanations of their extreme rarity in pra-Cretaceous deposits.
The evidence tends to show that Monocotyledons (?) of some sort
existed as far back as the Trias, possessing leaves of the most primi-
tive type, such as we now meet with in Yucca, Dracena, etc., and
that during the Jurassics decided Monocotyledons, which can be
placed in the Pandanacee, and others with jointed stems like
Graminea, flourished side by side with more problematical plants
such as Williamsonia. Little more than this can yet be said, though
Saporta and Marion bring forward an array of arguments and
inferences wherewith to build up a family tree,” which if not quite
carrying conviction, are certainly highly suggestive, and deserve the
most careful consideration.

1 Murchison and Buckman, Outline of the Geology of Cheltenham, 1845.
* Evolution des Phanérogames, Saporta and Marion.

A. Smith Woodward—On the Genus Notidanus. 205

IIT.—On toe Panmontronocy oF THE SELACHIAN GENUS JVOTIDANUS,
CUVIER.
By A. Smrrx Woopwarp, F.G.S.,
of the British Museum (Natural History).
(PLATE VI.)

MONG the Selachians of the existing fauna, there are none of
greater interest and higher morphological importance than
Notidanus, Cestracion, and the recently-discovered Chlamydoselachus
from Japanese seas. These are the solitary survivors of once
flourishing types, whose immediate congeners are only known to
Biological science through the fragmentary remains preserved in the
geological record ; and the value of the archaic features they present
is even further enhanced by the slight information already acquired
regarding the geological distribution of their numerous extinct allies.
Hitherto, however, there appears to have been no attempt at a
systematic treatment of the Paleontology of the first of these genera,
although the Cestraciont and Cladodont types have received a large
share of attention. I therefore propose to offer a short account of
the present state of knowledge of this subject—summarizing the
results of previous research, making known a few interesting fossils
that have not yet been described, and adding some general remarks
on the extinct congeners of the Notidanide, so far as they can be
determined from the evidence of detached teeth.

Briefly reviewing the main anatomical features of the living Noti-
danus, in the first place, there are several peculiarities especially
worthy of note. The skull is remarkable from its close approach to
the amphistylic type of Professor Huxley.! Unlike all other living
Selachians, the upper element of the hyoid arch is extremely slender
and takes no part in the support of the pterygo-quadrate and man-
dibular cartilages; but this is compensated for by a distinct facette
upon the otic process which articulates with the post-orbital process
of the chondrocranium.? The mandibular and hyoid arches thus
most nearly retain their primitive condition, and there is also only
a very slight advance upon this stage in Cestracion:* in this genus,
the pterygo-quadrate articulates with the pre-orbital region of the
chondrocranium, and the “hyomandibular” is only just becoming
worthy of that name. These characters are so important, when
taken in conjunction with others exhibited by the same types, that
in dividing the Selachii into four great suborders, Prof. Theodore

1 T. H. Huxley, ‘‘ On Ceratodus Forsteri, with Observations on the Classification
of Fishes,’’ Proc. Zool. Soc. 1876, pp. 40-45.

2 See excellent figures by C. Gegenbaur, ‘‘ Das Kopfskelet der Selachier’’ (1872),

plate x.
*3 T. H. Huxley, loc. cit. p. 42, fig. 8.

206 A. Smith Woodward—On the Genus Notidanis.

Gill’ regards the Notidanide and the Cestraciontide as the sole
existing representatives of the first two.

Notidanus is also remarkable for the persistence of the notochord.
One section of the genus (Hexanchus) exhibits this gelatinous rod
merely subdivided by transverse membranous septa, while the other
(Heptanchus) has annular cartilages in the sheath which only show
traces of calcification in the region of the tail.”

As regards fins, the genus under consideration differs from other
Sharks (except Chlamydoselachus) in possessing only a single dorsal,
without spine, which is placed far back, partly opposite the anal.
The latter is well marked off from the caudal. The structure of
these locomotory appendages in Notidanus is also interesting, but
there is much difference of opinion as to the conclusions to be drawn
from them. Prof. Huxley has given reasons* for regarding the
pectorals as of a more primitive type than those of other living
Selachians and as most nearly related to the so-called ‘“ archiptery-
gium” of Ceratodus; while Prof. Mivart* is led to dissent entirely
from this interpretation, and to look upon it as nothing more than
“an ingenious speculation.” The latter has also shown (loc. cit.)
how the basal cartilages of the dorsal and ventral fins, and, to a less
extent, those of the anal, have become fused together into a nearly
continuous mass,—a fact of considerable significance if, as seems
probable, the basals were a parallel series of thin cartilaginous bars
in-the earliest forms of fin.

Another curious feature of Notidanus consists in its possession
of more than five gill-openings besides the spiracle, and in this
peculiarity it differs from all other living Sharks except the Chlamy-
doselachus. Some of the species have six of these openings and
others seven ; and most ichthyologists prefer to regard each of these
types as constituting a distinct genus, the first named being termed
Heaanchus, and the second Heptanchus or Heptranchias. Dr. Gin-
ther,® however, is inclined to admit no such separation, and as it is
quite impossible for palzontological purposes, it cannot be adopted
here.

But the points to which the paleontologist is naturally led to
devote most minute attention are those relating to the harder struc-
tures capable of preservation in the fossil state. And it fortunately

1 In Jordan and Gilbert’s ‘‘ Synopsis of the Fishes of North America,’’ Bull. U.
§. National Museum, No. 16 (1888), p. 967.

2 See detailed descriptions of C. Hasse, ‘‘ Das Nattrliche System der Elasmo-
branchier—Besonderer ‘Theil’? (1882), pp. 39-82, pls. vi. vil.

3 Loc. cit. p. 50.
_ 4 St. G. Mivart, ‘“‘ Notes on the Fins of ieee Trans. Zool. Soc.
vol. x. (1879), p. 471.

5 A, Ginther, ‘‘ Catalogue of Fishes Brit, Mus,”’ vol. viii. (1870), pp. 397-399.

A. Smith Woodward—On the Genus Notidanus. 207

happens that in the living Notidanide there are very decided dif-
ferences in the teeth of the various species. It is also true, on the
other hand, that the dentition of each individual exhibits a certain
variability in its components according to their situation in the jaw ;
but a careful comparison of actual specimens, descriptions, and
figures, appears to reveal a few characters that are practically con-
stant, and suggests the possibility of at least determining detached
side teeth.

In a typical species like WV. indicus the upper teeth on and near
to the junction of the pterygo-quadrate cartilages have some
resemblance to very thick, depressed teeth of Lamna, without
lateral denticles, but placed upon a fibrous base undivided into
radicles. The side teeth exhibit one or two distinct denticles or
denticulations in front of the principal cone, and an increasing num-
ber of small cones behind this, the latter being larger in proportion
to the main cone the more remote is the tooth from the front of the
jaw. The mandible exhibits a single symphysial tooth, with three
or four laterally directed toothlets on each side, but no median cone;
and then follow six nearly similar comb-shaped teeth, both to the
right and the left. In these, the principal cone is serrated anteriorly,
and the hindermost tooth—as in the upper jaw—shows the principal
cone least predominant. At the back of both jaws, there are also
minute teeth—diminutive knife-edges of enamel, each upon the
characteristic form of base.

Besides the widely distributed species whose dentition has just
been described, Dr. Giinther recognizes three others in his British
Museum Cat. Fishes, and about three more have subsequently been
determined in America.! Ichthyologists thus distinguish about
seven living forms of Notidanus, and on referring to their published
diagnoses, it appears that at least three features in their dentition
are specially looked upon as of specific value. These are (i.) the
presence or absence of a median tooth, and the presence or absence
of a median cone in such a lower tooth ; (ii.) the relative prominence
of the principal cone in the mandibular side teeth—whether incon-
spicuous, proportionately stout, or notably elongated ; and (iii.) the
character of the denticulations in front of the principal cone of the
lower teeth. It is obvious that, of these distinctive features, only

the two latter are available to the paleontologist, except on rare
occasions ; but it is satisfactory to find that the upper teeth apparently
exhibit the same specific modifications as the lower—e.g. a stout or
long cone in the one corresponding to a stout or long cone in the

1 Jordan and Gilbert, ‘‘ Fishes of N. America,” Joe. cit., p. 62: and 8. Garman,
Bull. Essex Institute, vol. xvi. (1884), pp. 56, 57,

208 A. Smith Woodward—On the Genus Notidanus.

other—and it is thus possible to restore the dentition of some of the
extinct types with a considerable approach to accuracy.

Of fossil Notidanidz, no undoubted traces have hitherto been
recorded from beds beneath the Middle Oolite. Miinster,' it is true,
mentions a small tooth from the Lias as belonging to Notidanus, but
no figure is given, and there is not sufficient proof of the accuracy
of the determination. Oppel? also makes known another tooth from
the Upper Lias of Swabia, which he ventures to name specifically
N. Amalthei, though evidently recognizing the slenderness of the
grounds for this procedure; his figure shows nothing beyond a
laterally-compressed cone, and neither this nor the description
suffices to distinguish it from the tooth of a large Oxygnathus. It is
further interesting to note that Tate and Blake* have recorded
Oppel’s species from the Middle Lias of Whitby, and this determi-
nation is equally unreliable: the original fossil is said to be pre-
served in the Whitby Museum, but Mr. Martin Simpson has failed to
discover it during a search he has kindly undertaken in response
to my inquiries, and I am also indebted to Professor Blake for a
reference to his note-books, which likewise afford no definite par-
ticulars.

The Oxfordian N. contrarius and N. Miinsteri are thus the earliest
species of the genus at present described, and with these we com-
mence an enumeration of the different specific types that appear to
be distinguishable upon the evidence of detached teeth.

1. N. conrrarius, Minster.
1843, NV. contrarius, Graf yon Minster, ‘‘ Beitr. zur Petrefaktenkunde,”’ pt. vi.
p. 54, pl. ii. fig. 3

Founded upon a broken tooth from the Lower Oxfordian‘ of
Rabenstein, Bavaria. The fossil exhibits two small diverging cones,
with a denticle behind, but is much too fragmentary for specific
determination, and does not appear to have been recorded since
Miinster’s original description.

2. N. Monsrert, Agassiz.

1843. WN. Miinsteri, L. Agassiz, ‘‘ Rech. Poiss, Foss.”’ vol. iii, p. 222, pl. 27,
figs. 2, 3.

A species founded by Agassiz upon some detached teeth from the
Oxfordian (Weiss Jura y, Quenstedt) of Streitberg, Franconia, and
of Randen, Schaffhausen, Switzerland. The type specimen figured
exhibits a principal cone destitute of anterior serrations and relatively
large both in breadth and height; this is followed by three well-
marked secondary cones, closely approximated, and rapidly decreasing
in size, and the crown terminates in a small denticulation.

1 Minster, ‘‘ Beitrage zur Petrefaktenkunde,”’ pt. vi. (1843), p.

2 IN Oppel, ‘‘Der mittlere Lias Schwabens,” Wiirttb. J aan a x. (1854),
p. 62, pl. 1. fig. 1.

3 Tate and ‘Blake, “ The Yorkshire Lias’”’ (1876), p. 256.

4 This and the other Jurassic horizons have been ieaaly supplied by Mr, Etheridge.

Pp

Geol. Mag.1886. Decade II]. Vol. I. Pl. VI.

G.M Woodward del. etlith. West, Newman & C° imp.

’ Fossil Notidanidee.

pe atts
Ye j r pee

4 vv
Orie”! s San

A. Smith Woodward—On the Genus Notidanus. 209°

There seems to be no undoubted reference to teeth of this type
since Agassiz’ original description, though the name is mentioned
in several lists of Continental Jurassic fossils. The specimens from
Schnaitheim figured by Quenstedt as N. Miinstert are almost cer-
tainly referable to a distinct form next to be considered.

3. N. exruius, Wagner. Pl. VI. Figs. 3—5.
1849. WN. Miinsteri, Beyrich and Frischmann, Zeitschr. Deutsch. Geol. Gesell. vol. i.

p. 436, pl. vi.
UGS a a F. A. Quenstedt, ‘“‘ Handb. Petr.’’ p. 167, pl. 13, fig. 4.
Hehe) 35 i F. A. Quenstedt, ‘‘ Der Jura,”’ p. 662, pl 96, figs. 33, 34.

1861. NV. eximius, A. Wagner, Abh. k. bayer. Akad. d. Wiss. cl. ix. vol. ix. pp.
292-296, pl. iv. fig. 2.

The Lithographic Stone (Lower Kimmeridgian) of Bavaria is the
only deposit that has hitherto yielded remains of Notidanus other
than detached teeth. But from this fine-grained rock at least three
comparatively perfect fishes have been described, in addition to one
other fragment of the caudal extremity. Of these, the finest speci-
men was figured by Beyrich and Frischmann, loc. cit., in 1849, and
the subsequent studies of Dr. Andreas Wagner resulted in its being
separated from all other known species under the name of N. eaximius.

The important fossil just referred to was obtained from the
quarries of Hichstidt, and is complete with the exception of the tip
of the tail: it indicates an original length of about nine feet, and
exhibits a very definite outline, owing to the presence of plentifully
scattered shagreen granules in the skin. The head is rounded and
obtuse in front, and a considerable number of teeth are exhibited in
the region of the mouth. The pectoral fins are evidently larger than
the ventrals, and the anal is small compared with the dorsal; the
latter is almost entirely in advance of the anal, although appearances
may be deceptive owing to pressure during fossilization. But the
most remarkable character displayed in this specimen is the presence
of well-marked annular cartilages in the sheath of the notochord.
These have been carefully studied by Dr. Hasse,' of Breslau, who
has shown that they agree in microscopical structure with those of
the living Heptanchus ; and this Kimmeridgian form is thus the only
fossil species hitherto discovered that it has been possible to refer to
the correct subgenus. The vertebral rings in the caudal region are
further apart than in the more anterior portions of the body.

The two other specimens of WVotidanus from the Lithographic Stone
are of small size, not exceeding 44 inches in length, and are regarded
by Wagner as probably the young of the species under consideration.
No figures have been published, but a plaster cast of one of these
immature fishes is exhibited in the British Museum.

A group of the teeth of N. eximius are figured by Beyrich and
Frischmann, and Wagner also represents a solitary example. The
drawings of the Hichstidt fossil, however, do not appear to illustrate
the variation of the dentition in different parts of the mouth, nor do
the authors offer any particular observations upon this point. In

1 C. Hasse, “ Natiirl. Syst. Elasm.—Besond. Theil,” pp. 51, 52, pl. vii. figs. 23-25,
DECADE I1I.—VOL. III.—NoO. v. 14

210 A. Smith Woodward—On the Genus Notidanus.

the ordinary lateral teeth, the principal cone is destitute of serrations
on its anterior border, and is followed by three (or sometimes four)
much smaller cones. These teeth chiefly differ from JV. Mimsteri
in the wider interspaces between the successive cones. They are
also. somewhat larger, and the apex of each cone occasionally ex-
hibits a slightly hooked appearance.

Other teeth of the type just described are met with in the Upper
Corallian beds of Schnaitheim, Wiirtemberg, and were originally
figured by Quenstedt (loc. cit.) under the name of N. Miinsteri.
Wagner makes a brief allusion to these at the end of his description
of N. eximius, and hints that they may possibly belong to his newly
determined species. The National Collection contains a good series
of specimens from the same deposit, which appear to leave no doubt
of the correctness of this identification, and three of these form the
subjects of Figs. 8-5. The teeth exhibit considerable variation in
size—from one to two centimetres in length—and this may be due
not only to age, but also to differences corresponding to the various
parts of the jaw. All, however, are characterized by wider inter-
spaces between the cones than is the case in N. Miinsteri. In teeth
that are probably from the front region of the mandible (Figs. 3, 4),
the principal cone is relatively longer and less oblique than in those
further back; while in anterior teeth of the upper jaw, the principal
cone is still more prominent and placed erect upon the base. Fig. 5
represents one of the latter type, and the original of fig. 34, pl. 96,
in Quenstedt’s ‘‘ Jura,” is probably another from nearly the same
situation. Of lower teeth, the other illustrations of Quenstedt are
evidently characteristic examples, and Fig. 3 is a drawing of the
largest tooth in the British Museum Collection ; this specimen—like
two others, Nos. 22489 and pv. 4708—is remarkable on account of the
oblique abrasion of the apex of the principal cone, which appears to
have been produced during the life of the animal. The same figure
also shows a slight crimping at the lower part of the anterior edge
of the tooth; and fig. 33, pl. 96, of Quenstedt’s “Jura,” lkewise
exhibits this feature upon a greater extent of the border, but there is
no definite denticulation. |

It is interesting to add that Wagner further records a single tooth
of N. eximius from Daiting, and another from the Lithographic Stone
of Nusplingen, Swabia.

The upper tooth shown in Fig. 6 was also obtained from the
Schnaitheim beds, but it appears scarcely referable to LV. eximius,
and must remain at present specifically undetermined.

4, N. Waeyert, Agassiz, sp.

1848. Aellopos Wagneri, L. Agassiz, Rech. Poiss. Foss.” vol. iii. p. 233.
1861. Notidanus Wagneri, A. Wagner, Abh, k. bayer. Akad. d. Wiss. cl. ix.
vol. ix. pp. 296-299.

In the volume of the “Neues Jahrbuch” for 1886, p. 581, Count
Miinster briefly recorded a Selachian fossil from the Kelheim Litho-
graphic Stone under the name of Aellopos elongatus. It exhibited
nothing more than the hinder region of the body, and its affinities

A. Smith Woodward—On the Genus Notidanus. 211

were thus somewhat problematical, but the distinguished paleon-
tologist just mentioned felt justified in regarding it as the type not
only of a new species, but also of a new genus. Some years later,
when preparing his classical work on Fossil Fishes, Agassiz con-
firmed Miinster’s original determination, and founded a second species
of Aellopos—termed A. Wagneri—upon another specimen preserved
in the Munich Museum. This likewise exhibited only the hinder
region of the body, but the great relative size of what was then
considered to be the second dorsal fin, and the distinctly calcified
vertebral rings, were quite sufficient to separate it from all fossil
sharks at that time known. No figures were published, however,
and Agassiz’ short notice embodied all available information until
1861, when Dr. Andreas Wagner was engaged in investigating the
fish-fauna of the Solenhofen Stone, and succeeded in elucidating the
problematical fossil by a reference to the magnificent specimen of
Notidanus eximius, figured by Beyrich and Frischmann. His re-
searches led to the conclusion that Miinster’s A. elongatus was really
a Squatina (or an allied genus), and that Agassiz’ A. Wagneri might
be referred with equal certainty to the genus Notidanus. The con-
siderable dimensions of the supposed ‘“‘ second” dorsal fin were thus
no longer remarkable, and the comparatively advanced condition of
the vertebral column was recognized as quite similar to that of the
complete specimen just quoted. Some minor differences are sufficient
to distinguish N. Wagneri from N. eximius, and among others, may
be mentioned the relatively greater length of the dorsal fin: the
vertebre are also longer, and wide interspaces between them do not
begin to appear before the middle of the tail, whereas in N. eximius
this character is obvious quite at its commencement.

5. N. inrermepius, Wagner.
1861. WV. intermedius, A. Wagner, loc. cit. p. 299, pl. iv. fig. 3.

A species founded upona single tooth from the Lithographic Stone
of Miihlheim, near Solenhofen, and characterized by the large size of
the denticulations in front of the principal cone, which is thus placed
not far in advance of the middle of the tooth. Behind the principal
cone are five smaller ones.

As Wagner observes, this determination is merely provisional, for .
the dentition of N. Wagneri is at present wholly unknown, and the
form of tooth in question may eventually prove to belong to the
latter species.

6. N. Htceenra, Minster.

1843, WN. Hiigelig, Graf von Minster, “ Beitrage zur Petrefaktenkunde,’’ pt. vi.
p- 54, pl. i. fig. 5.

EERE a, - (?) F. A. Quenstedt, ‘‘ Handbuch der Petrefaktenkunde,”’ p.
167, pl. 13, figs. 5, 6.
1858. __,, 36 F, A. Quenstedt, ‘“‘ Der Jura,’’ p. 519.

This species was founded by Miinster upon a broken tooth from
the Corallian of Gammelshausen, near Boll, Wtrtemberg. The
specimen exhibited a large principal cone (without anterior serrations)
followed by two small cones of about one-third the size of the first.

21D A. Smith Woodward—On the Genus Notidanus.

The originals of the figures in Quenstedt’s ‘‘ Handbuch ” are very
much smaller than the type specimen, and are characterized by the
presence of anterior serrations ; it is doubtful, indeed, whether they
are truly referable to this form.

7. N. serratus, Fraas. Pl. VI. Fig. 7.

1855. NV. serratus, O. Fraas, Wirttemb. Jahresh. vol. ix. p. 98.
SoS se 7. F. A. Quenstedt, ‘‘ Der Jura,”’ p. 784, pl. 96, fig. 44.

This species was originally named by Fraas, but does not appear
to have been completely defined before the publication of Quenstedt’s
work on the Jura. The last-mentioned paleontologist records a
group of about 14 teeth, naturally associated, and figures one of the
most typical forms. This, as a Jurassic type, is remarkable on
account of the number of distinct cones that make up its crown,
and the prominence of the sharp denticulations on the front edge of
the principal cone; the latter is comparatively broad and long, and
is succeeded by seven minor cones, of which the anterior is very
much the largest. The species occurs in the Corallian of Nusplingen,
Swabia.

A detached specimen in the British Museum (No. 35667), obtained
by the late Mr. Bean from the Oxford Clay of Scarborough, agrees
so closely with the tooth of this species figured by Quenstedt that it
cannot be separated on present evidence. The fossil in question is
shown of the natural size in Fig. 7, and is in an almost complete
state of preservation. 'The principal cone of the crown is relatively
very large, and is succeeded by five secondary cones, while at its
base in front there occur three closely approximated denticles, the
first being of considerable size. Of the secondary cones, the most
anterior is directed sharply backwards and makes a wide angle with
the posterior edge of the principal cone; it is nearly a third larger
than that immediately following, and the remaining three are quite
small. The base-line of the crown is arched, and the lower border
of the root has a somewhat crimped appearance. This is evidently
a tooth of the upper jaw, and the respects in which it differs from
Quenstedt’s figure are precisely those in which the upper teeth of
living species differ from the lower.

8. N. Davisst, sp. nov. Pl. VI. Fig. 8.
1871. Hybodus polyprion, J. Phillips, ‘‘ Geology of Oxford,”’ p. 305, pl. xii. fig. 18.

The scarcity of remains of Notidanus in the Jurassic rocks of
Britain appears somewhat remarkable when it is remembered how
frequently they have been recorded on the Continent: and in addi-
tion to the Scarborough tooth already described, I have only succeeded
in meeting with two other specimens.' These were erroneously
referred. to Hybodus by Professor Phillips, op. cit., and they have
been kindly pointed out to me by Mr. William Davies, who recog-

1 Besides others already named, I have also to thank the following friends and
correspondents who have kindly assisted me in the search for Jurassic Notidanidie :—
Mr. K. T. Newton, of Jermyn Street; Mr. T. Roberts, of the Woodwardian
Museum, Cambridge; Mr. H. M. Platnauer, of the York Museum; Mr. H. J.
Moale, of the Dorset County Museum; and Mr, H. E. Quilter, of Leicester.

A. Smith Woodward—On the Genus Notidanus. 213

nized their true affinities some years ago when identifying fossil
vertebrata in the Oxford Museum; I am also indebted to the kind-
ness Of Professor Prestwich for the opportunity of studying and
publishing a further notice of the original teeth.

The specimens in question were obtained from the Oxford Clay of
St. Clement’s, near Oxford, and as they cannot be safely identified
with any form at present known, I propose to apply to the most
satisfactory tooth (Fig. 8) the provisional name of N. Daviesii: the
second fossil (Fig. 9) may possibly be a variety of the same species,
but this is at present uncertain. In the type specimen shown in
Fig. 8, the principal cone is relatively large, both in breadth and
height, and is destitute of serrations on its anterior border. ‘This is
followed by four rapidly diminishing secondary cones, and the crown
terminates in a minute denticulation. The apices and edges of all
the cones are remarkably sharp, and the base is short and thick com-
pared with that of the majority of later species. The second tooth
(Fig. 9) has a very peculiar form, and consists merely of two back-
wardly curved cusps, though other small ones may have been broken
away behind. The lower part of the anterior edge of the principal
cone is crimped, and the enamelled sides of the crown exhibit vertical
wrinkles suggestive of those of Hybodus.

N. Daviesii appears to approach N. Minsteri more closely than any
other, but it is easily distinguished from this species by the different
relative proportions of the principal and secondary cones.

9. N. mrcropon, Agassiz. Pl. VI. Figs. 10—15.

1822. Tooth of Squalus ? G. A. Mantell, “‘ Fossils of South Downs,” p. 227,
pl. xxxii. fig. 22.

1843. NV. microdon, L. ea es Bee Poiss. Foss.” vol. iii. p. 221, pl. 27, fig. 1,

. 86, figs. 1, 2.

1843? ,, a HR, Geinitz, “‘Schichten und Petrefakt. d. sachsisch.-béhm,
Kreidegeb.”’ p. 38, pl. ix. fig. 2.

1846. ,, a A. E. Reuss, ‘‘ Verstein. d. bohm. Kreideform.”’ pt. ii. p. 98,
pl. xli. fig. 8.

1850. _,, + F. Dixon, ‘“ Geol. and Foss. Sussex,”’ pl. xxx. fig. 30.

NS Seuetes 35 A. Fritsch, “ Rept. u. Fische d. bohm. Kreideformation,’’ p.
12 (woodcut).

Almost all the teeth of Notidanus met with in the Upper Cretaceous
formations are referable to a single widely-spread species, N.
microdon. This is a small form with a total number of five to nine
distinct cones in its side teeth, each of these being slender and sharply
pointed, and the principal cone usually much elongated compared
with the remainder: there are also well-marked denticulations on
the front edge of the crown.

On examining a large series of specimens, such as that available
for study in the British Museum, considerable variations are at once
apparent; but there are scarcely any discrepancies in size, and the
presence of intermediate forms renders it quite impossible to recog-
nize more than a single specific type. Some (Fig. 10) are obviously
from the front of the upper jaw, and consist only of a single large
cone, with one or two small denticles behind; while the short teeth,
with prominent principal cone and 4—5 secondary cones (e.g. Figs.

214 A. Smith Woodward—On the Genus Notidanus.

11, 12) may be referred with almost equal certainty to situations in
the upper jaw somewhat further back. The elongated teeth, which
belong to the sides of the lower jaw—and perhaps partly to the
upper—usually have the principal cone relatively prominent (Figs.
13—15), though in one or two examples such is not the case.
The anterior serrations are mostly fine and numerous, but in a few
instances (of upper teeth) they are reduced in number and increased
in size.

Of British Cretaceous strata, the various divisions of the Chalk
appear to yield the most abundant remains of N. microdon, although
the Cambridge Greensand also affords a considerable number. The
National Collection comprises specimens from Maidstone, Burham,
and Charing in Kent; Lewes and other localities in Sussex; Guild-
ford in Surrey ; and Swaffham and Norwich in Norfolk.

10. N. tanczoxatus, sp. nov. Pl. VI. Fig. 16.

In the Egerton Collection of the British Museum there is a single
upper tooth of Notidanus (rp. 1227) from the Gault, which it appears
impossible to identify with any species hitherto described. It is
much larger than the corresponding teeth of N. microdon, and as its
most conspicuous feature consists in the comparatively long and
narrow form of the cones, I propose to distinguish this type of
tooth by the provisional name of N. lanceolatus. The principal
cone is relatively prominent, and is preceded by two very long
denticles : there are three secondary cones, and the crown terminates
in a minute denticulation. The great development of the anterior
denticles renders it likely that the lower teeth were somewhat
similar to those of N. pectinatus, Ag., but the latter is a much smaller
species.

11. N. pecrinarus, Agassiz.
1848. WV. pectinatus, L. Agassiz, ‘‘ Rech. Poiss. Foss,’ vol. iii. p. 221, pl. 36, fig. 3.

A species founded upon a tooth from the Chalk, about the size of
N. microdon, but especially differing from that form in the conversion
of the anterior serrations of the crown into a series of distinct
denticles. This type of tooth appears to be extremely rare, and I
have not seen any examples.

12. N. penvatus, sp. nov. Pl. VI. Figs. 17, 18.

Among the Selachian remains in a collection of New Zealand
fossils sent by Dr. Hector to the British Museum in 1876, there are
two teeth from the Cretaceous of Amuri Bluff which are undoubtedly
referable to the genus Notidanus. In several respects they differ
from one another to a considerable extent, but an acquaintance with
the dentition of living Notidanide can leave no doubt that they
belong to a single specific type, and that the one is an upper tooth,
while the other formed part of the mandibular series.

The lower tooth, which is ‘shown of the natural size in Fig. 18,
exhibits three small denticles in front of the principal cone, the first
being the largest and having a recurved apex, the second slightly
smaller with straight but backwardly-directed point, and the third

A. Smith Woodward—On the Genus Notidanus. 215

very much more minute. Behind the principal cone, which is
scarcely more robust than that immediately following, there are
ranged three other cones, of gradually diminishing size ; and posterior
to these a minute denticulation is visible.

In the upper tooth (Fig. 17) the principal cone appears more
definitely contrasted with the others. In front there are two distinct
denticles, the first being three times the size of the second, and the
principal cone itself is placed almost vertically with respect to the
base-line of the crown, although its anterior edge has a much less
abrupt slope than the posterior. Behind this, there are three other
cones rapidly decreasing in dimensions; the first, somewhat inclined
backwards and three-fourths the size of the principal cone; the
second, backwardly directed at a corresponding angle, but only
about one-third as large as the first; and the third, a minute, broad
acuminate denticle. Though now imperfectly shown, the base-line
of the crown was obviously arched, and the remains of the root
indicate the usual configuration and robust proportions of an upper
tooth.

On considering this assemblage of characters, the substitution of
distinct denticles for the ordinary serrations on the anterior edge of
the principal cone in the lower tooth, is obviously the most striking
feature; and hence it is proposed to distinguish the present modifi-
cation under the specific name of WV. dentatus. The only other fossil
Notidanus that exhibits this peculiarity is the very rare N. pectinatus
from the English Chalk, but this is a much smaller species, and
differs in possessing a longer series of cones behind the principal.
Among existing forms, however, one appears to be remarkable for
its possession of the very same character.! This is the little WN.
pectorosus from the seas off the Patagonian coast, and Mr. Garman’s
description ? of the lower tooth of this form agrees almost precisely
with the particulars given above ; he states that each tooth “has one
to two small, followed by four moderate-sized, cusps, the anterior of
the four being little if any longer than the other three; and, in cases,
there is also a small cusp on the posterior portion of the base.”
Indeed, in the absence of figures, WV. dentatus can only be distin-
guished from N. pectorosus by the presence of one more anterior
denticle in its teeth, and by its relatively gigantic size—for’ the
Patagonian species is only 16 inches in total length.

If subsequent researches tend to substantiate the latter statement,
the fact becomes of unusual interest, since it was from the same
deposit at Amuri Bluff that Mr. E. T. Newton, a few years ago,°
made known a tooth of Callorhynchus, differing only in minor points
from C. antarcticus of the present southern seas. This living
Chimeroid ranges through the same ichthyological province as Mr.
Garman’s new species of Notidanus, and the association of two extinct

1 The lower teeth of V. cinereus also exhibit some approach to this character,

2 §. Garman, ‘‘A species of Heptranchias supposed to be new,’ Bull, Essex
Institute, vol. xvi. (1884), pp. 56, 57.

3 EK. T. Newton, ‘‘On Two Chimeroid Jaws from the Lower Greensand of New
Zealand,’ Q. J. Geol. Soc. vol. xxxii, (1876), pp. 329, 330, pl. xxi. figs. 6—9.

216 A. Smith Woodward—On the Genus Notidanus.

allies in a formation said to be of Cretaceous age in New Zealand is
a very remarkable circumstance.!

13. N. serratissimus, Agassiz. Plate VI. Figs. 23-26.

1766. Dens Squali, G. Brander, ‘‘ Fossilia Hantoniensia,” fig. 111,

1843. WV. serratissimus, eae “ Rech, Poiss. Foss.’’ vol. iii. p. 222, pl. 36,
os. 4, 5.

1870. eS 53 F. Romer, ‘Geologie von Oberschlesien,’’ p. 379, pl. 48,
g. 1.

This species was founded upon two teeth from the London Clay
of Sheppey, said to be preserved in the collection of Dr. Bowerbank,
but not now recognizable among the specimens acquired by the
British Museum. The teeth are comparatively small—the largest
I have examined not attaining a length of two centimetres—and the
total number of cones appears to vary from five to ten, according to
the situation in the mouth. The principal cone is only slightly longer
than the first of those immediately following, but it is somewhat
more robust and has its anterior edge much produced forwards and
strongly indented with a series of regular serrations throughout half
its length. The apices of all the cones are more or less blunt.

Fig. 23 represents a typical tooth of this species, such as was
known to Agassiz. I have not succeeded in satisfactorily deter-
mining whether it appertains to the upper or the lower jaw; but in
addition to this form the London Clay also yields a number of more
elongated teeth, which are undoubtedly referable to the mandibular
series. An adult specimen is preserved in the Museum of Practical
Geology, and there are several immature examples in the British
Museum. Three of the latter are shown in Figs. 24-26, and, except
in size, they only differ from the adult in being either destitute of
anterior serrations or exhibiting very delicate traces of them.

In England, N. serratissimus appears to be almost exclusively
confined to the London Clay, rarely occurring in the Middle Hocenes
of Barton and Bracklesham. On the Continent, however, Dr. Romer
has described (loc. cit.) a similar tooth from the Lower Miocene of
Zabrze, Silesia.

14. N. primicenius, Agassiz. Pl. VI. Figs. 19-22.

1843. WV. primigenius, L. Agassiz, “ Rech. Poiss. Foss.’’ vol. iii. p. 218, pl. 27,
figs. 4-8, 13-17.

1843, NV. recurvus, L. Agassiz, ibid. p. 220, pl. 27, figs. 9-12.

1849. NV. primigenius, R. W. Gibbes, Journ. Acad. Nat. Sci. Philad. ser. 2, vol. i.
p. 195, pl. xxv. fig. 95.

1852. ,, a A. Quenstedt, ‘‘ Handb. Petrefakt.” p. 167, pl. 13, fig. 3.

1S Seuee Bs J. Probst, Wiirttb. Jahreshefte, vol. xiv. pp. 124-127. )

USiieeiis » R. Lawley, Atti Soc. Toscana Sci. Nat. pp. 66-68, pl. i.
figs, 1-6.

1877. WV. recurvus, R. Lawley, ibid. pp. 69, 70, pl. ii. fig. 1. 4
1379, 5; 5 J. Probst, Wiirttb. Jahresh. vol. xxxv. pp. 162, 163, pl. iii.
figs. 12-17.

1 Tn addition to Notidanus dentatus, the National Collection also comprises three
teeth of Oxyrhina and one of Odontaspis from these beds; the former bear a very
close resemblance to the common O. Mantelli of the European Cretaceous, though
there are not sufficient materials to establish their identity ; and the Odontaspis is
indistinguishable from the well-known O. subulata of the same age.

8. 8. Buckman— Jurassic Brachiopoda. 217

1879. WN. primigenius, J. Probst, ‘bid. pp. 158-162, pl. iii. figs. 1-5.
1885. ,, 5 F. Noetling, Abh. Geol. Specialk. Preussen u. Thiiring.
Staaten, vol. vi. pt. 8, pp. 17-19, pl. i. figs. 4, 5.

Among the fossil Notidanide, the dentition of N. primigenius
appears to be more completely known than that of any other.
Lawley in Italy, and Probst in Wiirtemberg, have both contributed to
its elucidation, and though Agassiz stated that during his elaborate
researches he had only succeeded in determining lower teeth, there
can be little doubt now that he also figured some belonging to the
upper series. It seems probable that fig. 138 of plate 27 in the
“ Poissons Fossiles’” really represents a tooth of the upper jaw; and
if the originals of figs. 4-8 are correctly associated with the others
(which is perhaps questionable), these likewise must be referred to
a similar situation: it is almost certain, too, that the so-called N.
recurvus is an upper tooth of the same species.

In the mandibular teeth of N. primigenius (Fig. 22), the principal
cone is only slightly longer and more robust than that immediately
following, but the lower part of its anterior edge is much produced
forwards and bears a number of small serrations, which decrease
in size from above downwards. The secondary cones gradually
diminish as they approach the hinder end of the crown, and of these
there are usually five or six. The median lower tooth is not yet
certainly known, although both Probst and Lawley venture to claim
its discovery. The former figures it as having a median cone, while
the latter represents it as possessing only lateral cones—so that as
it is impossible for these to belong to the same species, neither deter-
mination can be accepted as correct until more satisfactory evidence
of association is forthcoming.’

(To be continued in our next Number.)

II].—Nores on Jurassic BRACHIOPODA.
By S. 8S. Buckman, F.G.S.

HE following notes relate to two Brachiopods—a Rhynchonella
and a Terebratula—figured by the late Dr. Davidson in his last
plates in the Paleontographical. Of the first a change of name is
‘necessary ; of the second, I consider that the identification needs
revision, and that it deserves a separate name. Both species are
from the Inferior Oolite.

RHYNCHONELLA LiosTRACA, 8. Buck.

1883. Rhynchonella bilobata, S. Buck., Brachiopoda Inf. Ool. Dorset, Nat. Hist.
Soc. Proc. vol. iv. p. 50.
— bilobata, Davidson, Appendix to Supplement Brachiopoda,
Paleontographical Soc. Proc. vol. 38, plate 19,
figs. 18, 19.
Having given the above references, there can exist no doubt as to
the species intended; but having subsequently found that the name
bilobata had been used for a species of Rhynchonella previous to my

1884.

1 In his second paper (1879) Probst confirms his original determination (1858) and
suggests that Lawley’s fossil probably belongs to WV. ggas or N. Meneghinit.

218 S. S. Buckman—Jurassie Brachiopoda.

applying it to this one, I take an early opportunity of altering the
name of the species to Rhynchonella liostraca.

The late Dr. Davidson, whose kind assistance I have so often
experienced, gave capital figures in his Brachiopoda (reference
quoted above) of this most peculiar species. In the Inferior Oolite
of England there is not as far as is known any species that at all
approaches to this one in character, or with which it could pos-
sibly be confounded. The complete absence of any ribs, except just
at the junction of the valves at the base, has induced me to give it
the name of liostraca. It is an extremely rare form, and has only
been met with at a few places. There are probably not more than
eight or nine examples known. Its horizon is the Sowerbyi zone at
one or two quarries near Bradford Abbas in Dorset, and near Corton
Denham in Somerset.

The late Dr. Davidson, under the name Dilobata, figured the types
of this species, both of which were collected by myself. The one
represented in fig. 18 I presented to Dr. Davidson, and it is now
probably in the Natural History Museum.

The only species at all resembling this one with which I am
acquainted is Rhynch. trigona, Quenstedt, Brachiopoda, plate 40, fig. 71;
but, as I stated in first describing this species, it differs from Rh.
trigona in having a well-marked deepish furrow in dorsal valve,
no ribs at all, but only notched at base, and dorsal valve convex from
beak to base.

TEREBRATULA EUIDES, 8. Buck.

1883. TLerebratula dorsoplana Buck., non Waagen. Proc. Dorset Nat. Hist. Soc.
vol. iv. page 14.

1884. Terebratula Fleischeri? Davidson, non Oppel. Brachiopoda, Paleont. Soc.
Proc. Appendix to Supplement, plate 19, figs. 4-4a, page 262.

This peculiar biplicated species has been a considerable puzzle.
As can be seen, I referred it to Terebratula dorsoplana, Waagen ; 1
but Dr. Davidson, in the course of correspondence with Dr. Waagen
on the subject, came to the conclusion that this identification was
incorrect, a view in which I now alsoconcur. In fact, a comparison of
the beaks of the specimens as represented by Waagen and Davidson
will show the difference. The foramen in Waagen’s figure being
very small, separated from the umbo, and showing the deltidium,
while this species possesses a large circular foramen almost touching
the umbo. One point that is not quite brought out in Davidson’s
figure is the rather pinched appearance of the beak, in consequence
of rather prominent beak ridges and a carina down the middle of
the ventral valve.

Dr. Davidson referred this species to Terebratula Fleischeri, Oppel,
but with this I cannot agree. Dr. Oppel? took as the type of his
Tereb. Fleischeri the specimen figured by Davidson, Jurassic Brachio-
poda, Pal. Soe. pl. xiii. fig. 7, which is an elongated slightly biplicated
shell, much longer and narrower than the one under discussion, and
it lacks the peculiar beak ridges and pinched appearance of the beak.

1 Geog. Pal. Beitrige, plate 31(8), fig. 7.
2 Oppel, Juraformation, page 497.

Grenville A. J. Cole—Igneous Rocks of Stanner. 219

Our species has often been confounded with Tereb. perovalis, Sow.,
and Tereb. Stephani, Davidson. From the first it is easily dis-
tinguishable by its larger plications and its carina down the larger
valve, but these characteristics unite it with Tereb. Stephani, from
which, however, it may be distinguished by a shorter, less incurved
beak, and its plications not extending so far up the valves. The
characteristic beak ridges as mentioned before are not possessed
by either of these other two species.

Terebratula ewides is rather rare. It has been found chiefly in a
quarry about two miles from Sherborne, in Dorset, in a sandy bed at
the very bottom of the Murchisoniz zone, along with Terebratula
simplex, Buck., also at one or two other places near Sherborne. It is
somewhat variable in width, and the edges of the valves are generally
slightly thickened by lines of growth. I take as the type of this
species Davidson’s figure, Brachiopoda, Pal. Soc., Appendix to
Supplement, plate 19, figs. 4, 4a, which are drawn from a specimen
in my collection.

This species is frequently longer and narrower than the speci-
men figured by Davidson, sometimes, but rarely, wider. The folds
are also slightly variable.

IV.—Tut Ienrous Rooks or STANNER.

By Grenvitte A, J. Corz, F.G.S.,
Demonstrator in the Geological Laboratory, Normal School of Science and Royal
School of Mines.

(7\HE area near Old Radnor marked by invitingly igneous colouring
on Sheet 56 8.H. of the Geological Survey Map deserves atten-
tion from more than a petrographic point of view. Murchison, in
his “ Silurian System,” has extolled the charms of the surrounding
scenery, and the Rev. W. 8. Symonds has repeated this admonition
to the tourist. The borderland is in truth here eminently picturesque,
from the great escarpment of the Ludlows to the high moor of
Radnor Forest, the very stratified deposits yielding singular variety
of form. The present paper, however, deals merely with one ridge,
called Stanner Rock, comparison being occasionally made with its
rival, Hanter Hill, from which it is divided only by a narrow vale.
Murchison! in 1839 compared the masses composing both these
hills to the “ hypersthene”’ rocks of Loch Coruisk, and stated that
a variety of greenstones and “felspar rock”’ were also to be found.
The differences, indeed, between specimens obtainable within short
distances of one another may account for the fact that on the Survey
Map Hanter Hill is coloured as syenite and Stanner Rock as green-
stone; whereas Murchison clearly recognized the close relations of
the main masses of the two. Dr. Callaway has also touched on the
constitution of these hills when dealing with the Pre-Cambrian
rocks of Shropshire,” and mentions a compact grey felstone as

occurring in the centre of the ridge of Stanner Rock.
It is, indeed, at once apparent when one faces the bold cliff which

1 Silurian System, p. 318, 2 Quart. Journ. Geol. Soc. vol. xxxv. p. 660.

220 Grenville A. J. Cole—Igneous Rocks of Stanner.

terminates Stanner Rock that the dark mass is traversed by pale
intrusive veins of a very different nature; and an examination of
the “greenstone” itself reveals a number of dykes and veins of
every variety of grain, reminding one of those cutting through the
gabbros in the mountains round Coruisk. No true lavas or scoria-
ceous products remain about the flanks of Stanner, as about Corndon
in the north or the Carneddau farther west ; we have to deal largely
with crystalline materials, which divide themselves at the outset into
a more acid and a more basic series. The former, clearly intrusive
in the latter, marks the later stages of eruption.

With the relations of these masses to the surrounding deposits I
am not as yet prepared to deal. Murchison’s prediction that igneous
intrusions underlie the altered Woolhope of Nash Scar! has not, so
far as I am aware, been verified, and evidence of the penetration of
this crystalline limestone by igneous veins is wanting at Brook
Quarry and Yat Hill. I have failed to find satisfactory junctions
between Stanner and Hanter Hill; but may add that I have not
found pebbles from these hills in the ancient conglomerate of Old
Radnor, which underlies the Woolhope Limestone. It is yet un-
certain whether the local alteration can be attributed to faulting and
to crushing down against hard earlier igneous masses, or whether it
is due, as Murchison held, to the intrusion of those masses in times
later than Silurian. ,

I. Tam Acip Surrzs.

The most highly crystalline member of this series is a pale pink-
grey pegmatite—the word being employed in its original sense *—
which passes from a well-developed graphic granite through finer
varieties to a practically micropegmatitic form. This gradation is
beautifully seen on the edge of a vein in Stanner cliff, of which
a microscopic section has been prepared; where the cooling has
been fairly rapid, along the line of junction with the more basic
rock, a selvage of minuter graphic structure occurs, graduating off
in a distance of 3 millimetres into the normal coarser form (Fig. 1).

This graphic granite is best developed in veins, not many inches
wide, on the southernmost summit of Stanner Rock. Under polar-
ized light the felspar presents the microcline structure, and extin-
guishes—as one would have inferred from its cleavage-surfaces on
the rock-mass—uniformly over considerable areas. The areas of
entangled quartz show similar optical connexion, as is the case in so
many pegmatites, as though we dealt, not with isolated inclusions
in a felspar, but with a complex intergrowth of large quartz and
felspar crystals. Some portions exhibit a lamellar arrangement of
the two constituents; but this appears to have no relation to
proximity to the edges of the vein.

The rock is much cracked and .faulted, minute bands of fault-
rock appearing in microscopic sections. Hornblende prisms, and
perhaps tourmaline, occur in a subordinate manner.

The less crystalline members of the Acid series are found in

1 See “ Siluria,”’ 5th edition, p. 108.

* Hatiy, Traité de Min. 2nde édit. tome iv. p. 536. “De mnypa, c’est-a-dire
renfermant des piéces qui sont comme fichées dans une matiére principale.”

Grenville A. J. Cole—Igneous Rocks of Stanner. 221

several dykes crossing the ridge approximately from east to west.
In the hollow north of the pegmatite summit there is a considerable
development of grey-white and compact felsite, which, from its
frequent appearance at the surface, must form a great part of
the centre of the hill. In section this rock is seen to contain
scattered porphyritic crystals of quartz, a few plagioclase felspars,
and irregular patches of fibrous hornblende, which is to all appear-
ance secondary. Numerous small green prisms, often chloritized,
are associated with the matrix, which consists of closely-set spheru-
lites, often formed about minute felspars, the structure being only
revealed by polarized light." The radial lines of the spherulites are

Fic. 1.—Section showing Junction of Pegmatite and ‘‘Diabase,” Stanner Rock. x 7.
Fic. 2.—Section of Quartz-Felsite, Stanner Rock, showing corroded quartz and
felspar microlite, serving as centres to spherulites. x 70. ;

Fig. 3.—Section cf Augite-Diorite (‘‘ Diabase’’), Stanner Rock, showing inter-

growth of biotite and augite. x 70.

1 Very similar rocks from eastern Victoria have been described by Mr. Howitt
under Kosenbusch’s name of Quartz-granophyrite (“The Rocks of Noyang,”
Trans, Roy. Soc. Victoria, 1883),

222 Grenville A. J. Cole—Igneous Rocks of Stanner.

brought out distinctly, but, in place of the formation of a black
cross, extinction occurs in two, three, or more sectors at a time,
which yield coloured polarization in intermediate positions. This
points to secondary crystallization having set in, with the usual
passage from a glassy or cryptocrystalline to a microgranular con-
dition. Just as the most detailed structures of the original glass,
down to the forms of the minute included crystallites, are preserved
in the secondary granules of our ancient rhyolites, so here the
spherulitic form and structure remain, in spite of more complete
crystallization of the mass. Under higher powers the polarization-
effects of the sectors are themselves seen to be complex. A delicate
feathery structure has developed, sometimes in pinnate diverging
lines, sometimes as a mere network, and the areas into which the
spherulite has divided have often become thus minutely pegmatitic.
The network commonly extinguishes in one position, while the
interspaces extinguish in another—a point best observed when
magnified some 400 diameters.

MM. Fouqué and Lévy have figured’ a quartz-porphyry from
near Saulieu, Cote-d’Or, which is almost the precise counterpart of
the felsitic rocks of Stanner. They find in the spherulites sur-
rounding porphyritic and corroded crystals of quartz a network
that extinguishes simultaneously with the pre-existing central
crystal; a complete predominance of this material in the spherulite
gives rise to what they have termed Quartz globulaire. ‘The micro-
pegmatitic structure of these authors appears to give similar effects,
as if the radiating lines of quartz were an attempt to enlarge in
optical continuity the crystal about which they have developed. A
dyke running E.N.H. in the wood upon the northern slope of Stanner
contains, in addition to a multitude of orthoclase and plagioclase
microlites, numerous corroded grains of quartz; each of the latter
has served as a centre of devitrification (Fig. 2), and in several
instances the highly-interesting observation of MM. Fouqué and
Lévy may be repeated on these British spherulites. When com-
parison is made with similar rocks of much more recent date, it
appears at least probable that the mesh-work structure (of quartz
and felspar?) is in reality of secondary origin. So far as I am
aware, it does not occur, at any rate freely, among the compactly-
spherulitic rhyolites of later Tertiary days; but in a dyke traversing
the Lias of Broadford, Isle of Skye, and belonging to the pre-
Miocene series of eruptions, we have what looks remarkably like
the commencement of such a structure by alteration. The spheru-
lites mostly exhibit a dark cross, with, however, a tendency towards
a granular condition; and the meshy micropegmatitic appearance
occurs only in a few individuals, in a manner strongly suggesting
a development of quartz among their previously homogeneous fibres.*
It is quite conceivable that such secondary quartz might adopt the
orientation of an included and rounded crystal, just as it is known
to do when deposited in sandstones from solution.

1 Minéralogie micrographiqne, pl. xii. fig. i. 2 Tbid, pp. 193-94.

SOE aTNddE Omani VoremMetealedeootaull aiaeyeTe. es

Grenville A. J. Cole—Igneous Rocks of Stanner. 223

In order to see whether the felsites of Stanner could be corre-
lated with the clearly acid and more crystalline pegmatite, as
common offshoots of some granite mass below, I made the following
analysis of a specimen from the central area. The specific gravity,
determined from a large specimen by Attwood’s balance, is 2°62.

SPHERULITIC QuarRtz-FeEtsitE, STANNER Rock.

SiO: ... bio 74°80
Al,Os... ssuoye8"89
Fe,03... wed trace
CaO ... 900 2°59
MgO... bat 05
K20 ... ee 2°74
Na20... Rh 5°45
Loss on Ignition 77

100°29

The rock belongs, then, fairly to the Acid series, but to the
“oranitite” rather than the granite group; similar proportions
of the alkalies, implying a fair amount of oligoclase-material, are
found even among the rhyolites.

I have not been fortunate enough to find these white felspathic
rocks repeated on Hanter Hill, though the community of other
characters in the two hills leads one to suspect that they occur.

Il. Tue “Drasase” SERIES.

The greenstones that compose the bulk of Stanner Rock form
various links in the series between the augite-plagioclase rocks
and the ordinary hornblende-diorite group. In coarse-grained speci-
mens from Hanter Hill, as well as from Stanner, green fibrous
crystalline areas occur that by their extinctions may well be altered
enstatite. The pale green products that abound, however, are very
largely chloritic, and may be considered “tertiary ” in origin, when,
as is so frequently the case, they are derived from the acicular or the
more massive hornblende that is itself developed at the expense of
diallage or augite. Olivine was very probably a constituent part
of the summit masses of Hanter Hill; and, following the nomen-
clature adopted by Prof. Judd,’ the rock is there a diallage-gabbro
traversed by veins of dolerite, to which the small rounded augites
give a marked granulitic structure. The felspars are extensively
“schillerized,”* and even the minuter augites of the dolerites
are in the diallage condition, chloritic pseudomorphs resulting from
their complete and final alteration. In one gabbro the passage from
diallage into hornblende is very beautifully seen.

But many of the greenstones of Stanner show no signs of former
olivine, while chlorite is extensively developed in them from diallage,
augite, and green hornblende. In one fine-grained holocrystalline
rock, with a specific gravity of 2°86, biotite and augite are closely
intergrown (Fig. 3), and form, with plagioclase felspar, the chief
original constituents. Titanoferrite and prisms of apatite are also
present. The biotite and the augite alike pass into green products,

1 “ Tertiary Gabbros, etc., of Scotland,’ Q. Journ. Geol. Soc, vol. xlii. p. 62.
* Judd, Q. J. G.S, vol. xli. p. 383.

224 Grenville A. J. Cole—Igneous Rocks of Stanner.

among which hornblende is occasionally recognizable ; and quartz
often fills the interspaces between the sharply-defined ends of
felspar prisms. In other specimens, notably in a coarse variety on
the most northern summit, ophitic structure prevails, the felspar
being labradorite, according to a determination by Szabé’s method
made by Mr. J. F. Brooks. The most finely-grained rock of this
series appears as a compact grey-green vein above Stanner cliff,
and, with its porphyritic plagioclase felspars characteristically cor-
roded by the matrix, and its brown clouded patches of augite, at
first difficult of recognition, must be classed as an augite-andesite,
and, when fresh, must have resembled many Tertiary lava-flows.
The whole of the foregoing altered series, from the decomposed
(olivine) gabbros to this hemicrystalline vein, come, then, con-
veniently under the head of ‘“ Diabase.” It is, however, this very
comprehensiveness, sanctioned by long usage—witness “ Diabas-
mandelstein”—that makes the name valueless when limited to one
rock-species.

Prof. Judd! has recently pronounced against “‘ Diabase”’ in favour
of “Gabbro” for coarsely-crystalline rocks that can be shown to
have contained olivine as well as plagioclase and augite, and has
discussed the current terminology from a basic point of view. Since
there is a growing tendency to employ ‘“ Diabase” for the granitic
augite-plagioclase rocks, thereby defining closely what has ‘become
a really valuable field-term, I may perhaps venture to give briefly a
historic outline of the position.

In 1813 Alexandre Brongniart? put forward the name Diabase
for rocks “composée essentiellement d’amphibole hornblende et de
felspath compacte,” including in this the famous orbicular rock of
Corsica. Haiiy * subsequently employed Diorite (implying the dis-
tinctness of the two constituents) for the same rocks, which he
distinguished from syenite by a greater predominance of hornblende ;
and this name prevailed so far that Brongniart in 1827* very grace-
fully yielded up his prior term—invented, as he pathetically remarks,
by one familiar with ancient and modern languages—lest science
should be cumbered with two names for precisely the same thing.
He admits diallage and mica among the accessory minerals of the
Diorite which he thus helped to establish.

Diabase therefore ceased to exist, until Hausmann ® very effectually
revived it for the series of rocks containing ‘‘ hypersthene,” labra-
dorite, and chlorite, varying in structure from highly-crystalline to
scoriaceous, which he found associated with his two classes of
Diallage-Labradorite and ‘“ Hypersthene ”-Labradorite rocks. But
this ‘‘hypersthene” being for the most part only a lustrous augite,
analyses revealing its chemical identity with diallage,* Diabase

1 Quart. Journ. Geol. Soc. vol. xlii. pp. 61-2.

2 « Kesai d’une classification des roches,”” Journ. des Mines, July, 1813.

3 Traité de Min, 2nde édit. tome iv. p. 536.

4 Classification des roches homogénes et hétérogénes, p. 80.

5 Ueber die Bildung des Harzgebirges, 1842.

6 See vom Rath, “Chemische Untersuchungen einiger Griinsteine aus Schlesien,”
Poggend. Annalen, xcy, (1855) p. 546.

Grenville A. J. Cole—Igneous Rocks of Stanner. 225

naturally came to cover all augite-labradorite-chlorite rocks, of
whatever grain, i.e. (pre-tertiary) altered masses verging on one side
into the diorite, and on the other into the (olivine) gabbro series.

What, then, are we to do with the highly-crystalline representa-
tives of the augite-andesites? It seems unnecessary to extend
Eucrite (augite-anorthite rock), if we can employ some more familiar
term. The bulk of the gabbros are, as Prof. Judd has shown, so
connected with the basalts, that we are still left with a gap, and into
this diabase has somewhat naturally stepped. Messrs. Hague and
Iddings' employ it in this sense, connecting, in their admirable
series of observations, diorite and hornblende-andesite, diabase and
augite-andesite ; and De Lapparent® also makes of his diabases a
series exactly parallel to his (hornblende) diorites. But the diffi-
culty of thus defining their position as distinct from diorite is shown
by Boricky’s* use of diabase for hornblende-plagioclase rocks
where the former mineral can be shown to have been derived from
augite; and the fact that many diorites are in this sense altered
diabases must lead to considerable confusion,* two parts of the same
mass retaining the same essential structure, and yet receiving different
names.

Now Zirkel® has long ago given us a class of augite-diorites
distinguished from his diabase by containing oligoclase and not
labradorite ; but now that the nature of the felspar no longer
restricts the diorites, this class becomes correspondingly extended
and fills admirably the vacant place. Augite and enstatite diorites
should seem no more strange than the corresponding varieties of
andesite, and the close relations of the pyroxenes and the amphi-
boles appear to support this comprehensive view, viz. that the
diorites form a natural group, containing now hornblende, now
mica, now augite, or now, as in the case of rocks at Stanner, two or
even three of these constituents.

Diabase then remains much where Hausmann placed it, as a
common term for the more basic altered augitic rocks, without
question as to their age or much regard for structure. Not that
it is better in itself than ‘‘ Greenstone,” but that it is sanctioned
by more international usage. My excuse for dwelling thus far on
what may seem foreign to the mere description of the rocks of
Stanner lies in the fact that so many areas of augite-plagioclase
rocks (Augite-Diorites) occur upon our western border. Vague
and general terms are too valuable to be lost sight of in the
field ; but the use of an inexact name where another more closely
expresses an observed relationship can only be, and has been in
the past, a source of misapprehension and confusion.

Many of the rock-sections above referred to have been made, and
the chemical work has been carried out, in the Geological Laboratory
of the Normal School of Science and Royal School of Mines,

1 Bulletin U. S. Geol. Survey, No. 17.

2 Traité de Géol. 2me édit. p. 627. 3 Tscherm. Mittheil. ii. (1880) p. 78.
4 See Hague and Iddings, Bull. U. S. Geol. Sury. No. 17, p. 21.

5 Lehrbuch der Petrogr. (1866) ii. p. 7.

DECADE III.—VOL. III.—NO. V, 15

226 Notices of Memoirs—Prof. J. W. Judd—WNile Delta-Borings.

N@OTtCGznS )9O2 |) | ava VEO Ss

—E—E—EE

I.—ReEport oN A SERIES OF SPECIMENS OF THE DEPOSITS OF THE
Nite DeELtTA, OBTAINED BY THE Recent Borinc OPpERrAtIons.
By J. W. Jupp, F.R.S., Pres. Geol. Soc. Proceedings of the
Royal Society, No. 240, 1886, pp. 213-27.

HIS paper contains the results of a microscopic analysis of
specimens from the borings, which have lately been carried on,
under the auspices of the Royal Society, in three different places in
the Nile Delta. That at Kasr-el-Nil, Cairo, was carried to a depth
of 45 feet, whilst those at Kafr-ez-Zayat and Tantah, places about
half-way between Cairo and the Mediterranean, were 73 and 84 feet
deep respectively. In none of these borings was the rocky floor of
the Nile valley reached. The beds passed through consisted of an
admixture, in varying proportions, of blown sand and alluvial mud.
The sands, when examined under the microscope, are seen to consist
. of two kinds of grains; the larger, usually perfectly rounded and
polished, are of quartzitic materials evidently derived from granitic
rocks, with particles of red and brown jasper, Lydian stone, frag-
ments of silicified wood, nearly unaltered felspar grains, hornblende
and jade. The smaller sand grains, often subangular and angular,
include a greater variety of minerals than the larger, and comprise,
in addition to those above mentioned, mica, augite, enstatite (?),
tourmaline, sphene, iolite (cordierite), zircon, fluorspar, and mag-
netite, all in a nearly unaltered condition. These sand grains have
been derived either directly from the breaking up of granitic and
metamorphic rocks, or from older sandstones formed of the debris of
these rocks.

The mud is singularly deficient in kaolin, and seems to be com-
posed of extremely minute chips and flakes of quartz, felspar, mica,
hornblende and other minerals, mingled with some organic particles
and frustules of Diatomacez. In the Tantah boring fragments of
tufaceous limestone were also met with.

The striking feature in the character of these delta deposits is the
comparatively unaltered condition of the felspars and other complex
silicates in the sands and muds, and the absence of kaolin. Under
the usual processes of disintegration of rocks in temperate climates,
the felspars and other silicates are reduced by chemical action to
soluble silicates of potash, soda, etc., and carried away in solution,
whilst the kaolin remains behind. It appears, however, from the
nature of these deposits, and from the small amount of soluble solid
matter in the water of the Nile, notwithstanding the concentration
resulting from extensive evaporation, that chemical action has had
but little effect in the drainage area of the Nile, in comparison with
the mechanical influences resulting from extreme variations of tem-
perature, the action of the winds, and torrential rains. G. J. H.

Notices of Memoirs—J. Petho—Mammalia from Baltavar. 227

IJ.—Ueser pie Fosstnen SAUGETHIER-UEBERRESTE VON BALTAVAR.
Von J. Pernod. Jahresbericht d. K. Ung. Geolog. Anstalt fiir
1884, pp. 63-73. Budapest, 1885.

On tHE Fosstn Mammantan Remains Fron Battavirz. By
Dr. J. Perso. Annual Report of the Royal Hungarian Geo-
logical Survey for 1884.

BOUT 385 years since, some remains of fossil mammalia were
discovered near Baltavar, in the Trans-Danubian province of
Hungary, which Prof. Suess determined to be nearly entirely
identical with the Pikermi fauna. They consisted of the following
species : Muachairodus cultridens, Hycena hipparionum (=H. eximia,
Gaudry), Dinotherium, Rhinoceros, Sus erymanthius, Antilope brevi-
corms, Helladotherium Duvernoyi, and Hippotherium gracile. The
deposit was supposed to have been exhausted, but now lately fresh
remains have been discovered by the Hungarian Survey, and from
these, and from the collection stored in an adjoining monastery, Dr.
Petho has determined the under-mentioned list of fresh species,
which further show a remarkable connection with those from
Pikermi. They include Mesopithecus Pentelicit, Wagn., Dinotherium
giganteum, Kaup, Mastodon Pentelicit, Gaudr. et Lartet, Tragoceros
amaltheus, Roth-Wagn., Cervus, sp., cf. Matheronis, Gerv., Chali-
cotherium Baltavérensis, n.sp., and Rhinoceros pachygnathus, Wagn.

gee at) VP SED IVY -

THe Survey or Western Patestine. Memoir on THE PHysIcaL
GEOLOGY AND GEOGRAPHY oF ARABIA PETR#A, PALESTINE, AND
Apsornineé Districts, Wirn SpeciaL REFERENCE TO THE MopE
or FormaTION oF THE JORDAN-ARABAH DEPRESSION AND THE
Dap Sea. By Epwarp Hutt, LL.D., F.B.S., 4to. pp. 145,
with Maps and Sections. (Published for the Committee of the
Palestine Exploration Fund, 1886.)

T is now generally recognized that the social and political history

of the inhabitants of any country has been largely influenced
by its physical characteristics, and that consequently in order to
elucidate the one, it is necessary to obtain a thorough knowledge of
the other. The Committee of the Palestine Exploration Fund, in
its efforts to obtain a complete knowledge of the ancient inhabitants
of Palestine, took therefore a wise step in organizing an expedition
to this country to study its physical structure. Prof. Hull was chosen
as the leader of the expedition, and the present memoir gives the
outcome of his observations.

The geological features of Palestine and the adjoining regions
have for many years past been pretty well known through the works
of several competent investigators, amongst whom may be mentioned
Bauerman, Lartet, Milne, Fraas, Ritter, Russegger, and others, and
considerable light has also been thrown on its geology by the
explorations of Zittel in the Libyan Desert. A very excellent
résumé of the existing knowledge of the subject has been given by

228 Reviews—Prof. Hull's Survey of Palestine.

Mr. W. H. Hudleston, in a presidential address to the Geologists’
Association in 1882, to which the same author added further notes
in March, 1885.

It can hardly be expected that in the course of the short period of
two months, in which the active work of the Expedition was carried
out, Prof. Hull should have been able to add very materially from his
own observations to the already existing knowledge of the subject.
But though the contents of this memoir have been, to no small
extent, derived from secondary sources of information, it is still a
valuable contribution to the geology of Palestine, and the statements
and opinions it contains will be, by many, more relied on than those
of equally competent but supposed less orthodox investigators. As
arule, however, Prof. Hull’s researches confirm those of previous
investigators. By a strange irony of fate indeed, the author has
proved that one of his own pet theories of the former outflow of the
Jordan, through the Arabah valley into the Red Sea, is not tenable,
and he now finds the water-parting in this valley to be some hundreds
of feet above the level which the waters of the Dead Sea basin
reached, even in their greatest extension.

As regards the ancient crystalline rocks of the Sinaitic region, the
author accepts, though somewhat hesitatingly, the views of Fraas and
others that they are of Archean or Laurentian age. On this sup-
position, the volcanic series which penetrates through them may be,
the author states, “of Lower Silurian age, but if we consider the
older schists to be metamorphosed Cambro-Silurian beds, then the
newer series may be of Upper Silurian or of Devonian age.” It
would be interesting to know the grounds, if there are any, for con-
sidering these crystalline schists to be of Cambro-Silurian age. The
author says in a footnote, ‘As in the case of those portions of the
British Isles where the Lower Silurian rocks have been metamorphosed
previous to the deposition of the Upper Silurian beds to which they
are unconformable.” We fail to derive any assistance from this
remarkably indefinite comparison, and should have preferred to have
had a more particular reference.

There is a great gap between the Archean crystalline and volcanic
rocks of the Sinaitic peninsula and the succeeding formation of purple
and red sandstones, of Carboniferous age, which overlie them un-
conformably. In the Wady Nasb this sandstone is covered by a
band of limestone, in which Mr. Bauerman discovered fragmentary
fossils of Carboniferous age. Some doubt was thrown upon the
determination of these fossils, but this expedition obtained others
which decisively prove the Lower Carboniferous age of the lime-
stone, and the sandstones beneath are also regarded as of the same
period. The band of Carboniferous limestone is, in its turn, overlaid
by sandstones of similar characters to those beds below it, and
these higher or Nubian sandstones pass upwards into limestones of
Cretaceous age, and are themselves probably of Cenomanian age.
In the absence of the Carboniferous limestone band—which appears
to be not extensively developed—there are no means of determining

whether the basal beds of the variegated sandstones are Carboniferous

Reviews—Prof. Hull’s Survey of Palestine. 229

or whether they are wholly Cretaceous and belong to the Nubian
series. At the Wady Nasb the Carboniferous sandstone is from 150
to 250 feet in thickness, and Prof. Hull assigned to it the not very
distinctive name of “ the Desert Sandstone,” whilst for the Cretaceous
sandstone, which has an extremely wide development both in Palestine,
the Sinaitic Peninsula, Egypt, and the Libyan Desert, the name of
the “ Nubian” Sandstone is retained.

Another outcrop of the Carboniferous Limestone is believed to have
been met with by the Expedition among the hills of Moab, east of
the Ghor, but “for lack of time” the fossils in it were not collected,
and Prof. Hull does not therefore feel confidence respecting its age.

No fresh details of importance were noted respecting the Cretaceo-
Nummulitic series of rocks of which the greater part of Palestine
and of the country east of the Jordan valley is composed. The
series consists of the Nubian Sandstone below, followed by thick
beds of limestones with bands of chert. The succession and the
character of the rocks very much resembles that described by Zittel
in the Libyan Desert, and there is also a similar absence of any
clear line of demarcation between the limestones of Cretaceous and
those of Hocene age. Fossils appear to be rare throughout the
series—the Expedition does not seem to have discovered any in fact.
It would be interesting to know whether the numerous bands and
masses of flint and chert, which occur equally in the Cretaceous
and in the Eocene strata, are, like those of the Upper Chalk of Eng-
land, derived from siliceous sponges; but nothing is noted about
them beyond that shells of Molluscs and Hchinoderms now siliceous
are occasionally found in them.

The author briefly refers to the occurrence of beds of a calcareous
sandstone, the presence of which is stated to be the key to the
physical features of the western margin of Palestine from Mount
Carmel to beyond Gaza. No thickness is assigned to the deposit,
its conformability or otherwise to the Eocene limestones below is not
mentioned, and the only fossils in it are unrecognizable fragments
of shells.

The author refers the formation provisionally to the Upper Hocene,
“ chiefly on the grounds: (1) that it is older than the sand and
gravel of the 200 feet sea-border, which may be inferred to date back
to the Pliocene: (2) that there is no evidence of any Miocene beds
in Palestine; and (3) that the rock has a very solid character and
is traversed by joint planes, similar to those of the Cretaceo-Nummu-
litic limestone.” The rock may indeed belong to the Upper Eocene,
but the grounds on which it isso placed are of the weakest character.
Thus, because Miocene beds are not known elsewhere in Palestine, is
certainly no argument why these beds may not belong to this period,
and as for the very solid character of the rock being evidence of its
Upper Eocene age, it is stated on the preceding page that this rock
“7s sometimes rather solid, but generally porous.”

With the great uncertainty respecting the age of this calcareous
sandstone, it would seem to be rather premature on the part of the
author to devote a chapter to the subject of ‘‘ Miocene period unre-
presented in Palestine and Border,’ in which it is stated that in

230 Reviews—Prof. Hull’s Survey of Palestine.

Palestine and Idumar this period is “ one of disturbance and elevation,
of faulting and flexuring and denudation of strata.”

In the chapter on ‘“ Later Pliocene to Recent Beds (Pluvial),” the
author points out that after the leading features of the land and
coast-lines had been formed by denudation, there was a depression
of about 220 feet in relation to the present sea-level. The evidence
for this is the presence of raised beaches with recent shells in the
vicinity of Cairo, also near Gaza and Jaffa at elevations of about 220
feet. The author also discovered recent corals and shells in gravelly
beaches in the Arabah valley at elevations of 80 and 130 feet above
the sea-level.

A depression of about 220 feet would unite the basins of the Red
Sea with the Mediterranean, and at the shallowest part of the
channel between them there would be a depth of 150 to 170 feet of
water. On the theory of the union it is difficult to explain the
remarkable differentiation which exists between the faunas of the
Mediterranean and the Red Sea at the present day, for if there was
such an open channel in Pliocene times, the period which has since
elapsed does not seem sufficiently long to have given rise to the
extreme dissimilarity which now exists. Prof. Hull assumes that
the two seas were disconnected in Miocene times and that the
differentiation which took place in that interval was not materially
interfered with by the Pliocene communication ; since the water was
not deep enough to allow of free commingling of the two faunas.
To most naturalists this will appear an unsatisfactory and untenable
explanation.

The author refers in some detail to the terraces of marl silt and
gravel with fresh-water shells in the more elevated beds, which
mark the different elevations of the water in the Jordan-Arabah
valley up to a level of about 1400 feet above the present surface of
the Dead Sea, or about 100 feet above the Mediterranean.

The Jordan-Arabah depression is ascribed to the direct result of a
fault or fissure of the crust, accompanied by a displacement of the
strata, arising from the tangential pressure of the Harth’s crust due
to contraction, and the depression was produced at the close of the
Kocene period. It is thought probable that the first waters of the
Dead Sea basin were those remaining from the ocean itself, and that
the fauna of the Lake of Tiberias may thus have had, in the main, a
marine origin. The author does not venture to apply this theory to
the distinctive species of Unio and other fresh-water mollusca, now
inhabiting the Jordan Valley, but regards the fishes as the descendants
of those which lived in the waters of the Eocene seas. It is, of
course, possible, but we should like to have seen some facts brought
forward in favour of the hypothesis.

According to the author this isolated basin-full of Eocene salt-
water then suffered a process of contraction, whether from evapora-
tion or otherwise, is not stated, and at the close of the Miocene, or at
the commencement of the Pliocene, the waters had been reduced to
about the level they are at present, and in the meantime the region
was being carved out by denudation into the hills and valleys of the
present day. ‘This contraction is correlated with a similar reduction

Reviews—Prof. Hull’s Survey of Palestine. 231

in volume of the Mediterranean Sea—whether both originate from a
common cause is not stated ; but whilst the reduction of the Mediter-
ranean is inferred to have taken place “at an epoch not very remote
and which may be represented by the Interglacial stage of the
Quaternary period,” the reduction of the Dead Sea is placed further
back, at the beginning of the Pliocene.

The next stage in the geological history of the Dead Sea to which
the author introduces us is that of “The Pluvial Period (Pliocene
and Post-Pliocene),” in which there was a general subsidence of the
whole region bordering the Levant and a general rising of the
inland waters, till the Jordan-Arabah depression was filled by a
lake (fresh-water ?) over 200 miles in length and over 2000 feet in
depth. This great change appears to have been produced by the
climate of the Glacial period, when the temperature of Palestine is
stated to have been 25° Fah. lower than at present, and the climate
resembled that of the British Isles. But the Dead Sea basin even
then was not filled to the brim, and it would at that time have
required no small engineering capacity to have cut a canal through
the water parting in the Arabah valley, to unite its waters with those
of the Red Sea.

Subsequently to the Pluvial period we are told by the author that
the more modern physical conditions set in, and by gradual degrees
the waters in the Dead Sea basin were for a second time reduced to
the low level now existing.

The author devotes a special chapter to the “Origin of the Saltness
of the Dead Sea,” from which it appears to be his opinion that it is
merely owing to the concentration by evaporation of the saline
ingredients which the rain-water of rivers and streams has dissolved
out of the strata through which it passes.

The author makes the following novel comparison between the
water of salt lakes and that of the ocean: “It is probable that the
water of the ocean itself has become salt owing to the same cause
which has produced saltness in the inland lakes, as it may be re-
garded as a mass of water without an outlet.” It is, however,
arguing in a circle to attribute the saltness of the ocean to the land,
whilst the land itself, including the salt (leaving eruptive rocks out
of the question), may be attributed to the ocean.

The author makes no allusion to what has become of the enormous
mass of solid materials which has been removed from the surface of
the drainage area of the Dead Sea, and carried into its basin. Some
of it is, of course, represented by the terrace deposits, but we can
hardly account for the rest, without supposing that the depression
of the Dead Sea has originally been much deeper than it is now,
and that it has been partially infilled.

In an appendix Mr. F. W. Rudler describes the microscopic,

structure of the specimens of crystalline rocks collected by Prof.
Hull in Arabia Petrezea.

The work is illustrated by two geological maps and by numerous
sections and profiles which show very distinctly the stratigraphical
relations both of Palestine itself and the Sinaitic peninsula,

ee

232 Reports and Proceedings—

Sees @ re as ASIN GS) eke © CS abr seat eee

GroLtocicaLt Society or Lonpon.

I.—March 24, 1886.—Prof. J. W. Judd, F.R.S., President, in the
Chair. The following communications were read :—

1. “On the Genus Diphyphyllum, Lonsdale.” By James Thom-
son, Hsq., F.G.S.

The author commenced by giving a definition of the genus Diphy-
phyllum, and then proceeded to discuss its relations with some
allied forms, such as Lithostrotion, Lithodendron, and Campophyllum.
Diphyphyllum was shown to be restricted in Scotland to the lower
portion of the Carboniferous system, and not to have survived the
great development of volcanic action in the upper part of the Car-
boniferous-Limestone series, whereas in Belgium and elsewhere the
range of this genus was more extensive.

It was shown that in Diphyphyllum reproduction took place both
by fissiparity and by calicular gemmation, examples of both forms
being cited. It was also pointed out that the development of central
vertical plates, showing a tendency to a passage into Lithostrotion,
was due to the corals having lived in a sea periodically affected by
the influx of sediment from the neighbouring shore.

After a history of the views held by different writers since Lons-
dale, and especially by M‘Coy, Milne Edwards and Haime, Hall,
Billings and De Koninck, on corals referred to this generic type, the
author gave a description of the species found in North Britain, ten
in number, of which seven were new; and after pointing out their
differences, showed that all exhibit a tendency to vary, and that, if
a sufficient series were available, a passage might be traced not only
between these different species, but between Diphyphyllum and the
various allied genera.

2. “On additional Evidence of the Occurrence of Glacial Con-
ditions in the Paleeozoic Hra, and on the Geological Age of the Beds
containing Plants of Mesozoic Type in India and Australia.” By Dr.
W. T. Blanford, F.R.S., Sec. G.S.

After recapitulating briefly the principal facts known as to the
correlation of the Karoo formation of South Africa, the Gondwana
system of India, and the Coal-measures and associated beds of
Hastern Australia, and especially noticing those phenomena in the
different strata that had been attributed to the action of ice, the
author proceeded to describe the additions recently made to previous
knowledge by various members, past or present, of the Geological
Survey of India, and especially by Mr. R. Oldham and Dr. Waagen.
These additions had recently been published in the Records of the
Geological Survey of India.

Mr. R. Oldham, in a recent visit to Australia, had come to the
same conclusion as all other geologists who had visited the country,
and clearly showed, as the Rev. W. B. Clarke and many others had
done, that beds containing Glossopteris, Phyllotheca, and Noggera-
thiopsis were intercalated among marine beds with Carboniferous

Geological Society of London. 233

fossils. The age of these marine beds was shown by Dr. Waagen
to be that of the European Coal-measures. Mr. Oldham, had how-
ever, further ascertained the presence in abundance of smoothed
and striated boulders, evidently transported by ice, in the marine
Carboniferous beds north of Newcastle, N.S.W., and he consequently
considered these beds, and not the overlying Hawkesbury, the
equivalents of the Bacchus-marsh beds of Victoria, and of the Tal-
chirs of India, a view which was in accordance with the relations
of the fossil flora.

Meantime Dr. Waagen had received from Dr. H. Warth some
fossils from the Salt-range of the Punjab. The fossils came from
the upper part of a boulder-bed, the resemblance of which to the
Talchir group at the base of the Gondwana system had long been
recognized, but which had hitherto been classed with a stage im-
mediately overlying, containing Upper Cretaceous fossils. The
fossils now found by Dr. Warth included two forms of Conularia
found in the Australian Carboniferous rocks, besides some other
species evidently of Carboniferous age. Dr. Waagen consequently
classed the boulder-bed together with other similar formations in
other parts of the Salt-range as Carboniferous. There was one
difficulty, the fossils just referred to were considered by Mr. Wynne
to be contained in pebbles derivative from another bed. It was,
however, shown that this did not affect the age of other boulder-
beds in the Salt-range, and that the latter were connected with the
Talchir beds in Central India by another discovery of Mr. R. Old-
ham’s that a boulder-bed in the Indian deserts was also probably of
Talchir age, and that the question as to whether the nodules con-
taining the Conularia, etc., were concretions or pebbles, might await
further examination in the field.

Another contribution to the question had been made by Mr.
Griesbach, who had recently found a boulder-bed which, from its
character and fossils, he considered as Talchir, in the neighbourhood
of Herat.

It was pointed out that the existence, over such extensive areas,
of boulder-beds, all of which might, without any improbability, be
of approximately the same age, rendered it highly probable that all
were really contemporaneous and due to one Glacial period ; that
this period must have been towards the close of the Paleozoic era,
which it may possibly have terminated by exterminating many of
the principal forms of life. The peculiar flora of the Australian
Newcastle beds and of the Indian Damudas, having nothing in com-
mon with the contemporaneous Kuropean Carboniferous flora, afforded
an important proof of distinct botanical provinces in past times.

II.—April 7, 1886.—Prof. J. W. Judd, F.R.S., President, in the
Chair.—The following communications were read :

1. “On Glacial Shell-beds in British Columbia.” By G. W.
Lamplugh, Esq. Communicated by Clement Reid, Hsq., F.G.S.

This paper was divided into two parts, relating respectively to
Vancouver Island and the Fraser Valley. Having to spend nearly a

234 Reports and Proceedings—Geological Society of London.

month at the city of Victoria in 1884, the author had leisure for the
investigation of the geological features of the district, but he expressed
his regret that, at the time, he was unacquainted with the publications
of Mr. Bauerman and Dr. Dawson on the subject.

The most important shell-beds were disclosed in an excavation for
a dry dock at Esquimault, V.I. Here a fissure in an igneous rock
had been filled in by glacial beds. Shells were most numerous on
the north side of the dock in Boulder-clay, associated with irregular
sandy seams, the whole being softer than the general mass. The
containing rock was not glaciated at this point. Leda, NVucula,
Cardium, Tellina, Mya, and Saxicava are the principal genera.

There was great difference in the state of preservation according to
position ; the shells below the water-line being remarkably fresh,
while acidulous waters, engendered by vegetable decay, had attacked
the upper portions.

The author concludes that the whole mass of drift, including the
shells, had been pushed up by ice in its passage southwards. The
general mode of occurrence was very similar to that at Bridlington.
He further observed that the rocks were not striated in the first
instance by these shelly clays, but he believed the glaciation to have
taken place through the action of harder substances, and that after-
wards a milder term set in, when an arctic fauna established itself in
the neighbourhood, after which fresh ice pushed the sea-bottom along
with other accumulations into its present position.

The shell-beds in the Fraser Valley are about 100 feet above sea-
level. Three sections of glacial beds were given. ‘The stratified
clay in which the shells were found contains no pebbles, and, though
somewhat disturbed, has evidently been deposited where it now
occurs.

2. “On a Lower Jaw of Macherodus from the ‘ Forest-Bed,’
Kessingland.” By James Backhouse, Esq., F.G.S.

The author believed that hitherto no example of a lower jaw of
Macherodus has been met with in this country; he consequently
gave a detailed description and measurements of a right mandibular
ramus obtained by him from the Forest-bed at Kessingland, in Suffolk.
Owing to the imperfect condition of the incisors and canines, it was
Impossible to say whether these teeth were serrulated or not, and
consequently it was uncertain whether the bone belonged to
Macherodus cultridens or M. latidens.

3. “A Contribution to the History of the Cetacea of the Norfolk
‘Forest-Bed.’” By H. Tulley Newton, Hsq., F.G.S.

This paper was principally devoted to the description of two fossil
specimens. The first of these was a tooth, shown by external and
microscopical characters to have belonged in all probability to the
Sperm-whale, Physeter macrocephalus. The specimen was obtained
by Mr. Clement Reid, at Sidestrand. ‘The second fossil, also from
Sidestrand, and now in the possession of Mr. James Backhouse, con-
sisted of the right half of the seven anchylosed cervical vertebra of
a species of Balena. The specific determination was less certain in
this case; but the form approached most nearly to that of B. biscay-

Correspondence—Major H. W. Feilden. 239

ensis. Of other vertebre from the Forest-bed, one, a caudal, was
referred to Balena ; another, from the lumbar region, to Balcenoptera.

The following specimens were exhibited :—

A series of Plant-remains from the Cromer Forest-bed, exhibited
by Clement Reid, Esq., F.G.S.

Specimens from the Shell-beds in British Columbia, exhibited by
G. W. Lamplugh, Esq., in illustration of his paper.

Specimens from the “ Forest-bed,” exhibited by James Backhouse,
Esq., and H. Tulley Newton, Hsq., in illustration of their papers.

(GO aS Sea HS SOUND Eas ae

—__@—_—__

ON THE DISTRIBUTION OF HIPPOPOTAMUS AMPHIBIUS.

Sir,—I have lately read with great pleasure Dr. Henry Wood-
ward’s interesting and instructive article, on “ Recent and Fossil
Hippopotami,” published in Dec. III. Vol. III. 1886, pp. 114-118,
of this Macazine. In that paper, Dr. Woodward assigns to the two
species of Hippopotamuses the tropical or warmer parts of Africa as
their present habitats. As a generalization of their present distribu-
tion, this statement may be accepted as strictly correct, but during my
journeyings in South Africa, in the upland regions of Natal, the
Orange Free State, and elsewhere, I was surprised to find some of
the reedy “vleys”’ or lakes called “‘ Leekoe Vley.” Such a name is
in itself evidence that the Boer immigrants, or early settlers, found
Hippopotamuses in such localities; indeed, I have been informed by
old settlers that such had been the case in their own knowledge, or
else that the natives bad told them of the former existence of the
animals in such places. I have been credibly informed that 50
years ago Hippopotamuses were abundant in the Umzinduzi river,
close to where now the city of Pietermaritzburg in Natal is built.
The fact of these animals having inhabited localities in the uplands
of Natal, and the Free State, is I think beyond question, and as those
districts are at times subjected to very inclement weather, it raises
the question whether the Hippopotamus amphibius is not capable of
enduring far greater changes of temperature than is usually
supposed. I was encamped in the vicinity of Newcastle, Natal,
on the borders of the Transvaal, in the winter of 1881 (i.e. the
summer of our northern hemisphere), and we experienced very
severe weather. Water froze in the buckets left outside the tents at
night, the snow lay deep over the country, herds of sheep and cattle
were buried and frozen to death in the snow. Many farmers
suffered great loss in stock. In the highlands of the Orange Free
State, across the Natal border, the losses of flocks and herds from
the snowstorms were greater than in Natal. The question arises,
whether Hippopotamuses were denizens of these upland lakes and
rivers, or only summer visitors. If residents, they must have been
subjected at times to extraordinary changes of climate. I regret
that during my residence in South Africa, I did not pay more
attention to this interesting subject.

236 Correspondence—Ur. A. B. Wynne.

I venture to send you this communication in the hope that it may
attract the attention of some naturalist in South Africa, of greater
experience than myself, as the subject is one of considerable interest
to the geologist.—I am, Sir, your obedient servant,

We ts, Norrouk, 2nd April, 1886. H. W. FErnpen.

DISCOVERIES IN THE PUNJAB SALT-RANGE.

Sir,—Since the abstract of my paper to the Royal Geol. Soc. of
Ireland on the subject of Dr. Warth’s discoveries in the Hastern
Salt-range appeared in the GroxtogicaAL Macazine for March, a
paper on the same subject by Dr. Waagen, of Prague, in the Records
of the Geol. Survey of India (vol. xix. pt. 1), has reached me.
Several points in this paper relate to the stratigraphy of the Salt-
range as interpreted in my Geological Survey Report, and one or
two especially touch portions of my paper referred to, and its
abstract.

With reference to these last, I may notice that certain of the
fossils to which IJ alluded as undetermined have now been fully
described by Dr. Waagen, and are referred to the Carboniferous, not
Devonian age, as I had been informed. Beyond accepting the
purely paleontological determinations of Dr. Waagen, I have little to
say: he gives his evidence, describing most of the species as new or
indeterminate, or requiring further comparison, and he appears to be
now satisfied as to their age. Their reference to the later period
tends to reduce the interest which the discovery of Devonian forms
would have possessed, on account of the absence of recognizable
Devonian rocks, in that or the adjacent country.

Dr. Waagen’s paper, however, differs from my own in describing
these fossils as having been found in concretions, not in pebbles, and
as occurring in situ in the Conularia layer. Upon this point rest
very extensive and important deductions, and it is one upon which
some uncertainty seems to have prevailed, leading both Dr. Warth
and Dr. Waagen to reconsider matters and to change their minds:
hence I am glad to learn we may expect to hear further about the
matter from the officers of the Geological Survey of India.

Dr. Waagen’s latest announcements, as above stated, seem to date
from the end of last year or the very commencement of 1886. Dr.
Warth, writing to me with specimens from this layer (and some others)
under date Dec. 1, 1885, strongly maintains that the fossils are not
in situ, but derived, and in support of this he calls attention to one
of the specimens, a single rolled fossil Conularia, which itself formed
one of the pebbles of the layer. Turning to the specimens I
received (and they were few), I found they consisted of fine. pale,
non-calcareous sandstone, presenting no signs of concretionary
structure, their smoothed surfaces intersecting the inclosed fossils,
while the special example referred to has all the appearance of a
once more perfect fossil detached from its matrix, abraded and rolled
till its general form alone remains, with just sufficient of its original
markings to show certainly what it is. Another of the same kind
shows only the outer form, and greater abrasion.

Correspondence—Prof. T. G. Bonney. 237

On this confirmatory evidence I adhere to the view expressed in
my paper as to the derived or remanié character of the Conularia
layer, until something more conclusive is brought forward than has
been yet produced.

The “ Olive group ” of the Salt-range which contains this Conularia
layer, from its circumstances of position and from a few of its fossils,
found in a determinable state, was classified by Dr. Waagen and
myself as probably of Cretaceous age, before he left the Punjab.

It has been recorded for years that certain Boulder-beds, lying
just beneath this Conularia layer, and included in the Olive group,
contain glaciated blocks, and resemble the Talchir Boulder-beds of
the Gondwana series in Peninsular India; also that there are in

other parts of the Range, and at different vertical positions in its

sections, Boulder-beds of very similar aspect.

I have never found reason to believe that the stratigraphic
relations of these Salt-range Boulder-beds supports the idea now
advanced, that all occur upon one and the same horizon; and I must
say I am still unconvinced of the fact, while admitting that this
would be both important and interesting if proved.

Kinestown, 19th March, 1886. A. B. Wynne.

THE PALZONTOGRAPHICAL SOCIETY.

S1r,—The fortieth volume of the Memoirs of the Paleontographical
Society is now in progress; with the current year the series will
have completed the number generally assigned to a period of pro-
bation. That it has well endured the trial of time none can deny.
The unremunerated labours of many of the leading paleontologists
of Britain have enriched their fellow-workers with a series of mono-
graphs, sometimes dealing with various genera or classes, some-
times presenting a synoptic view of certain portions of the fauna or
flora of an important Geological period. To these workers and to
all who have taken an active part in the direction of the Paleonto-
graphical Society, geologists, not of Great Britain only, are deeply
indebted. Never, we may confidently assert, has so magnificent a
series of admirably illustrated monographs been placed in the hands
of students or at so low a price. For an annual subscription of one
guinea, a bulky volume is received, containing usually about thirty
plates and three hundred pages of letterpress. At the present time
monographs are in preparation or in progress on Pleistocene
Mammals and Old Red Sandstone Fishes, on Jurassic Ammonites
and Gasteropods, on Cretaceous Starfishes, on Palzeozoic Sponges and
on the Flora, both of the Carboniferous and of the Hocene periods.
There is evidently no failure either in material or in writers. More-
over, up to the present time the Society has successfully paid its way
and has occasionally had a small balance to the good. Death how-
ever of late years has unfortunately removed many of the original
subscribers, and new members come in more slowly than might have
been expected. Accordingly the Secretary announced at the last
meeting of the Council that very shortly, unless there was a sub-
stantial increase in the number of subscribers, the quantity of matter

ee

_—

ae

—

238 Correspondence—Prof. E. D. Cope.

included in the annual volume must be reduced, and thus the issue of
the monographs delayed. This announcement is not altogether
creditable to the geologists of Great Britain. The number of persons
interested in the study of this science has not diminished, nay, has
become decidedly larger, since the foundation of the Palzonto-
graphical Society. Many more than those whose names are on the
list of subscribers could well spare the annual guinea needed to
secure the efficiency of the work, but it may be feared that there is
among them some lack of public spirit. The rapid development of
every branch of geology has perhaps contributed to this by render-
ing its students more of specialists than they formerly were; but
even if the number of monographs in the series bearing on this or
that man’s hobby be small, he is bound, I think, on public grounds
to see that this useful work does not languish for want of funds.
In almost every career of life there are certain associations to which
one feels bound to belong: may I then be forgiven for suggesting
that every geologist not absolutely impecunious should consider
the Paleontographical Society one of these. True, the number of
back volumes is now formidable to those who desire a complete set,
but these can be purchased on easier terms by subscribers, and the
less wealthy student may console himself for a broken series by the

thought that he is doing a good work in securing its continuance.
T. G. Bonney.

NOTES ON PHENACODUS.

Sir,—I must remark on your late article on Phenacodus! (Gxo-
tocicaL Macazine, No. 260), that having selected for publication
my earliest conclusions regarding it, issued in 1881, my more
mature views are not stated. In order to insure the dissemination of
the latter rather than the former, through your journal, I give the
following points.

A few months after the publication of the note from which you
have principally copied, I published a systematic analysis of the
Ungulata in the Proceedings of the American Philosophical Society
(1882), in which it was shown that the carpal bones in Phenacodus
are in linear and not alternating series, and that it therefore cannot
be referred to the Perissodactyla. With the Hyracoidea and other
forms having similar carpal and tarsal characters it was placed in an
order Taxeopoda. This order I regarded and still regard as ancestral
to all Ungulata, Amblypoda and Proboscidea included. It thus
realized, so far, the prophecy which I made in 1874 (Journal
Academy Philad.), that the ancestral type of higher Mammalia
would prove to be pentadactyle and bunodont. The history of this
question is set forth in my illustrated account of the Condylarthra
published in the “ American Naturalist” for 1884.

A further study of the extinct Taxeopoda has shown me that
although furnished with hoof-like unequal phalanges, they are not
very different from the Lemurs of the primitive type known as the
Adapide. I now believe that the order Taxeopoda must include

-1 See February No. pp. 49-52, Pl. II.

Correspondence—Ur. R. Etheridge, Jun. 239

not only Phenacodus and allies (=Condylarthra), but also Hyracoidea,
Lemuroidea, Simmopithecoidea, and Anthropoidea, although the
last-named diverge a little in the characters of the carpus. Moreover,
some of the Taxeopoda of the Puerco epoch show that the Ungui-
culate forms can readily have descended from them, for as the
carpus and tarsus of this order are thoroughly Unguiculate, it
only requires intermediate forms of ungues to connect them, and
these have been found. These facts and conclusions are set forth in
the ‘‘ American Naturalist ” for 1885, in a paper on the “ Evolution
of the Vertebrata Progressive and Retrogressive.”

It thus appears that Lemurine forms were the ancestors of all
Placental Mammalia, as was already anticipated by Haeckel in his
far-seeing ‘ Schépfungsgeschichte.” KE. D. Cope.

NOTE ON #RISICHTHE.

Srr,—A careful perusal of Mr. Davies’ note on this subject in your
number for March reveals the fact that he agrees with me in the asso-
ciation of the fin-spines in question with Hrisichthe, and not with
Ptychodus. He corrects me as to the authorship of the term Xiphias
Dizoni, and agrees with me again that the weapon of that species
also belongs to the fish I have called Hrisichthe. But he wishes me
to use the name Protosphyrena, Leidy, in the place of the one I
have proposed. In this point I hope Mr. Davies will yet again agree
with me.

Two species are catalogued! by Leidy under the name of Proto-
sphyrena, P. ferox and P. striata. If now his P. ferou be a species
of the genus I have named LHrisichthe, Leidy’s name should, in
accordance with all usage, be retained for the P. striata, provided
the two belong to different genera. When in London, in 1878,
either Mr. Davies or Mr. E. T. Newton showed me a jaw containing
teeth of the P. striata, which was plainly not an Hrisichthe. For
this statement I depend on memory alone. If I be correct, it is for
this genus that the name Protosphyrena should be retained, if it be
used at all.

In its present status, however, the name in question is nomen
nudum, and under the rules not more entitled to recognition than
new names in museum or sale catalogues. The rules of the
American and British Associations are explicit on this point, and
properly so. EK. D. Corr.

NOTOCHELYS COSTATA, OWEN.

Sir,—In his description of this interesting fossil,? Sir Richard
Owen stated that the “nature and age of the deposit from which it
came was unknown to him.” I am informed by Prof. Archibald
Liversidge, by whom Notochelys was sent to Prof. Owen, that it was
found associated with certain other fossils described * by myself from

1 The name is not referred to in the text of his paper by Leidy, but only appears
in a catalogue at the end of it.

2 Quart. Journ. Geol. Soc. 1882, vol. xxxviii. p. 178.

3 Journ. R. Soc. New South Wales for 1883 [1884], vol. xvii. p. 87.

240 Correspondence—Ur. F. G. Hilton Price.

the Cretaceous beds of Landsborough Creek, a tributary of the
Thomson River, such as Ancyloceras Flindarsi, M‘Coy, <Aucella
Hughendensis, Eth., sp., a probable Hamites and large Inocerami.
These would appear to indicate beds about the horizon of the
Marathon or Hughenden series of the late Mr. R. Daintree.*

R. ErueripGs, Jun.

THE LANDSLIP IN THE WARREN NEAR FOLKESTONE,

Sir,—It is only right that a record should be kept of the very
extensive landslip which occurred in the undercliff of the Warren
near Folkestone on the 19th January last, not only because few
know anything of the circumstance, but that it might be useful in
case of future investigations.

The area affected by this slip is very considerable, extending from
the Warren House, near the Martello Tower, eastwards to a spot
locally called the Jetty, a distance of nearly a mile in length and by
about a quarter or rather less in breadth. This undercliff is entirely
composed of rubble and débris from the Chalk cliffs above, which
have been falling and slipping over for centuries. This slip appears
to have taken a horizontal line from the seaward side of the railway
cutting, in fact, in some parts it started from the outside of the
actual railway bank. Hadit broken away a few yards further inland,
and there is no reason why it should not have done so, the passengers
by the South-Eastern would then realize the danger to which the line
is exposed. This large area gave way and went down bodily for a
depth of from 12 to 20 feet, varying in places; this had the effect of
forcing up the beds upon the shore several feet in height for about
amile of the coast. Towards the east end of the slip, the Chalk-
marl is raised nearly 20 feet. It is a remarkable coincidence that
since this happened, there have not been any heavy seas upon this
coast, consequently no further damage has been done; but when
heavy seas do come in, which they inevitably must, they will wash
away thousands of tons of the rotten rubble cliffs which, upon the
shore-line, are composed for the most part of débris from the cuttings
and tunnels, which when cleared away will give further impetus for
another and perhaps a more disastrous landslip to take place,

The whole floor of the shore is much raised, with here and there
a depression which is probably the level of the old shore. In one
place the Upper Gault is raised into a hillock several feet high.

The coming spring will afford an excellent opportunity for those
interested in Cretaceous geology to examine the Chalk-marl as it is
now placed. I may add, the whole of this area is constantly moving,
and another slip may occur at any moment.

F. G. Hinton Price,

13th April, 1886.

1 Quart, Journ. Geol. Soc. 1872, vol. xxviii. p, 279,

THE

GEOLOGICAL MAGAZINE.

NEWS SERIES? DECADES IIE VOR Til:
No. VI.—JUNE, 1886.

(Ouse aE y-CdI by NASR Orns

i
I.—On MareEKAnITE AND 1TS ALLIES.

By Professor Joun W. Jupp, F.R.S.,
President of the Geological Society.

bas almost every collection of minerals there may be found speci-

mens of the curious little glassy balls, which, from the locality
of their occurrence—the great Marekanka, near Okhotsk in Siberia—
have received the name of Marekanite. These glassy balls are more
or less perfectly rounded in form, they vary in their colour, through
different shades of smoke-grey to orange-brown, while in size they
range from the dimensions of a pea to those of a walnut. Most
mineralogical treatises still continue to recognize Marekanite as a
mineral, and class it either as a variety of Obsidian or of Pearlstone.

While totally disallowing the claim of Marekanite to rank as a
mineral-species or even variety—the petrographer recognizes in this
substance a type of rock, which proves to be by no means devoid of
interest, when its properties are carefully studied, nor destitute of
suggestiveness, when its mode of occurrence is thoughtfully considered.

Occurring as it does on a spot frequently visited by travellers, the
appearance and surroundings of Marekanite have been very fully
described ; among others by Steller, Laxman, Allegretti and Pallas ;
it was the last-mentioned naturalist who appears to have made the
rock widely known by sending specimens from St. Petersburgh to
most of the Museums of Europe.

The first mineralogist who seems to have expressed an opinion on
the nature of Marekanite was Sewergin, who in 1796 described it as
a “Glasszeolite.”1 To this conclusion he was probably led by
studying its behaviour with the blowpipe.

Lowitz and Gmelin made analyses of the substance,” and these,
though very imperfect, as might be expected from the early date at
which they were undertaken, showed the rock to contain a very high
percentage of silica with some alumina and a small proportion of the
alkalies and alkaline earths.

The author to whom we are however indebted for most of our
knowledge of the properties of this curious substance is Klaproth,

' Nova Acta Acad, Petropol. T. xii. (1801) p. 237.
2 Neue Nord Beitrag, vol. ii. p. 299.

DECADE IlI.—VOL. III.—NO. YI. 16

242 Prof. J. W. Judd—On Marekanite and its Allies.

whose memoir entitled ‘‘Chemische Untersuchung des Marekanits”’ *
was read before the Berlin Academy on the 15th May, 1812.

Klaproth showed that the Marekanite-balls were sometimes almost
colourless and translucent, at others dark-coloured and opaque; the
former he found to have a specific gravity of 2°365, the latter of
2:335. The composition of the two varieties he determined to be
as follows :—

Transparent Variety. Opaque Variety.

Silica Nor araestereco: elersecieiens STROO29 etree 76°50
PAU INIT ay ee rcieleloveneeinve ORSON | avetrsets 10°50
MAMNG eevee oaaiets cvotereter Seve ce OFF in TE tte 0°50
Tron Oxadey ee rereicicectereters S60 Ses 1:00
MP OLAS gaveinte aieralarevesteevareye DT OM eights 2°70
SOd ase era sntel arexets enatane aleve a 4°50 oi. wimieissevees 4°50
Undetermined constituent .. ht amma iets Aye 9°50
Waiter” dicate veycrierensierersteleiis ere OPO ers 0°50

99°13 98°70

No more recent analyses of the rock would seem to have been
published. Klaproth further showed that while many of these glass
balls resist a tolerably smart blow with a hammer, yet when they
do yield they break up into a mass of fine particles, hike unannealed
or toughened glass. He noticed, too, their singular behaviour when
heated, which will be described in the sequel.

Klaproth’s analyses show that Marekanite is an obsidian, and if
his separation of the soda and potash can be relied upon, which is
doubtful, we might conclude that it is a dacite- or quartz-andesite-
glass rather than a rhyolite- or quartz-trachyte-glass.

With the exception of some observations by Erman? and Herter,’
but little seems to have been added to our knowledge of Marekanite
since the time of Klaproth.

Professor Bonney informs me that the late Professor W. H. Miller,
of Cambridge, told him that Marekanite-balls had been known to
explode spontaneously. Mr. J. Gregory some time ago communi-
cated to me the interesting fact that a lapidary who had attempted
to cut a section of a Marekanite-ball found that during the operation
it flew to pieces with a slight explosion. Kalkowsky states that
many of the Marekanite-nodules, when struck with a hammer, de-
crepitate to dust.*

In these characters the balls of Marekanite appear to present
so many points of resemblance with the well-known “ Rupert’s
drops” that I thought it would be of interest to make a fuller
comparison of the natural and artificial substances.

In the first place, the more transparent varieties of Marekanite,
when examined between crossed Nicols, were found to depolarize the
light in a very striking manner, giving rise to the well-known appear-
ance presented by unannealed glass or glass when subjected to
mechanical strain. Compared with the appearances presented by

1 Berlin Abhandl. Physikal Klasse (1812—13), pp. 49—48.

2 Archiv. f. d. Wissensch. Kunde von Russl. iii. (1843), p. 175.
3 Zeitschr. d. d. Geolog. Ges. xv. (1863), p. 469.

4 ¢¢ Klemente der Lithologie ’’ (1886), p. 80,

Prof. J. W. Judd—On Marekanite and its Allies. 248

transparent Rupert’s drops between crossed Nicols, the Marekanite
was found to be precisely similar in its behaviour.

In the second place, ten nodules of Marekanite, varying in size and
colour, were selected for cutting by the lapidaries’ wheel; and their
behaviour, carefully watched, was as follows :—

One, the largest, was cut through without undergoing fracture.

Six, while being cut, had one or more cracks developed in them,
and the formation of these cracks was accompanied by distinctly
audible, snapping sounds.

In the remaining three cases, snapping sounds were heard from
time to time while the cutting was taking place, and when the mass
was nearly cut through, a distinct explosion occurred, the fragments
being thrown to the distance of several yards.

In the case of two Rupert’s drops, treated in precisely the same
manner, it was found that before the saw had passed half through
them, an explosion occurred, which was more violent than that accom-
panying the breaking up of the Marekanite-nodules. These facts
point to the conclusion that the glass of the Marekanite-balls is in a
condition of intense strain, in some cases approaching that which
characterizes the Rupert’s drops.

In the case of both the Rupert’s drops and the Marekanite-balls,
the portion left embedded in the cement after the explosion was
found to be traversed by a system of radial cracks, and on the
attempt being made to grind them they fell to pieces. The fine
splinters into which the Marekanite-balls broke up were found,
when examined by the microscope, to be quite similar to those
derived from the Rupert’s drops. Acting upon a suggestion made
to me by my colleague, Prof. F. Guthrie, F.R.S., I annealed some
of the Marekanite-balls by heating and slowly cooling them. They
were then found to have lost their power of depolarizing light, and
were easily cut and ground into thin sections.

I must now proceed to describe another set of remarkable
phenomena—those namely which are exhibited by the Marekanite-
nodules when they are heated.

If one of the balls be subjected to a gas-jet, blown by a moderately
strong air-current, it will be seen that, as redness is approached,
thin films of glass detach themselves from the surface of the ball
and these films are successively broken up into fine particles, so that
there is maintained a constant dispersal of excessively minute glassy
dust, which is thrown to a considerable distance. If the temperature
be now raised to whiteness, the whole mass swells up in cauliflower-
like excrescences, till it has attained eight or ten times its original
bulk. The resulting white mass is found to be a true pumice, which
floats upon water, and microscopic sections of it are indeed quite un-
distinguishable in appearance from many natural pumices. Some
of the Marekanite-balls, however, exhibit this property in a much
more striking manner than do others.

These experiments prove that the quantity of volatile ingredients
in these Marekanite-balls is very great, sufficient indeed, on being
liberated by heat,.to convert the obsidian into a pumice. Herter

244 Prof. J. W. Judd—On Marekanite and its Allies.

states that Marekanite loses on ignition from one to four per cent. of
its weight.

The last point to which I have to direct attention with respect
to Marekanite is its microscopic structure. This is found to differ
in a remarkable degree in the several varieties.

Some of the Marekanite-balls are almost colourless and perfectly
translucent. These, as pointed out by Zirkel,' are among the purest
of natural glasses, and are comparable to Fuleurite and Boutellen-
stein. From these translucent varieties we found every gradation
to the more opaque types which are of deep smoke-grey and orange-
brown tints, their opacity being evidently due to primary devitrifi-
cation.

Porphyritic crystals are rare, and of small size in Marekanite.
Those observed appear to be referable to hornblende, magnetite, and
a brown mica. Black trichites and reddish or yellowish-brown
globulites abound, the latter being usually drawn out by the move-
ment of the glass into cloud-like wisps, and the rock being very dis-
tinctly banded by the disposition of these in the mass.* In many cases
the commencement of a pumiceous structure is exhibited through
the abundance of cavities drawn out in the direction of the flow.
The Marekanite-nodules exhibit all the characters of a volcanic glass
undergoing incipient devitrification and exhibiting flow structure,
with occasionally the beginnings of pumiceous distension.

Now the peculiar characters of Marekanite seem to be capable of
simple explanation when we take into account its mode of occurrence,
which has been so clearly described by Erman and other writers.*

According to the information supplied from these different sources,
there occurs in the district around Okhotsk a considerable tract of
highly acid, igneous rock (rhyolite or quartz-andesite), which is
sometimes vesicular, at other times compact, and appears to be some-
times intrusive in strata containing Devonian plants. This rock is
generally stony in texture, but sometimes passes into “ hornstone-
like ” varieties ; while locally, as on the banks of the great Marekanka
brook, it assumes a more or less pefectly glassy condition. At the
locality mentioned, the igneous mass forms a cliff between 200 and
300 feet in height, the rock varying in colour from snow-white to
reddish-brown, and its different varieties constituting wavy bands,
which, as is so commonly the case with the vitreous lavas, simulate
the appearances presented by many crumpled, foliated rocks.? This
banded, glassy rock is seen to be traversed by numerous concentric
joints, so that globular masses breaking up like onions accumulate
in immense numbers at the foot of the cliff, forming a talus which
reaches half-way to its top. The nuclei of these concentric masses,

1 Mikroskop. Beschaff. der Mineralien und Gesteine (1873), p. 361.

2 See Wichmann, Zeitsch. d.d. Geol. Ges. xxxv. p. 849; Diller, Amer. Journ. Se.
Xxvili. p. 252; Rutley, Quart. Journ. Geol. Soc. vol. xli. (1885), p. 152.

3 Compare Zirkel, Mikroskop. Beschaff. der Mineralien und Gesteine (1873), p. 361.

4 Erman, Archiv. f. d. Wissensch. Kunde Russlands, iii. (1848), p. 175; Herter,
Zeitsch. d. d. Geol. Ges. xv. (1868), p. 459.

5 See Grou. Maa. Dec. I]. Vol. IL. pp. 68 and 69, Fig. 9.

Prof. J. W. Judd—On Marekanite and its Allies. 245

which vary in size from a pea to a fist, constitute the well-known
bodies usually called Marekanite.

A number of rocks have been described from other localities,
which in their peculiar characters or mode of occurrence appear to
closely resemble Marekanite.

In 1844 Damour gave an account of a specimen of obsidian,’
which was said to have been obtained from India, though its locality
could not be more precisely determined. It was spheroidal in form,
and about 21 inches in diameter; its colour was black by reflected
light and bottle-green by transmitted light, and it had a specific
gravity of 2-47. Unlike Marekanite, it was found to melt slowly
without expansion, and to form a colourless glass. This ball of
obsidian, while being cut by a lapidary, was found, when sawn through
to the extent of nearly two-thirds of its diameter, to emit a kind of
hissing sound, and this was followed by astrong detonation, the mass
being at the same time broken up into fragments, which were thrown
in all directions with considerable violence. The fragments when
collected were found to show a radiated structure like that seen in
the Marcasite-nodules of the Chalk.

The obsidian described by Damour was found by him to have the
following composition, so that it must be regarded as a dacite-glass.

Silica ... ves oe Sa 70°34
Alumina atte ane ae 8°63
Ferrous oxide... Ss ses 10°52
Manganous oxide Pe eas 0°32
Lime ... hae ute neh 4°56
Magnesia... poe coc 1:67
Soda ... AbD Sate wath 3°34

99°38

It is said not to have lost weight on ignition.

In 1824 the late Mr. Poulett Scrope described? an interesting
vein of green, porphyritic pitchstone with contorted banding, which
occurs at the Chiaja di Luna in the Island of Ponza; he showed that
the rock is made up of columns, each of which incloses a number of
globiform masses that break up concentrically like gigantic onions.
Mr. Scrope’s drawing of this remarkable rock-mass is reproduced in
the accompanying woodcut (see page 246).

In 1874 I had an opportunity of visiting this very interesting spot,
and noticed a remarkable property exhibited by this green rock ;
when struck with a hammer, it broke up with curved planes of
fracture parallel to the central nuclei; when freshly broken, the
surfaces showed a perfectly vitreous lustre, but within a few seconds
a most remarkable change was seen to take place over the glassy
surfaces thus exposed. They appeared as though breathed upon and
were gradually overspread by a whitish film, that looked like the bloom
upon a peach; this white film was found to be permanent, and in

1 Comptes rendus, vol. xviii. (1844), p. 46.
4 Trans. Geol. Soc. 2nd ser, vol. ii, p. 205, plate 24. See also Volcanoes, 2nd
ed. p. 105.

246 Prof. J. W. Judd—On Marekanite and its Allies.

consequence of its presence, specimens of the rock exhibit not the
vitreous lustre of obsidian, but the duller lustre of pitchstone.1

At the time when J made this observation, I thought that the
remarkable change in the surface of the rock might be due to
chemical action, and was the result of some kind of exudation on the
freshly-formed surfaces. But subsequent study of the surfaces with
the microscope, and discussion of the case with others, including
Prof. Bonney and also Dr. Guthrie, who has paid much attention to the
subject of the fracture of colloids, has convinced me that the change
is really mechanical, and one of a very peculiar kind.

Pitchstone Vei

Experimenting with colloid substances, like plate-glass and
Canada-balsam, I found that when relief from intense strain took
place by the breaking of a mass which had been bent, till it could
no longer resist the force applied, the fractured surfaces show a
dull appearance, which under the microscope is seen to be caused
by the wrinkling up of a thin film on the suddenly liberated
surfaces. These cases differ from the one described from
the Ponza Islands, in the circumstance of the appearance of the
wrinkled film apparently instantaneously, instead of after an ap-
preciable interval of time. But it is, I think, consistent with well-
recognized physical principles that the recovery of particles from
a condition of strain, which has been long maintained, should take
place more slowly than that which follows from a strain of short
duration.

The study of cases which we have been considering all point to
the conclusion that, besides the local strains so well known to occur

1 Grou. Mac. Dec. II. Vol. II. (1875), p. 308.
2 See Phil. Mag. ser. 5, vol. viii. p. 25.

Prof. J. W. Judd—On Marekanite and its Allies. 247

around the crystals in porphyritic glassy rocks, which have recently
been discussed by Mr. Rutley' and Mr. Waller,’ there are other
conditions of tension which affect much larger masses of natural
glass, and which are comparable in the degree of their manifestation
to those which are exhibited by the well-known Rupert’s drops.

This condition of tension appears to be manifested in two different
ways. In the case of the Marekanite-balls, and the obsidian from
India described by Damour, the molecules are in a state of such
unstable equilibrium that a jar, or an incision, is sufficient to bring
about that partial re-arrangement which leads to their breaking
up with more or less explosive violence. But in the case of the
Ponza rock, the relief of newly-formed surfaces from strain leads
to the separation of a thin, more or less wrinkled, film. A con-
nection between these two cases is perhaps established by the
experiment of submitting the Marekanite-balls to moderate heat, when
thin white films like those formed spontaneously on the surfaces
of the Ponza rock are seen to make their appearance.

The study of the mode of occurrence of these different rocks shows
that the condition of extreme tension belongs to the nuclei of per-
litic masses. It has long been recognized that the perlitic structure
is the result of contraction in a rock-mass, and in 1879 it was shown
by MM. Fouqué and Levy,’ and in 1880 independently by Mr.
Grenville Cole,* that this structure could be produced in colloid bodies
by artificial means.

It has long been known that some of the natural glasses contain
a considerable amount of water and other volatile substances, up to
as much, indeed, in some cases, as 10 per cent. of their whole weight.
It has often been asserted that the presence of a large percentage of
water is characteristic of pitchstones, and of a much smaller amount
of the obsidians. But the perfectly vitreous Marekanite-balls show
by their behaviour when heated that they contain a very large pro-
portion of volatile matter, and other similar exceptions to the supposed
rule might be adduced. It is probably true that volatile matters are
more likely to be retained within masses which have cooled down
while subjected to the pressure of superincumbent material; and
under the same conditions, that slower cooling would take place,
which would lead to the more abundant development of crystallites
and the acquirement of the mass of the resinous lustre characteristic
of pitchstone.

Now, so far as my experience goes, the glasses containing a large
amount of volatile materials have an abnormally low specific gravity.
If the water be slowly separated from the mass, it is scarcely con-
ceivable but that contraction should take place and the density rise.
The materials in which the perlitic structure has been artificially
produced—namely, precipitated silica and Canada-balsam—both con-
tain volatile matters, and it is during the gradual removal of these in
drying that the perlitic structure is produced. The spirally-curved

1 Quart. Journ. Geol. Soc. vol. xli. (1884), p. 340.
* Grou. Mac. Dec. IIL. Vol. II. (1885), p. 91.

3 Mineralogie Micrographique (1879), pl. xix. fig. 2.
4 Grou. Mac. Dee. II. Vol. VII. p. 116.

248 Prof. T. Rupert Jones and J. W. Kirkby—

cracks seen on the surface of American cloth in railway-carriages can
be accounted for in the same way.

These and many other facts, which I will not now adduce, have
led me to the conclusion that while the first series of straight cracks,
which often produce columnar structures in rocks, owe their origin
to the contraction which takes place during cooling, the secondary
systems of curved cracks, which give rise to the perlitic and similar
structures, are more probably due to the contraction which goes on as
the volatile materials which they contain are slowly separated from
them. I hope to adduce some further illustrations of this principle
on a future occasion.

IJ.—On CarpBoniFeRous OstTRACODA FROM THE GaAyToN Borne,
. NorRTHAMPTONSHIRE.

By Prof. T. Rupzert Jonzs, F.R.S., and James W. Kirxey, Esq.

(PLATE VII.)

HE Carboniferous Ostracoda here described are from the deep
Gayton Boring, near Northampton. Hand-specimens of the
rock, obtained by H. J. Eunson, Esq., F.G.8., were given to us by
R. Etheridge, Hsq., F.R.S., some months ago; and Mr. Eunson
kindly gave us another piece lately.

To explain the situation of the bore, as well as the position of the
Carboniferous strata in it, we quote as follows from Mr. H. J.
Eunson’s paper ‘On the Palaeozoic Rocks beneath Northampton,” in
the Quart. Journ. Geol. Soc. vol. xl. 1884, p. 485, etc.:

“The second trial took place near the village of Gayton, five miles
south-west of Northampton, not far from the Banbury-lane crossing
of the L. and N.-W. Railway, about two miles north-west of Blis-
worth Station (see Ordnance Map 52 §.W.). It was thought that,
under the known attenuation of the Trias westward, the Waterstones
could be found, if only the site selected was at a sufficient distance
beyond the Carboniferous rocks to have allowed the lower beds of
the Triassic series to be deposited near Northampton.

“This boring, 282 feet above sea-level, was commenced at the
junction of the Upper with the Middle Lias, followed by the Lower
Lias clays, the aggregate thickness of which was 581 feet.”

The White Lias and Rheetic beds, 36 feet thick, are described as
resting on a slightly eroded surface of the Triassic strata, which are
82 feet 6 inches thick. The lowest of these latter contained much
débris of Carboniferous rocks. These last began, in the boring at
699 feet, with the eroded Carboniferous Limestone. From about 31
feet 6 inches lower down was brought up a bluish-grey shale; and
from a little below that a greenish-grey shale. The former has yielded
the little fossils here described. The latter contains similar Microzoa.
The boring was continued into the Old Red Sandstone, and to a
depth of 994 feet, without getting the supply of water sought for.

The minute specimens under notice were obtained for us by Mr.
C. D. Sherborn by breaking and washing the rock in which they had
been imbedded. There is a fair quantity of them,—certainly a few

Geol. Mag. 1886. Deigade Ml Voli Pi Vil.

J. W.K. del. : WestNewman &Co.imp.
E.C Knight lith.

Carboniferous Ostracoda.

Carboniferous Ostracoda from the Gayton Boring. 249

hundreds. The majority are single valves; and all of them are
thick-shelled and have a robust appearance.

In the hand-specimens referred to we found—in the greenish-grey
shale (at 731 feet), a few Ostracoda, and numerous fragments of
calcareous organisms, chiefly of Serpule, some of Shells, and some
possibly Encrinital :—in the bluish-grey shale (at 730 feet), many
Ostracoda, besides numerous calcareous fragments as above.

In both shales the organic remains are crowded here and there
along irregular planes and in other groups.

For the lists of fossils in the associated beds see Quart. Journ.
Geol. Soc. Aug. 1884, pp. 487-8.

Remarks on the Species.

1. KirKBYA VARIABILIS, sp. nov. Pl. VII. Figs. 4a, 4b (type); 5a,
5b (var. a) ; 6, Ta, 7b (var. b) ; 8a, 8b (var. c).

The prevailing form among this little group of Ostracods is a
Kirkbya which has strong Beyrichian affinities. Some specimens of
it are scarcely to be distinguished from such unisulcate species of
Beyrichia as B. arcuata (Bean) ; but most examples show the valves
ribbed after the fashion of Kirkbya, in which genus we place it.

It varies much in relative length and height; some specimens are
nearly twice as long as high, others are only a fourth longer than
high, while some, indeed, are nearly as high as long. What may
be taken as the local typical form, being the most common, can be
described thus:

Suboblong in outline, height rather more than half the length,
dorsal border straight, ventral border convex, extremities rounded.
The more compressed end, which we take as the anterior,’ is more
perfectly rounded than the posterior, which projects above, and is of
less height than the other. Valves compressed in front, swollen
behind, with a transverse subcentral sulcus; this is crossed by a
strong longitudinal rib, which gives its lower portion the form of a
subcentral pit; traces (more or less strong) of another and lower
rib are usually present along the ventral convexity of the valve ;
and there is nearly always a narrow, sharp-edged rib near to, and
almost parallel with, the dorsal margin. The valves are thick-shelled
and the right is larger than the left, and overlaps it strongly along
the ventral and extreme margins. Seen from above almost lanceolate
in outline, with the greatest diameter behind. Surface smooth.
Length 35 to #5 inch.

Var. a. Figs. 5a, 50.

This is a shorter form, being only a fourth longer than high; with the
ventral margin more convex, and with the posterior extremity much
the highest. The sulcation and costal arrangement are the same,
and the right valve overlaps the other, as in the type form.

Var. b. Figs. 6, Ta, 7b.
This variety is short and high, like that just noticed, but the

1 This is the view we take now; but it was not followed throughout in a former
paper on Kirkbye, Ann. Mag. N. H. March, 1885.

250 Prof. T. Rupert Jones and J. W. Kirkby—

carapace is fully as high at one end as the other, the curve of the
posterior extremity forming a more obtuse angle with the ventral
margin, which is but slightly convex. The general outline is thus
more subquadrate than in the others.

Var. c. Fig. 8.

This is very like Beyrichia arcuata (Bean) in appearance, and we
were at first disposed to keep it apart from the present species, for it
shows no indications of the two stout ribs along the centre of the
valves, but it possesses the sharp dorsal rib or crest in full force.
This latter feature, and similar ventral overlap by the right valve,
together with the way in which the ribs become nearly obsolete in
other examples of variabilis, cause us to group it with this species.

From the number of specimens of this species obtained. from the
shale of the boring, it would appear to have been of gregarious
habit. Most of the specimens are single valves.

2. Kirxpya puicata, Jones and Kirkby. Plate VII. Figs. la, 18,
2, 3a, 3b.

K. plicata, J. and K. 1867, Trans. Geol. Soc. Glasgow, vol. ii. p. 221.

K. plicata, J. and K. 1885, Ann, Mag. Nat. Hist. ser. 5, vol. xv. p. 184, pl. iil.
fig. 9, 10a, 0.

Valves of this species are not rare among the Gayton Ostracods.
They differ a little from typical specimens; their outline is more
nearly oblong, the dorsal and ventral margins being almost parallel,
and the ends nearly alike. The two longitudinal ribs that traverse
the central portion of the valve are well marked, slope upwards
posteriorly, and are looped together forward (in most examples). The
subcentral pit or constricted sulcus is deep and placed anteriorly.
One of the specimens shows a finely reticulated surface; all the
others we have examined are smooth. The shell is thick; and the
length about 3; inch.

K. plicata is not a common species. It was first found in Car-
boniferous Limestone, at Backwell, Charterhouse, and Weston-super-
Mare, in Somerset. It has not been noticed elsewhere in England.
In Scotland it occurs at various localities of the Calciferous-Sandstone
Series ; and very rarely in beds in the lower portion of the Carbon-
iferous-Limestone Series.

3. ByrHocyPRIS SUBLUNATA, Jones and Kirkby, MS. Plate VII-
Figs. 9a, 9b, 9c, 10, 11.

This is a species well known to us, though as yet undescribed.
It was first sent us by Mr. James Bennie (Geological Survey of
Scotland), in a washing of shale from Staneshiel Burn, Roxburgh-
shire; also from another shale, at Tweeden Burn, in the same
county. Both these localities are in the Calciferous-Sandstone
Series. The species may be briefly described as follows :—

Carapace subtriangular or lunate in outline; tumid: with left
valve overlapping the right all round. Dorsal margin boldly and
almost evenly arched; ventral margin straight or slightly convex ;

Carboniferous Ostracoda from the Gayton Boring. 251

extremities pointed and nearly alike, though the posterior is rather
the most acute; seen from above ovate, with the greatest diameter
rather behind the centre. Within and a little below the margin of
each valve a thin sloping ledge or plate projects inwards, and is
most developed at the extremities (Fig. 10); surface smooth (finely
polished in examples from Staneshiel Burn) ; shell thick ; length
35 inch.

We refer this species to Bythocypris doubtfully. The over-
lapping valve appears to be the left, but it is difficult to speak with
decision on this point, both in this case as well as in some other
Carboniferous species. Were the right valve the largest, then
Macrocypris would apparently be the better genus in which to
lace it.

: It is a comparatively common form among the Gayton Ostracods,
occurring both as single and united valves. Individuals show some
differences in relative length and height. Fig. 11 represents one
of the longest of them, and rather suggests relationship with
another Lower-Carboniferous species—Argillecia equalis, J. & K. MS.

Cythere? lunata, J. & K. (undescribed), from the Carboniferous
Limestone of Holwell, Somerset, has some resemblance to the pre-
sent species, though larger; and it may probably be a related form.

4, Macrocypris Jonusiana, Kirkby. Plate VII. Fig. 12.

Bairdia Jonesiana (Kirkby), 1859. Ann. and Mag. Nat. Hist. ser. 3, vol. il.
p: 432, pl. xi. figs. 1, 2.

Fig. 12 represents a specimen that comes nearer to this species
than anything else we know. The dorsal margin is not so regularly
arched as in B. sublunata, the posterior slope being longer and
flatter than the anterior; and the anterior extremity is broadly
rounded, while the posterior is subacute. We refer it to M. Jonesiana,
with some doubt.

5. CYTHERELLA EXTUBERATA, Jones and Kirkby. Plate VII. Figs.
13a, 186, 13e, 18d.

Leperditia Okeni (Minster), var. extuberata, J. & K. 1880, Quart. Journ. Geol.
Soc. vol. xxxvi. p. 588.

This species was discovered by one of us several years ago in the
Calciferous Sandstones of Fifeshire. It was then considered to
belong to Leperditia, and to be probably a variety of the common
Carboniferous species, Z. Okeni (Miinster). This opinion was arrived
at by a study of specimens imbedded in the matrix, only partially
showing external characters, and by our taking the straight edge as
the uppermost or dorsal margin.

Some years after this we received examples of the same fossil
from our friend, Mr. James Bennie, who collected them from the
Calciferous-Sandstone shale, at Staneshiel Burn, already mentioned.
These specimens were, in many cases, single valves, finely preserved,
showing the interior; and from these it is evident, owing to one
valve being much larger than the other, and from it having an
internal marginal groove for the reception of the smaller valve, that

252 Prof. Jones & J. W. Kirkby—Carboniferous Ostracoda.

the species is more nearly related to Cytherella’ than to Leperditia.
To that genus then we refer it; and in doing so we consider that
the convex edge is the back, thus bringing the large valve to
the right hand, and the more compressed or narrowest half of the
carapace to the front as the anterior portion, and so have it in
harmony with what is to be observed in other Cytherelle.

From the Gayton specimens we give the following provisional
description, with the intention of noticing the species more fully on
another occasion.

Carapace subovate in outline; dorsal margin arched and highest
about the posterior third; ventral margin straight or faintly
incurved; extremities rounded, the posterior obliquely so; the
hinder third much higher than the anterior; the carapace is tumid
and high behind, compressed and low in front. The left valve is
much smaller than the right; not much more than half as high as
long, while the right is two-thirds as high as long; the right valve
overlaps the left round the whole of its margin. Viewed from above
the profile of the carapace is subovate, widest behind, pointed in
front. End view oval. It is rather thick-shelled; the surface is
smooth. Length > inch.

The only other English locality for this species is Skellygate,
Northumberland, where it occurs in a shale of the Lower-Carboni-
ferous Series. ;

6. CYTHERELLA ATTENUATA, Jones and Kirkby. Plate VII. Figs.
14a, 146, 14c.

Leperditia attenuata, J. and K. 1880, Quart. Journ. Geol. Soc. vol. xxxvi. p. 588.

One or two examples of another form, also formerly referred by
us to Leperditia, occur with the other specimens from Gayton. It is
often found along with C. extuberata in Fife, and, like the latter, it
probably belongs to Cytherella. Indeed, we are not sure that the
relationship may not be closer to the species just described, for it is
possible that the differences observed may be due to sex. These
differences consist chiefly in the somewhat neater form of attenuata,
in the less strong (though still complete) overlap of the right valve,
and in the lateral contour, when seen from above, being more
regularly lenticular, the ends being almost alike, and the greatest
diameter being near the centre. In this latter character it certainly
looks very different from C. extuberata, and for the present we leave
it a distinct species.

There are thus six recognizable forms, or species, among the
Ostracods from the Gayton Boring, namely—
Kirkbya variabilis, sp. nov. Macrocypris Jonesiana (?), K.
K. plicata, J. and K. Cytherella extuberata, J. and K.
Bythocypris sublunata, J. and K., MS. C. attenuata, J. and K.
Five of these were previously known to us from other localities ;
and one, which is the most abundant, is new. Of the former, all of
them are essentially Lower-Carboniferous forms, being most com-

1 See Monogr, Carbonif. Entom, Pal. Soc. 1884, p. 58.

A. Smith Woodward—On the Genus Notidanus. 253

monly found in the Calciferous-Sandstone Series of Scotland, and the
more or less equivalent Carboniferous Limestone of England. Three
of them, indeed,—B. sublunata, C. extuberata, and C. attenuata,—have
not occurred above the Calciferous Sandstones; and the other two
do not range higher than the lower portion of the Carboniferous-
Limestone Series of Scotland; that is, speaking of the Carboniferous

rocks only, for it should not be forgotten that M. Jonesiana is a
Permian species.

EXPLANATION OF PLATE YVII.
(The specimens are magnified about 25 diameters.)

Fig. 1-3. Kirkbya plicata, J. and K.; 1a, left valve; 14, view of ventral edge;

fig. 2, right valve; fig. 3a, left valve, showing reticulated surface ;
36, end view.

Fig. 4-8. K. variabilis, sp. nov. ; 4a, carapace, right valve outwards; 44, ventral
view; 4c, end view; fig. 5a, carapace, right valve outwards; 50,
ventral view ; fig. 6, left valve; fig. 7a, carapace, left valve outwards;
76, end view ; 8a, carapace, left valve outwards ; 84, ventral view.

Fig. 9-11. Bythocypris ? sublunata, J. and K.; 9a, carapace, right valve outwards ;

95, ventral view; 9c, end view ; fig. 10, interior of left valve; fig. 11,
left valve.

Fig. 12. Macrocypris Jonesiana ? Kirkby; right valve.

Fig. 13. Cytherella extuberata, J. and K.; 18a, carapace, right valve outwards;
134, left valve; 13c, dorsal view; 13d, end view; 13¢, interior of
right valve. Fig. 13¢ is from Staneshiel Burn, Roxburghshire.

Fig. 14. C. attenuata, J. and K.; 14a, carapace, left valve outwards; 142, ventral
view; 14c, end view.

II].—On tHe PatmontoLoey oF THE Senacutan Genus WVoripawus,
CUVIER.

By A. Smrra Woopwarp, F.G.S.,
of the British Museum (Natural History).

(Continued from page 217.)

F the upper dental series, Probst’ attempts to give a tolerably com-
plete account, but it is only illustrated by very imperfect wood-
cuts. Two of the foremost awl-shaped teeth are figured by Lawley
(l.c. figs. 2, 3), and the same author ascribes to the upper jaw of this
species three other of the Pliocene specimens. Fig. 19 represents an
anterior upper tooth from the Middle Eocene of Hampshire, and
the original of Fig. 20 is another from the Miocene of Baltringen,
Wirtemberg. The former (B. M., p. 4707) exhibits a short thick
base with an oblique principal cone, in front of which are a number
of minute denticulations ; posteriorly there is only one secondary
cone, pointing sharply backwards, and about half the size of the
principal cone ; and this is followed by another small denticle. The
second specimen (B. M. 85533) has alsoa short thick root, and shows
a somewhat similar crown ; the large principal cone is followed by
one small secondary and a terminal denticle, and in front there are

* In his first paper (“‘ Ueber das Gebiss des Notidanus primigenius, Ag.” Uc.) : in
1879 the author expressed doubts as to the accuracy of his previous work, but it is

not improbable that all the specimens at first figured may belong to the species under
consideration.

254 A. Smith Woodward—On the Genus Notidanus.

a few coarse serrations at its base. To a position somewhat further
back in the upper jaw may also be referred the tooth represented in
Fig. 21; this was obtained from the Red Crag of Woodbridge, and
is preserved i in the Reed Collection of the York Museum.

N. primigenius is perhaps the most widely distributed of all the
extinct species of the genus, and is especially noteworthy on account
of its considerable size. It is much larger than N. serratissimus, and
its lower teeth also differ from that species in having more secondary
cones, and in possessing finer anterior serrations, which are not
recular, but decrease from above downwards. With the exception
of a brief notice by myself,’ there appears to have been no record
hitherto of the occurrence of the species in Britain, but, as already
stated, the originals of three of the figures illustrating this descrip-
tion have been obtained from English deposits, and are derived
from the Middle Hocenes of Barton and Bracklesham, and the Red
Crag of Suffolk. It is not known to occur in the London Clay.

On the Continent there are numerous allusions to teeth of this
specific type, from the Oligocene and Miocene, and the British
Museum also contains specimens from the Hocene of Klein Spau-
wen, in Belgium. A single tooth has likewise been described by
Gibbes from the Eocene of Richmond, in Virginia, and shows that
this species extended into the New World in early Tertiary times :
it would be unsafe at present, however, to regard all the notices of
NV. primigenius as correct determinations, although the analogy of
other fossil sharks is far from rendering improbable so wide a range
in time and space as has already been assigned to it. Winkler
mentions specimens from the Middle Oligocene of Belgium ; Rouault
and others record the species in France; Orueta in Spain; Adams
in Malta; Lawley in Italy (Pliocene) ; and the references to German
specimens are far too numerous to mention.

15. N. repens, Probst.
1879. WV. repens, J. Probst, Wiirttb. Jahresh. vol. xxxv. pp. 163-166, pl. iii.
figs. 18-22.

Founded upon some small teeth from the Miocene of Baltringen,
Wiirtemberg. The cones are all extremely low, and were perhaps
eight in number in the lower teeth, with large anterior serrations :
the specific identity of all the specimens figured appears somewhat
doubtful.

16. N. srserratus, Miinster.
1842. N. biserratus, Graf von Minster, “ Beitr. Petref.’’ pt. v. p. 66, pl. xv. fig. 9.

This species was founded upon a small tooth from the Oligocene
of Neudorft in the Vienna Basin, but does not appear to have been
recorded since its original description. The principal cone is about
four times the size of the largest of the secondary cones, and the
latter are no less than twelve in number. The eight anterior cones
are distinctly serrated on both edges.

1 Smith Woodward, “‘ Chapters on Fossil Sharks and Rays.—II.,’’ Science Gossip,
vol. xx. (1884), pp. 229, 280.

A. Smith Woodward —On the Genus Notidanus. 255

17. N. Loozr, Vincent.
1876. WN. Loozi, G. Vincent, Ann. Soc. Malacol. Belgique, vol. xi. p. 126, pl. vi. fig. 5.

I am indebted to Mr. G. F. Harris for the reference to M. Vincent’s
description of a fragmentary tooth of Notidanus under the specific
name of N. Loozi. The specimen in question was obtained from the
Lower Landenien (Thanet Sand) of Belgium, and exhibits nothing
beyond the anterior portion of the crown: it indicates a species
about the size of N. primigenius, and it is distinguished from the
tooth of this well-known form by the peculiar shape of the cones,
and the very large denticulations in front. Notwithstanding its im-
perfect character, the type-specimen appears to justify the author’s
conclusions.

18. N. Tareront, Lawley.
1877. WN. Targionit, R. Lawley, Atti Soc. Toscana Sci. Nat. p. 71, pl. ii. fig. 3

A small species founded upon lower teeth from the Pliocene of
Tuscany. ‘The type specimens are evidently very similar to the
mandibular teeth described above as immature examples of J.
serratissimus.

19. N. ereas, Sismonda.
1857. NV. gigas, E. zeman, Mem. R. Accad. Sci. Torino, ser. 2, vol. xix. p. 460,
fig. 13.
TUS b Ow LSP ae Lawley, Atti Soc. Toscana Sci. Nat. p. 68, pl. i. fig. 6.

A species allied to N. primigenius, but with the lower teeth re-
latively ionger, the cones less regular, and the anterior serrations
of the crown more pronounced. Occurs in the Miocene of Mondovi,
Piedmont, and the Pliocene of Volterrano, Tuscany.

It is interesting to be able to add that teeth undoubtedly referable
to this species have also been obtained from the Pliocene of Britain.
Through the kindness of Mr. Reed, the Hon. Curator in Geology,
and Mr. Noble, the Hon. Secretary, of the York Museum, I have
had the opportunity of examining the beautiful series of Crag Noti-
danidz in the Reed Collection of that institution, and among these
there is a very perfect crown of JV. gigas, shown in the accompany-
ing woodcut (Fig. 1). The specimen has been considerably rolled

Fig. 1.—Tooth of Notidanus gigas, Sismonda. Red Crag, Suffolk.

[Reed Coll., York Museum. ]
and abraded, so that the anterior serrations are scarcely visible, and
the root is wanting, but it is otherwise a most typical example. An
upper side tooth in the same collection may also perhaps be asso-
ciated with this form.

20. N. Menrcuinu, Lawley.

1877. MN. Meneghinii, R. Lawley, Atti Soc. Toscana Sci. Nat. p. 72, pl. ii. fig. 4.

Some large mandibular teeth from the Pliocene of Volterrano,
Tuscany, have been described by Lawley under this specific name.

256 A. Smith Woodward—On the Genus Notidanus.

The principal cone is relatively large, and is followed by ten to
twelve secondary cones; at its base the enamel of the crown ex-
tends far down upon the root, and the long anterior border thus
produced is strongly serrated for quite two-thirds of its extent.

A tooth of this species from the Red Crag of Woodbridge is also

Fie. 2.—Tooth of Notidanus Meneghinii, Lawley. Red Crag, Suffolk.
[Reed Coll., York Museum. ]

preserved in the Reed Collection of the York Museum. It is shown
of the natural size in the woodcut (Fig. 2). An anterior upper
tooth from the Red Crag of Bawdsey is also perhaps referable to
the same form.

21. N. D’Anconm, Lawley.
1877. NN. D’ Ancone, R. Lawley, loc. cit. p. 73, pl. ii. figs. 1, 2.

A small species. The teeth consist of four to six acute cones, the
first or principal cone being very large compared with the others,
and the anterior edge is serrated for a considerable length. Itisa
rare form in the Pliocene of Volterrano and Orciano Pisano, Tuscany ;
and Probst’ also describes some teeth from the Miocene of
Baltringen, Wiirtemberg, under the same specific name, but this is
a very questionable determination.

22. N. propLematicus, Lawley.
1877. WN. problematicus, R. Lawley, loc. cit. p. 74, pl. iii. figs. 3, 4.

This is a very doubtful species founded upon an upper tooth from
the Tuscan Pliocene, and merely named—as the author states—to
call attention to the peculiar specimen figured.

23. N. anomatz, Lawley.
1877. NV. anomale, R. Lawley, Joc. cit. p. 74, pl. ii. fig. 5.

If the mandibular tooth figured by Lawley as the type of this
species is genuine—as seems probable, notwithstanding the fracture
across its middle—it represents the largest member of the genus.
hitherto recorded. There are no less than 14 secondary cones, and
the tooth measures more than five centimetres in total length. The
principal cone and the three following are curiously contorted—
though it is possible that this may be an abnormal condition—and
the anterior edge of the first is strongly denticulated. An upper
tooth is also figured (pl. iii. fig. 6) which may perhaps belong to the
same form. Both are from the Pliocene of Tuscany.

1 J. Probst “Beitrage zur Kenntniss der fossilen Fische aus der Molasse von
Baltringen,” Wiirttb. Jahresh, vol. xxxv, (1879), pp. 166—169, pl. iii. figs, 6—11.

A. Smith Woodward—On the Genus Notidanus. Dom

Such is a brief enumeration of the various specific types of fossil
Notidanide that have hitherto come under my notice. One other
form has also been assigned to this genus by Winkler,’ under the
name of JV. Orpiensis, but this is apparently an erroneous determina-
tion: the type-specimens are from the Thanet Sand (Heersien) of
Orp-le-Grand, Belgium, but only one (l.c. fig. 15) seems referable to
Notidanus, and that is too imperfect to name specifically.

And now, in conclusion, there are one or two general considera-
tions suggested by the foregoing facts to which it may be interesting
briefly to refer. On examining the various forms of teeth in strati-
graphical order, it is at once evident that there are distinct traces of
specialization. In the earliest Jurassic types hitherto known, with
a single exception (N. serratus), the secondary cones are only two,
three, or four in number, while most members of the genus of Cre-
taceous and Tertiary age possess at least six or seven in the lower
teeth, and one Pliocene species (N. anomale) has been recorded with
no less than fourteen: it is also noteworthy that some of the Jurassic
teeth are characterized by the absence of anterior serrations on the
principal cone. Again, it is interesting to observe that the very deep
compressed fibrous root of the more recent Notidanide only began
to assume its peculiar characters towards later Cretaceous times, the
base in such species as N. serratus and NV. Daviesii being compara-
tively thick and depressed, and very suggestive of that of Hybodus.
The earliest species of Notidanus, indeed, have teeth so remarkably
similar to those of certain Hybodonts, that not only did Phillips—
as already stated—figure two specimens under the name of Hybodus
polyprion, but at least one other paleontologist? appears to have
made the reverse mistake. A careful study of a large series of
specimens of the well-known Stonesfield species results in the dis-
covery of some teeth that may almost be regarded as links between the
two. The originals of Figs. 1,2, Pl. VI., for example, are such forms
as would-be commonly associated with Hybodus polyprion, but a very
slight modification is necessary to convert them into most typical
Notidanid, and I have considerable doubts as to the propriety of
placing them with Hybodus at all. To transform a long-coned
Hybodont tooth into one of Votidanus, it is only necessary to assume
lateral compression and the reduction or loss of the anterior secondary
cones, and the teeth represented in Figs. 1 and 2, Pl. VI., exhibit a
marked approach to this condition. Fig. 1 showsa large, compressed
principal cone, preceded by four secondary cones, and followed by
two others, the former being reduced to quite small denticles, while
the latter are comparatively well developed : the front edge of the
principal cone is distinctly denticulated for half its length, and so
also is the first secondary ; and there are traces of vertical wrinkles

1 T, C. Winkler, “‘ Mémoire sur quelques Restes de Poissons du Systéme Heersien,’’
Archiv. Mus. Teyler, vol. iv. fasc. i. pp. 12, 18, figs. 13-17.

2 E. Favre, ‘‘ Description des Fossiles du Terrain Oxfordien des Alpes Tribour-
geoises,’ Mém. Soc. Paléont. Suisse, vol. iii. (1876), p. 16, pl. 11. fig. 1. The tooth
is described as Notidanus sp., but the figure agrees much more closely with that of a
species of Hybodus.

DECADE III.—VOL. III.—NO. VI. 17

258 A. Smith Woodward—On the Genus Notidanus.

at the base of the crown. Fig. 2 is a smaller but very similar tooth,
and the characters of both these specimens are such that they might
well be looked upon as closely allied to ancestral Notidanide, even
if not actually upon the main line of descent of this family.

Another interesting fact worthy of consideration is the distinct
evidence of wear already noted in the dentition of the N. eximius of
Schnaitheim (p. 210) ; it is impossible to conceive of this taking place
in Sharks that have the teeth so loosely attached to the jaw, and so
frequently replaced as are those of the living Notidanide, Lamnide,
Carchariide, etc., and I have never observed the peculiarity either
in the Recent, Tertiary, or Cretaceous forms. The circumstance is
very suggestive, indeed, of the oldest Notidanidz having the teeth
as firmly implanted as those of the Hybodonts, in which there were
two or more rows in function at a time, and in which also the longest
cones often show most evident traces of abrasion. The shape of the
root is quite in accordance with this supposition. It is proper to
add, however, that I have met with no very decided abrasion among
the large series of British Museum specimens of 1. polyprion, which
seem most nearly to approach Wotidanus, although this fact may be
partly accounted for by the considerable rolling to which many of
the teeth have been subjected before entombment in the Stonesfield
Slate; the cones of the Carboniferous Cladodus are often much worn
down, and so likewise are those of the long-coned species of Hybodus
in the Muschelkalk.

As to the precise significance of these various points of similarity
between the Hybodonts and the primitive Notidanide, it would be
unsafe at present to express any definite opinion. Hxcept in the
structure of the skull, which is very similar,’ the latest members
of each family exhibit many important differences. The Hybodonts
have two (spinous) dorsal fins, and at least since Jurassic times the
. Notidanidze have possessed only one; in the last of the Hybodonts,
moreover, there are well-calcified vertebra, while so advanced a
stage is far from reached in the living Notidanide. I have likewise
been able to determine that the Wealden species of Hybodus only
possessed five branchial arches; and there are also other points of
divergence to be taken into account. When, however, more is
known of the anatomy of the earliest Mesozoic forms, it may still
be possible to show that the evidence of the teeth is not altogether
misleading, but that even if the Notidanidz are not an early offshoot
of the Hybodontide, they are at least derived from the same primi-
tive stock.

EXPLANATION OF PLATE VI.
Fie. 1. Tooth commonly referred to Hybodus polyprion, Ag. Great Oolite, Bath,
B.M. (e. 2186.)
2. Tooth commonly referred to Hybodus polyprion, Ag. Great Oolite, Stones-
field. B.M. (35494.)
3. Si Een we Wagn. ; lower tooth. Corallian, Schnaitheim. B.M.
(85763.

1 Smith Woodward, ‘‘On the Relations of the Mandibular and Hyoid Arches in
a Cretaceous Shark (Hybodus dubrisiensis, Mackie),’”’ read before the Zoological
Society, April 20th, 1886.

9

”

Professors Heim & Penck—Glaciers of the Isar and Linth. 259

Fie. 4. Notidanus eximius,Wagn. ; lower tooth, outer view. Corallian, Schnaitheim.
B.M. (35763 a.)
» 9. Notidanus eximius,Wagn.; upper tooth, inner view. Corallian, Schnaitheim.

B.M. (22500.)

» 6. Notidanus sp. ; upper tooth, outer view. Corallian, Schnaitheim. B.M.
(22502)

», 1. N. serratus? Fraas; upper tooth, outer view. Oxfordian, Scarborough.
B.M. (35667.)

» 8. N. Daviesii, A. 8S. Woodw.; lower tooth, outer view. Oxfordian, St.
Clement’s. Oxford Museum.

» 9. Notidanus sp. Oxfordian, St. Clement’s. Oxford Museum.

», 10. WN. microdon, Agass.; anterior upper tooth, outer view. Chalk, Norwich.
B.M. (24927.)

», ll. WV. microdon, Agass.; upper tooth, outer view. Chalk, Sussex. B.M. (4164.)

» Kent. B.M. (44580.)

” 9) 9 99
ap 8% Re 5 lower ,, Pinner ,, » Norwich. B.M. (24928.)
» 14, va sp ‘s yy Outer 5, 96 » B.M.(35648.)
Pela: ee A i a a AS ie » B.M.(48950.)
», 16. NM. lanceolatus, A. S. Woodw.; upper tooth, inner view. Gault. B.M.
P. 1227.
ee fig ele ee In S. Woodw. ; upper tooth, outer view. L. Greensand,
Amuri Bluff, New Zealand. B.M. (Pp. 2303.)
», 18. N. dentatus, A. S. Woodw.; lower tooth. outer view. LL. Greensand,
Amuri Bluff, New Zealand. B.M. (P. 2303 a.)
» 19. N. primigenius, Agass.; anterior upper tooth, inner view. M. Eocene,

Hampshire. B.M. (P. 4707.)

» 20. N. primigenius, Agass.; anterior upper tooth, outer view. Miocene,
Baltringen. B.M. (35533.)

» 21. WN. primigenius, Agass.; anterior upper tooth, outer view. Red Crag,
Woodbridge. Reed Collection, York Museum.

» 22. NN. primigenius, Agass. ; lower tooth, outer view. M. Kocene, Barton
Cliff. B.M. (e. 1224.)

», 23. N. serratissimus, Agass.; tooth, outer view. London Clay, Sheppey.
B.M. (24618.)

» 24. N. serratissimus, Agass.; young tooth, outer view. London Clay, Sheppey.
B.M. (28890.)

», 25. N. serratissimus, Agass.; lower tooth, young, inner view. London Clay,
Sheppey. ' B.M. (30550.)

» 26. WV. serratissimus, Agass.; lower tooth, young, inner view. London Clay,
Highgate. B.M. (43133.)

[B.M.= British Museum. All the figures are of the natural size. ]

ITV.—On tHE District or tHE ANcIENT GLACIERS OF THE ISAR
AND OF THE LINTH.

By Prof. Atpert Her, of Zurich, and Prof. ALBrecut Prnck, of Vienna.!

N order to interchange our views, and arrive at a common under-
standing on the question of the connection of glaciers with the
formation of lakes, we undertook a joint excursion in Upper Bavaria,
in the district of the Ammer Lake, Wuerm Lake, Staffel Lake, and
Rieg Lake, and later, in the month of September, we visited together
the shores of the Lake of Zurich, partly accompanied by Dr. K. I.
V. Steenstrup, of Copenhagen, Dr. A. Wettstein and Dr. EH. Brueckner,
of Hamburg. We have drawn up a short protocol, both on the facts
observed and of our views respecting them, which we here propose
to communicate.

1 Translated from the authors’ MSS., by Dr. G. J. Ilinde, F.G.S.

260 Professors A. Heim and A. Penck—

I.—The Division of the Quaternary Formation in the District of the
Highland Lakes of Bavaria.

Throughout the lake district of Upper Bavaria, the basement bed
is everywhere formed by the ‘“ Flinz” (Upper Miocene Clay, Marl,
and Clayey Sandstone), on which rest the Quaternary beds, which
are briefly characterized below.

(a.) A layer of Conglomerate (Nagelfluh) from 20 to 30 métres in
thickness, having a nearly even surface, and rising with remarkable
uniformity in a gentle slope towards the 8. and §.W. It consists of
pebbles of limestone and dolomite, and contains very few erratics of
Archean rocks. The material is fairly evenly rounded, and united
by a calcareous cement. Hollow boulders and decayed pebbles are
abundant in it.

(b.) A deposit of gravel which may readily be distinguished from
the Conglomerate (a) or ‘“ Deckenschotter,” by the greater irregu-
larity in the size of the pebbles, and the far greater abundance of
pebbles of Archzean rocks. It is seldom cemented into a conglomerate,
it contains no hollow boulders, but there are in it rolled fragments
of the diluvial Nagelfluh mentioned above (a). This gravel deposit
is the Lower “ Glacialschotter ” of Penck (Die Vergletscherung, ete.,
p. 142). It is also of great uniformity and is widely distributed.
Its general dip from south towards the north is less than that of the
diluvial Nagelfluh (a), so that in the lake district to the south it is
deposited lower on the slopes of the valleys (which consist of
Miocene Flinz) than the Nagelfluh (near Weilheim 100 m.), whilst
towards the north, near Munich, it overlies the Nagelfluh.

Here, in the Isar Valley above Grosshesselohe, an intermediate,
independent deposit of gravel (intermediate Schotter, Penck, Die
Vergletscherung, p. 290) is interposed between the Nagelfluh and
the Lower Glacialschotter, which has not yet been noticed in the lake
district.

(c.) An irregular covering of genuine morainic material, swelling
up in places into hilly ridges, extends in the lake district, in a very
discordant manner, as well over the elevations occupied by the
Nagelfluh, as over the Miocene Flinz, and the slopes of the diluvial
gravels (b), up to the foot of the hills. Only in the district of the
outer moraines (near Fiirstenfeld-Bruck, etc.), are the diluvial
gravels (b) and the slopes of Flinz free from this morainic covering.

The moraines show nearly the same admixture of pebbles as the
gravels (b). They contain scratched boulders, together with angular
fragments of the same kinds of rock. All these scratched and
angular fragments are usually small, they very seldom reach a
diameter of half a metre, generally they vary from the size of a nut
to that of one’s fist. This type which is characteristic of the ground-
moraine is particularly represented also by the longitudinal ridges.
Therefore the latter may be recognized as the ground-moraine scooped
out at the margin of the ancient glacier.

In the district embraced in our excursion, no moraines are present
at the base of the Nagelfluh or below the glacial gravels (b).
Below these latter, however, beyond the excursion district, near

Glaciers of the Isar and the Linth. 261

Toelz, Laufen on the Salzach, and at Stefansbriicke near Innsbruck,
Penck has discovered moraines; but at the base of the Nagelfluh,
Tertiary strata exclusively have been met with.

Where we met with recently exposed surfaces, showing the depo-
sition of the moraine on the diluvial Nagelfluh (at Tutzing, Berg,
Starnberg), the surface of this latter was smoothed and polished as
distinctly as if it had been a homogeneous rock, and striated in
the same direction as the course of the valley. The individual
pebbles in the Nagelfluh were also evenly cut through in section.

Also when the contact surface of the moraine and the glacial
gravels (b) was exposed, there was nearly always a sharply-marked,
often discordant, boundary between the two deposits, without dis-
turbance in the underlying gravel; and occasionally the projecting
boulders in the gravel were striated in the direction of the valley,
though no connected striated surface had been formed on them.

North of the Starnberg Lake, we noticed a moraine irregularly
interpenetrated with beds of gravel and sand; which we recognize
as a deposit formed near the terminal end of a glacier (Penck, Ver-
gletscherung, etc. p. 132, figs. 4, 5).

Il.—The Quaternary Deposits in the District of the Lake of Zurich.

In the valley of the Lake of Zurich, as in the lake district of
Upper Bavaria, Upper Miocene strata form the foundation on which
the Quaternary deposits rest, and these latter are also divided into
gravels (Schotter) and moraines.

In contrast, however, to the exceptional regularity with which the
gravel deposits in the Bavarian lake district succeed each other under
the moraines, those at the lower end of the Lake of Zurich show, on
the one hand, an extremely slight connected development, and on the
other, they present such great differences in regard to the respective
elevations at which they are deposited, that it seems almost impossible
definitely to mark out their limits, or to parallel the deposits of
different localities.

(a.) There is indeed found occasionally, on certain particular
elevations between the valleys, a deposit of Nagelfluh, resembling
petrographically the Bavarian diluvial Nagelfluh (Uetliberg 870 m.,
Baden 470—490 m., Sihlsprung near Hirzel [outside the bounds
of our united excursion | 580—640 m.) ; but this is so limited in its
distribution, and the places in which it appears are so far apart,
that, with our present knowledge, it cannot be considered as the
remains of a general covering. Besides, moraines occur under
the cavernous Nagelfluh of the Uetliberg, whilst they have never been
met with below the Bavarian diluvial Nagelfluh, and on the other
hand moraines do not any longer appear above this Nagelfluh as they
do in that of Bavaria. The cavernous Nagelfluh of Sihlsprung near
Hirzel rests, according to Heim, on ground-moraines, and is covered
by immense upper moraine deposits.

(b.) A somewhat different formation of loose gravels (Schotter)
and Nagelfluh, either with or without decayed pebbles, is present,
though in very few localities, on the slopes of the valley of the Lake

262 Professors A. Heim and A. Penck—

of Zurich (Waedensweil, Utznach). We find similar gravels and
Nagelfluh far wider distributed at the north-east border of the
Glatt Valley, where they lie between the ground-moraine and the
upper-moraine. Near Diirnten and Wetzikon, lignites are deposited
between the gravel and the ground-moraine. These deposits of
rolled materials also, which we here place under (0), are isolated to
such an extent, and deposited at such different heights, that they
cannot be regarded, at least so far as the valley of the Lake of
Zurich is concerned, as the remains of an extended connected valley
deposit.

(c.) The Nagelfluh of the Au peninsula, on the Lake of Zurich,
is distinguished by its ‘delta structure” from the above-men-
tioned deposits of rolled materials in the neighbourhood of the
Lake, and it has no equivalent in our Bavarian excursion-district.
It calls to mind the ancient Kander delta, on the Lake of Thun, and
according to Penck (Vergletscherung, etc., p. 843), the Nagelfluh of
Biber in the Inn valley, and that of the Ménchsberg of Salzburg. Its
relation to the moraines is not exposed. From the mode of its oc-
currence it very probably belongs to the base of the upper moraine.

(d.) Of all the Quaternary deposits, the moraines of the Lake of
Zurich play the most important part. There is an astonishing con-
_ trast between them and the typical Bavarian moraines. The morainic
hills are shown by the prevalence of large, angular, erratic blocks
and sand, and the diminished quantity of clayey material, to belong
mostly to the upper-moraines; such are altogether absent in the
Bavarian lake district. The pure ground-moraines form in Switzer-
land an irregular, but not very thick layer, overlaid by the upper-
moraines, or by the gravelly deposits above mentioned. Only the
terminal moraines, and not the longitudinal moraines, have obtained
a great part of their materials from the ground-moraines.

IlI.—The Relation of the Upper Bavarian Lakes to the Quaternary
Deposits.

The Ammer Lake and Wuerm Lake occur in wide valleys, which
form deep bay-shaped indentations in the southern margin of the
same deposit of Nagelfluh. In the valleys especially, which have
been excavated in the deposit of Nagelfluh, and also in the surround-
ing district of the above-named lakes, the gravels (I. b) are developed,
and, indeed, they can be seen with constant characters, in the lower
part of both lakes, in the upper part of Ammer Lake, and on the
east margin of Wuerm Lake. The Lakes of Staffel and Rieg are
situated to the south of the Nagelfluh district, where they extend
themselves in a basin in the ancient Molasse, which is partly filled
with the gravels I. 6. (Schotter). They are bounded above and below
by ridges of the dislocated Molasse, whilst between both only
horizontal beds of the gravels (I. b) are raised above the surface.

The moraines form a surface layer, alike on the tops of the hills
between the lakes, as on their slopes down to the margins of the
lakes, thus, as a rule, covering discordantly the outcrops of Nagelfluh,
Miocene Flinz and gravel (I. b) ; so that these various deposits are
only exposed in lateral gullys or in steep cliffs.

Glaciers of the Isar and the Linth. 263

Ammer Lake and Wuerm Lake are limited above and below
by recent deposits. Their valley basins are bounded below by
moraine walls, which the outflow from the lake cuts through,
forming extremely narrow valleys. In the sections laid bare, the
gravel (b) is shown under the moraine, and in the Wuerm Valley
the Flinz is also exposed. Lower down the valley, beyond the
moraine walls bounding the lake-basins, the gravel (I. >) forms
extended terraces, partly interrupting the covering of the Nagelfluh
and the outer moraine.

IV.—The Relation of the Lake of Zurich to the Quaternary Deposits.

Wuerm Lake and Ammer Lake, both in their relation to the
Quaternary deposits, and also to the Molasse valley to which they
belong, show very different phenomena to those of the Lake of
Zurich and of the other large lakes of the Alpine borderland of
Switzerland. The valleys in the Molasse in these latter are much
deeper. A deposit like the gravel (Schotter) (I.b) in Bavaria, which
both above and below the lakes exhibits the same uniform slope, is
altogether unknown in the Lake of Zurich, in which the only gravels
found are those mentioned under (II. b). On the declivities of the
valley of the Lake of Zurich, the Molasse rock is itself carved into
distinct erosion terraces, independent of the stratification, and these
are often only sparsely covered with glacial débris, and not seldom
altogether bare, whilst a similar conditian of things is not observable
on the borders of Wuerm Lake and Ammer Lake on account of the
slight elevation of the outcrop of the Flinz and of the valley slopes,
and of the soft character of the material. In Switzerland, for the
most part, the valleys below the lake basins remain widely open,
and show more especially the characters of main lines of ancient
valleys. Hardly anywhere is the outlet of a lake through a narrow
gully. The Molasse in the district of the Lake of Zurich is plainly
not horizontal, but it forms a shallow trough between the Alps and
Jura: the depression in this has affected the ancient erosion-terraces
in unequal proportions.

The Quaternary deposits rest on the dislocated Molasse terraces of
the declivities of the valley, so that the lateral moraines, with their
somewhat steeper inclinations in the direction of the valleys, cut the
margins of the Molasse terraces at an oblique angle.

On the other hand, Rieg Lake and Staffel Lake in some measure
call to mind certain of the smaller lakes of the Alpine borderland,
as, for example, Greifen Lake and Pfaeffikon Lake in the Glatt
district.

V.—The Question of the Origin of the Lake-Basins.

In our excursion in Upper Bavaria, Heim had the opportunity
of ascertaining the facts respecting this district published by
Penck in his “‘ Vergletscherung der deutschen Alpen.” + On the other

1 A review of this work is in the GzeonoercaL Macazine for 1883, Decade II.
Woly Xe) po 17.7.

264 Professors A. Heim and A. Penck—

hand, Penck was able to confirm the facts which had been pub-
lished by A. Wettstein in his work, “Geologie von Ziirich und
Umgebung.” Weare completely agreed respecting the facts observed,
and differences can only arise on the conclusions to be drawn from
the facts. The great differences in the Quaternary deposits of
Bavaria and of Switzerland deserve special prominence. They
teach that the greatest prudence is necessary, in regard to generali-
zations based on conclusions drawn from a limited area.

The grounds which Penck brings forward in favour of the Glacial
origin of the Bavarian highland lakes are :—(1) the coincidence of
the position of the lakes with the glacial deposits; (2) the
characters of the lake valleys are such as are produced by erosion ;
and (3) the age of the lakes.

Their character as products of erosion is made clear from the
fact that they are valley-shaped gaps in a continuous uniform series
of undisturbed stratified gravels, whilst their diluvial age is proved
by the fact that these stratified gravels end with the deposit of
the diluvial Nagelfluh (i. a). On the other hand, both above and
below the lakes, as well as round their margins, the horizontally
stratified gravels (Schotter) (I. b) are shown, in which the lake-basins
appear to form excavations. As these gravels (I. b) are, on the one
hand, covered by moraines, and on the other, contain a notable
number of pebbles of Archean rocks, which could only have been
transported by glaciers from the central region of the Alps over the
passes of the limestone Alps, they must therefore have been formed
immediately before the advance of the glacier into the lake district.
As, however, the lake-basins are excavated in these gravels, they are
necessarily more recent; they could thus not have yet been in
existence at the commencement of the last glaciation of this district
to which the gravels correspond. On the other hand, the deposition
of the moraines on the slopes of the lake-basins shows that these
latter were formed at the time of the retreat of the glacier. Their
origin must therefore have taken place at the time of the glaciation
itself.

Of these three grounds brought forward by Penck, the first one is
established. As regards the second, it might be said that the gaps
in the south margin of the covering of Nagelfluh might have been
produced in it originally; that glacial-tongues, which covered the
areas of the lake-basins, produced the Nagelfluh, as a fluvio-glacial
deposit, whilst they protected the lake-basins against the accumula-
tion of gravels. Against this, is,

(a.) The high degree of uniformity in the petrographical characters
and the stratigraphical deposition of the Nagelfluh (I. a).

(B.) The absence of any morainic material below the Nagelfluh,
as also the non-existence of genuine glacial materials, such as striated
boulders, etc., within it.

A further possible mode of formation of the lakes might consist in
a relatively small change of level in the lake district, by which the
original slope of the Nagelfluh was diminished, whilst the valleys
cut in it became reversed, and converted into lake-basins. This is

Glaciers of the Isar and the Linth. 265

the more conceivable, since the southern part of the covering of
Nagelfluh has a somewhat steeper dip than the more northern part;
this, however, may readily be regarded as its original structure.

A positive proof of such changes cannot be found in the oldest
deposits of the district of the Bavarian highland lakes, which thus
contrast with those of the Lake of Zurich, because connected erosion-
terraces are wanting, and more especially because the position of the
strata of the Miocene Flinz cannot be accurately determined. But
though the possibility of such an origin of the lakes through local
changes of level cannot be proved to be inconceivable, it is so,
nevertheless, if it leaves the coincidence of the extension of the
glacier with the formation of the lakes, and the absence of lakes
beyond the margin of the glacier, to be explained as the result of
pure chance.

As regards the third ground for the glacial origin of the Bavarian
highland lakes, the aye of the lake-basins, it may be remarked that
the gravels (I. b) are deposited on the slopes of Nagelfluh and Flinz.
As the gravels were formed before the advance of the glacier, the
valley which they cover, as well as the gaps in the covering of
Nagelfluh, must also have been in existence before the glacier,
as, moreover, Penck has already noticed (Vergletscherung, p. 357).
There remains, therefore, no further solid excavating work for the
glacier to perform, but merely the re-excavation of a part of the old
valley out of the gravels (I. b), leaving behind many fragments
of the same on the slopes, and further, the scooping out of the
hollow, 120m. in depth, in the soft Flinz. It may be noticed that
the Flinz is a marly-clay which falls to pieces in water, and although
rock in appearance, it would offer less resistance to the course of the
glacier, than even loose pebbles.

Staffel Lake and Rieg Lake lie between ridges of Molasse, parallel
to the Alps. The oblique partition separating them is formed of
huge masses of the gravels (I. 6), which can hardly have been origin-
ally deposited in their present limits. Heim acknowledges, in view
of this, that a re-excavation of a part of the gravels in the same
northerly direction in which the Alpine valleys become open, is by
far the most probable mode of the formation of these lakes. Heim
also accepts a similar origin for the now extinct lake of Murnau and
the lake Kochel. As, however, regarding these lakes, it is only a
question of the re-excavation of basins of dislocation, in which the
harder ridges of Molasse on their margins and the islands of the
same have not been destroyed, we are both entirely of the same
opinion respecting them.

On aconsideration of the Bavarian highland lakes, Heim conceives
the re-excavation of valleys filled with loose gravels, as also the
scooping out of depressions in very yielding materials, and thereby
the formation of lake-basins through glaciers, possible, as heretofore
(comp. “ Gletscherkunde,” p. 882 at top, and p. 886), and in the
present instances, as very probable. On the contrary, proofs of the
formation of extended basins in hard rock and of the excavation of
the same through glaciers cannot be found in this district.

266 Professors Heim and Penck—Glaciers of the Isar and Linth.

Of the three grounds, which, according to Penck, support the
glacial origin of the Lakes of Ammer, Wuerm, Rieg, and Staffel, only
the two former are applicable to the Lake of Zurich, and the other
large lakes of the Swiss Alpine borderland. But just as little as in
the first case, the position of the lakes in the area of glacial deposits,
and, in the second, the character of the lake valleys as produced by
erosion, can be disputed, even so little can the age of the lakes be
brought forward as a proof of their origin.

Whilst namely, on the one hand, the gravel deposits indicated by
II. a and II. b are only thus locally and sporadically developed, so that
no conclusion can be at present arrived at as to their former connection,
it can neither be proved that the lake valleys are depressions in a
former covering of diluvial Nagelfluh, nor that the lake-basins repre-
sent hollows in a gravel formation corresponding to I. b. There is
thus nothing to add to our information respecting their Quaternary,
a.e. Glacial age. But, on the other hand, the Nagelfluh of the Au
represents a probably very ancient deposit, which, by its delta struc-
_ ture, proves the existence of the Lake of Zurich already previous to
the commencement of the last glaciation, so that the lake cannot be
attributed to its action. At the same time, the position of the rock-
terraces of the declivities of the valley afford decisive proof of dis-
locations which affected the lake valley and produced the basin-
shaped depression in it. Penck holds with Heim and Wettstein that
there is undeniable evidence of the influence of dislocations in the
formation of the basin of the Lake of Zurich, but he is never-
theless of the opinion, that with a more thorough investigation of
the Swiss Quaternary gravel deposits, it may perhaps be found pos-
sible to discover a parallel between the deposits named I. 6 and II. b in
the two areas respectively, and he holds the view that the lake-basin
originally produced by dislocation may be toa greater or lesser degree
excavated by glacier action. Heim also does not question the fact of
a certain, though relatively small, amount of the scooping out of the
lake-basin being due to the glacier.

Penck holds that to re-excavation may very probably be attributed
the formation of the lakes of the Glatt valley, of the Greifen Lake
and Pfaffikon Lake, in the same way as in the case of Rieg Lake and
Staffel Lake, whilst Heim is disposed rather to explain the origin of
these two lakes of the district of the Glatt valley to the blocking-up
action of moraines.

There is, therefore, no real difference of opinion between us
touching the Lake of Zurich and the Lakes of the Bavarian high-
lands, either as regards the facts or the conclusions from them; and
as in the present case, so also does it often happen, that by a more
exact conjoint examination, differences become of much less import-
ance than they appear to be from a distance.

F. W. Rudler—Rocks from Arabia Petrea. 267

V.—Norzs on some Rocks rrom ARABIA PETRmA.
By F. W. Ruptzr, F.G.S.,
of the Museum of Practical Geology.

ROFESSOR HULL, soon after his return from Palestine, was

good enough to place in my hands, for microscopic examination,

a collection of twenty sections of rocks prepared from specimens

obtained in the course of his expedition. Subsequently I had the

advantage of receiving thirteen small specimens of the rocks from

which some of the sections had been cut ; and respecting these rocks

some lithological notes have been published as an appendix to Prof,

Hull’s Memoir.t At a later date I received seven other rock-

specimens, representing the remaining sections in my charge; but

for want of time these were laid aside unexamined until it was too

late to refer to them in the published work. The object of the

present notes is therefore to offer brief descriptions of these remain-

ing rocks. At the same time I gladly seize this opportunity of

correcting some errors which unfortunately crept into the previous
descriptions.

I. Pale Pink Granite, from a Dyke Penetrating Grey Granite, at Jebel
Watiyeh.

A fine-grained granitic rock, consisting mainly of opaque white
felspar and hyaline grey quartz, speckled with a few dark green
patches of an altered mica. It presents a general pinkish grey
colour, due to a small quantity of ferric oxide disseminated through
the rock, and specially marked on the weathered joint-surfaces of
the specimen. ‘The felspar is for the most part very turbid, even in
thin sections. Many of the crystals exhibit a zonal structure, which
is well defined by the arrangement of the included granular matter.
Some of the felspar appears to be orthoclase, in an altered condition,
and probably microcline is also present; but most of the felspar is
a plagioclase, with extinction angles, in relation to the line of twin-
composition, varying from 3° to 14°. In a good deal of the felspar,
however, the edges of the hemitropic lamelle are too blurred to
allow the exact angles to be taken. Some of the felspar crystals
measure in section as much as 8 mm. X 155mm. The quartz is
xenomorphous, occurring in the form of clear subangular grains,
ranging from 0-5 to 1 mm. in diameter, and traversed by reticulating
lines of pores. Much of it shows a polysynthetic structure in
polarized light. A few folia of muscovite, or other white mica
with straight extinctions, are distributed through the rock. This
mineral may be a secondary product. But the dominant micaceous
mineral is a biotite, or dark dichroic mica, occurring in aggregated
lamine, and mostly altered, after the habit of the ferro-magnesian
micas, to a chloritic mineral. A few acicular crystals of apatite are
present, penetrating alike the felspar and the quartz. Some grains
of epidote may be detected ; and magnetite is present in small quantity,
while scattered through the rock are small patches of hematite and
limonite, with here and there a few folia of chlorite.

1 “Memoir on the Physical Geology and Geography of Arabia Petraa, Palestine,
and adjoining Districts,’’ Palestine Exploration Committee (1886).

268 FF. W. Rudler—Rocks from Arabia Petrea,

Il. Red Granitoid Rock, with Micropegmatitic Structure, from Jebel
Watiyeh.

This rock is an intimate aggregate of flesh-red felspar and quartz,
with grains of vitreous quartz and crystals of felspar scattered
through the ground-mass. It may be regarded as a fine-grained
binary granite, almost a microgranite, with porphyritic quartz and
felspar ; thus suggesting a transition to a coarse kind of quartz-felsite
with a ground-mass of phanero-crystalline texture. The felspar is
highly charged with reddish-brown granules, perhaps kaolin with
limonite, which by their comparative opacity render the section very
nebulous. The felspar is presumably a red orthoclase, and is asso-
ciated with large crystalline grains of clear quartz with numerous
pores. In places the felspar and quartz of the ground-mass are so
intimately united as to form a beautiful micropegmatite or grano-
phyre. The association naturally suggests contemporaneous, and
probably rapid, solidification of the two minerals. In some cases
the formation of the micropegmatite has started from a pre-existing
crystal of felspar, whence the interblended felspar and quartz diverge
in plumose forms. This is the rock referred to by Prof. A. Geikie
in his “'Text-book of Geology,” second edition, 1885, p. 635, foot-
note 3.

The rock from Jebel Musa, No. 1, in the Appendix to the Memoir,
described asa gneiss, seems rather to bea fine-grained granitoid rock.
The faint tendency to foliation, suggested by a small specimen, is
illusory. The rock, though diverging greatly from the normal
granitic type, and presenting rather a granulitic texture, may pro-
bably be best described as a hornblende-granite.

Ill. Red Porphyrite from Jebel Musa.

This rock presents a compact base of deep tile-red colour, with
subconchoidal fracture, in which are disseminated porphyritic crystals
of red felspar and irregular dark green patches of an altered mineral,
apparently a mica. Some of the large felspars reach a size of 4mm.
x 15mm. Even in thin section they present a strong reddish
colour, which is deepest around the inner border of each crystal, where
the granules of ferric oxide are accumulated. Some of the crystals
seem to be orthoclase, but others show indistinct polysynthetic twin-
ning, with broad lamellation. Zonal structure is presented by some
of the crystals. The other porphyritic constituents are green crystals,
measuring about 1:25mm. x 1mm. These seem to be pseudomorphs
after biotite; at least such an origin is suggested by their strongly-
marked striz, which seem to represent the basal cleavage of a mica,
by the occasional curvature of the laming, and by the hexagonal
form of some of the sections. This green epigenetic mineral is
strongly dichroic, and is flecked with an opaque oxide of iron, pro-
bably magnetite. The slide also carries some irregular patches of
chlorite. Apatite is present in rather stout six-sided prisms, both in
the felspars and in the altered mica. Epidote occurs in aggregates
of greenish-yellow grains, inclosed in both the porphyritic minerals.
Quartz may be detected in interstitial spaces, but is apparently of

F. W. Rudler—Rocks from Arabia Petrea. 269

secondary origin. Probably the history of the rock has been some-
what of the following character :—The apatite, the biotite, the large
felspars and the ground-mass successively solidified in the order here
enumerated ; the mica was afterwards transformed into a chloritic
mineral, with separation of magnetite, while further alteration of the
chlorite resulted in the formation of epidote, which may also have
partly resulted from the decomposition of the felspar, inasmuch as it
occurs in the heart of some of the larger felspar crystals.

IV. Felsitic Tuff from Es Shomrah.

This rock appears macroscopically to be a porphyritic felsite, with
compact chocolate-coloured base and disseminated crystals of white
felspar. Under the microscope, however, it is seen to contain
angular fragments of various rocks, with broken crystals of plagio-
clase, forming a brecciated mass. Mr. F. Rutley, F.G.S., to whom
I am indebted for having examined some of my sections, points out
the general similarity of the ground-mass to that of the rhyolitic
rock from Pont-y-Gromlech, which he described some years ago;
but at the same time inclines to the view that in the present case
the ground-mass consists of fine dust, in great part felspathic,
perhaps associated with shreds of devitrified lava. Among the im-
bedded fragments, which vary in diameter from about 0-03 mm. to
2mm., are rhyolites, or devitrified rocks showing banded and
fluxion structure. Some of the fragments and imperfect crystals of
felspar reach a size of 2:25 x 1:3 mm., and though mealy in texture,
show traces of repeated twinning.

V. Hornblende-augite Rock from Es Safeh.

A coarsely crystalline, almost black rock, weathering with a rusty
surface. ‘Thin sections show large porphyritic crystals of brownish-
green hornblende, colourless augite, and decomposed felspar, im-
bedded in a pale brownish ground-mass of felspathic microlites,
with green products of decomposition. Some of the crystals of horn-
blende measure, in section, as much as3mm. X 1:2 mm. Most of
them are much fissured and carious, inclosing green alteration-
products, and having rather indistinct outlines, bordered by dark
greenish granules. The best-defined sections are those cut approxi-
mately normal to the perpendicular axis. These show the common
six-sided forms, bounded by the edges of {110} {010}, with inter-
secting lines of prismatic cleavage breaking up the section into
characteristic rhombs. Elongated sections parallel to the vertical
axis give longitudinal cleavage lines, and the extinction-angles in
relation to these lines vary from 0° in some of the sections which
are cut parallel to {100}, to a maximum of about 15°. The pleo-
chroism is not very marked: a=pale yellowish brown, b = pale
bottle green, r = olive green. Much of the hornblende is twinned.

The augite appears in very sharply-defined crystals, which in thin
sections are quite clear and colourless. Most of the sections are
eight-sided, being limited by edges of {110} {100} {010}. Some
of these measure nearly 1 mm. in the edge. The prismatic planes

270 F. W. Rudler—Rocks from Arabia Petrea.

dominate in some of the sections, and the pinacoids in others. The
characteristic cleavage parallel to {110} is well displayed. Some
sections of rhombic shape, cut approximately in the plane of sym-
metry (010), give extinction angles of nearly 40°.

Two sets of felspars may be noted. Those of the first consolida-
tion occur in groups of large crystals, some of which give sections
reaching a size of 2 mm. X 0:6 mm., three or four such crystals
forming a cluster. All the felspar is profoundly altered. By reflected
light it presents a dead white colour, but by transmitted light a red-
dish tint. Notwithstanding its advanced state of decomposition, the
repeated twinning of a plagioclase may be detected, and the wide
extinction angles of the broad lamelle suggest a felspar of high
basicity. The small felspars of later consolidation occur in crowds
of slender interlacing crystals, with irregularly-terminated lath-
shaped sections, measuring on an average 0:16 x 004mm. ‘The
meshes of this reticulating mass of microlites are occupied by a
green decomposition product, of fibrous and tufted structure, with
strong depolarizing action between crossed Nicols. There are also
large irregular patches of a green mineral, chloritic or serpentinous,
following irregular cracks in the rock, and associated with calcite and
epidote. The calcite also forms large crystalline masses and ill-
defined patches, with aggregate polarization. Olivine appears to be
represented by crystals which have suffered much alteration, and are
mostly converted into green pseudomorphs with a brown margin.
Magnetite is disseminated through the rock, and red and brown
oxides of iron occur in patches.

It does not appear easy to bestow upon this rock an appropriate
name. It is very similar to the rock No. 18, from Jebel esh Shomreh,
described in the Appendix to the Memoir as a hornblende-augite
andesite, but I am anxious to withdraw that name, as the rock is
decidedly basic. Notwithstanding the large proportion of horn-
blende, the affinities of the rock appear to lie rather with the
dolerites and diabases. Its structure is in no way related to that of
the diorites. With a little more olivine and a little less felspar it
might perhaps claim a place among the hornblende-picrites, which
have been so well described by Professor Bonney, D.Sc., F.R.S.

VI. Dolerite from Gehat es Shomrah.

A dark-brown, nearly black, rather fine-grained rock, with large
porphyritic crystals of greyish felspar with greasy lustre. The
ground-mass, viewed in the microscope, consists mainly of a confused
network of felspars, yielding lath-shaped sections, mostly binary
twins, with an average size of 0:03 mm. x 0-007 mm. The augite
occurs in crystalline grains and small crystalline masses, of brown
colour, occupying the spaces between the felspars, and evidently of
later consolidation. Indeed, the penetration of the augite by the
felspar gives rise to an indistinct ophitic structure. Olivine is
present, partly serpentinized, in the form of amber-coloured grains,
with here and there a small crystal. One well-marked crystal, of
irregular six-sided shape, measured 0°38 x03 mm.; like the other

Prof. T. R. Jones and C. D. Sherborn—Jurassic Microzoa. 271

olivines in the section it contains magnetite along its cleavage cracks
and curved fissures. Magnetite is freely disseminated throughout
the rock. With a high power crowds of colourless acicular microlites,
perhaps apatite, come into view. A little calcite, showing aggregate
polarization, is present as a secondary product. No distinct inter-
stitial matter can be detected, and indeed the rock appears to be
a holocrystalline dolerite. A porphyritic structure is imparted to
the rock by large crystals of felspar, the rectangular sections of which
may measure as much as 8 mm. xX 2 mm. This felspar shows
sharply-defined twin lamellation, and in some sections there are two
sets of lamellz approximately at right angles to each other, thus
suggesting that the plagioclase is twinned on both the pericline and
albite types. From its high extinction-angles, reaching 40°, it is
probably a basic felspar near to anorthite.

VII. Dolerite from Wady es Shick.

A medium-grained, dark-brown rock, much altered, and weather-
ing with a yellow rusty surface. It presents in thin section a dense
network of plagioclase in rather thick rectangular sections, with an
average size of 1 x 0-25mm. They inclose dark greenish-brown
granular matter, so disposed in some cases as to give a zonal appear-
ance to the sections. Augite occurs in crystalline grains and granu-
lar aggregates. The space between the felspars is largely occupied
by serpentinous matter, and much of the substance which at first
sight looks like interstitial matter is probably a product of alteration.
Magnetite is abundant, and scales of red oxide of iron are scattered
through the rock. Crowds of minute acicular microlites become
visible with a high power.

A re-examination of the diabase, No. 12 in the Appendix, shows
that all the quartz is of secondary origin, and hence the rock is
simply a diabase with quartz, and not a quartz-diabase. With
reference to the felsite, No. 10, it should have been stated that the
description applied only to the particular thin section under ex-
amination.

I am greatly indebted to Mr. J. J. H. Teall, M.A., F.G.S., and to
Mr. T. Davies, F'.G.S., for having examined with me some of the
sections described in these notes.

VI.—On tHE Microzoa FOUND IN soME JuRASSIC RooKs oF
ENGLAND.

By Professor T. Rupert Jonzs, F.R.S., anp C. D. Suerzorn, Esq.

N the Gronocican Magazine, Dec. II. Vol. IL 1875, p. 808, is

a list of some English Jurassic Foraminifera, a large number

of species being there noted as occurring in these rocks. We have
lately received, by the friendly courtesy of the Rev. H. H. Winwood,
F.G.8., and Horace B. Woodward, Esq., F.G.S., thirteen specimens
of the Jurassic rocks from the south-west of England. One of these
has yielded a most important series of Ostracoda. Whilst preparing
a special monograph, we hasten to offer some preliminary notes on
these interesting Jurassic Microzoa, at present merely noting the

272 Prof. T. R. Jones and C. D. Sherborn—Jurassic Mierozoa.

genera, in descending order of strata, and deferring the specific
nomenclature for a subsequent opportunity.

1. “ Kimmeridge Clay, near Coulston, Wilts.” H.B. W.

A mottled (blue and yellow-brown) clay, very stiff and greasy to
the touch. Residuum, after washing, a very little, fine, subangular
sand, with minute woody fibres. Microzoa rare and very small, of
a brown colour and with a sandy appearance. The Foraminifera are
Trochammina incerta; T., sp. near oligogyra, Hantken ; and another
near gordialis ; Marginulina = Cristellaria Zitteli, Schwager; Cris-
tellaria sp.; Nonionina, sp.; Orbulina neojurensis, Karrer; and a
three-chambered Globigerina. These minute fossils are beautifully
preserved. No Ostracoda were found.

2. «Clay at the base of the Lower Greensand and on the top of the
Corallian ; Seend, Wilts. Most likely Kimmeridge Clay.” H.B.W.

A pale-grey clay (when dry).

This specimen was washed completely away, leaving neither
Microzoa nor sand.

3. “Clay above IJron-ore deposit; Westbury Ironworks, 8. of
Station. ? Kimmeridge Clay.” Rev. H. H. W.

A stiff, mottled, blue clay, with numerous very small, rounded,
shining, black concretions.

This left a very small, but rich, residuum of Foraminifera, having
a very characteristic Jurassic facies. Amongst the forms are Lingulina
carinata, var. (this is an oval Nodosarina, and, although the mouth
appears to be a circle of radiating fissures, we think it should be
regarded as more Linguline than Nodosarine in character) ; Nodosaria,
sp. near nitidula (Gtimbel, ‘Streitberger Schwammlager ’) ; Dentalina
communis; Planularia reticulata; P. pauperata, narrow, broad, and
thin varieties; Vaginulina cristellarioides; V. orthonota; V. angus-
tissima; V. harpa, and two others (the first four are figured by
Reuss in his ‘ Norddeutschen Hils und Gault’); Cristellaria rotulata
with three varieties leading into the next “species,” Cristellaria
crepidula ; and Haplophragmium Canariense.

These forms are well preserved. No Ostracoda were found.

4, “Yellow Fullers-earth Clay ; Midford.” Rev. H. H. W. and
EB We

This and the following clay are described by Horace B. Woodward
in his “ Geology of England and Wales” (p. 182) as “a sandy clay,
which is described by Mr. Bristow as usually of a greenish-brown
or greenish-grey colour, sometimes blue. It is opaque, soft, dull,
with a greasy feel, and an earthy fracture.” The specimens sent
were of a yellow-brown colour,

From the specimen of yellow clay we obtained only two species
of Foraminifera, Cristellaria crepidula and Vaginulina legumen, var.

It is richer, however, in Entomostraca, five species of Cythere ;
two of Cytherideis; three of Cytherella; and one of Bairdia, re-
warding our search.

5. “Blue Fullers-Harth; Midford.” Rev. H. H. W. and H. B. W.

An indigo-blue clay, drying bluish-grey, extremely rich in Micro-
zoa, especially Ostracoda. lt is rather singular that this most

Prof. T. R. Jones & C. D. Sherborn—Jurassie Microzoa. 273

remarkable deposit of Entomostraca has not been noticed before.
We have mounted and arranged upwards of three hundred individuals
of more than fifty species already, and look for a much larger number
before we close our work. The majority of the species were
obtained from little more than one pound weight of material.
Foraminifera are much scarcer, but there is the same proportionate
abundance between the two groups as in the yellow-brown clay
above described. A few fragments of shells also occurred, but too
imperfect for identification ; also ossicles of Pentacrinus, and a few
broken minute spines of Echinoderms.

The Foraminifera include a subcarinate variety of Cristellaria
rotulata, near to one figured by Jones and Parker (Q.J.G.S. vol. xvi.
1860, pl. xx. f. 48); Cristellaria crepidula; Vaginulina legumen ;
Planularia, sp. near reticulata, Cornuel; Nodosaria lineolata, Reuss,
and Frondicularia peregrina, Reuss (‘ Bohm. Kreide’); and a simple
four-rayed star, like the “Siderolina-like forms” figured by Giimbel
from the ‘“Streitberger Schwammlager” in ‘‘Jahresh. Ver. nat.
Wirtt. 1862, Jahre. 18, p. 235, pl. iv. f. 19. This little specimen
has been shown to Dr. Hinde, who thinks that, although calcareous,
it is most likely a modified dermal spicule of a hexactinellid Sponge.

The Entomostraca represent, provisionally, thirty-four species of

Cythere; three of Cytherideis; three of Cytheridea; five of Cytherella;
six of Bairdia, also Cytherura, Pontocypris, Macrocypris, and possibly
Aglaia and Argillecia.

The examination of these forms is affording us very great pleasure,
being, though exceedingly small, very finely preserved and perfect.
It is interesting to note, that we identify some ten of them as oc-
curring amongst those figured from the Richmond Well in Q.J.G.S.
vol. xl. pl. xxxiv.

6. “ Loamy beds in Hinton Sand, Forest-marble ; Charterhouse-
Hinton, Somerset.” H.B.W.

A light-brown loam with small ‘clay galls.” This leaves after
washing a residuum of fine, subangular, quartzose sand. After
careful search we found some extremely small Foraminifera and one
Ostracod :—Cristellaria crepidula; Marginulina glabra; and a valve
of Cythere.

7. “ Bradford Clay; Bradford. This is the clean clay immediately
overlying the fossil-bed.” H.B.W.

A light-brown clay, which, on washing, left a few waterworn
Entomostraca and two much waterworn Foraminifera. The latter
are Cristellaria crepidula and Vaginulina legumen; and the former
are three varieties of Cythere.

8. “ Bradford, No.1. Near Canal. Zocus classicus.”’ Rev. H.H.W.

No Microzoa found on examination.

9. Bradford, No. 2. Near Bradford. Tuttle higher in position
than No. 1.” Rev. H.H.W. No Microzoa.

10. “Oxfordian; Upper Studley, Trowbridge. Probably Kella-
ways Rock.” H.B.W.

Dark greenish-brown, friable sandstone of subangular quartzose
sand, with calcareous cement. No Microzoa found.

DECADE III.—VOL. III.—NoO. VI. 18

274 Notices of Memoirs—M, Dollo—

11. “Oxford Clay; Bromham Brickyard. South of Sandridge
Hills, between Melksham and Devizes.” H.B.W.

A few fragments of shells, but no Microzoa, were found.

12. “Oxford Clay; Upper Studley, Trowbridge.” H.B.W.

Very pale, yellowish-grey, sandy clay, yielding after washing,
about 50 per cent. of extremely fine, white, subangular, quartzose
sand. No Microzoa.

13. “Oxford Clay ; Southwick, Trowbridge.” H.B.W.

Like No. 12, leaving, after washing, the same remarkably fine,
white sand, and presenting no trace of Microzoa.

Norse.—Beside the Jurassic specimens we have one from the
Cretaceous series of the same district, namely :—Clay seam in
Lower Greensand; Seend.” H.B.W.

A ferruginous sandy clay; bound together in places by the iron
and forming “pan.”

By washing, this specimen yielded abundance of subangular
sand, with a little mica.

No Microzoa were met with.

ANG OE RASCH S | (Spey awe VGO else St
J.—M. Dotto on tue Evonvution or tae Trxetu or HerBrvorovus
Drvosauria. 4
Aust palzeontologists who are interested in the marvellous reptilian
life of the Secondary epoch owe a debt of gratitude to M.
Dollo of the Royal Museum of Brussels for the ability and care with
which he has elucidated the structure and affinity of the un-
rivalled collection of Dinosaurian and other reptilian remains pre-
served in that Museum. One of the most interesting of his

eH
Ny

Fig: 3

Dracram A.—F 1g. 1. Tooth of Morosaurus. Fig. 2. of Scelidosaurus,
Fic. 3. of Hadrosaurus.

Evolution of the Herbivorous Dinosauria. 275

contributions! to our knowledge of the Dinosauria shows how the
teeth of the herbivorous members of that order have gradually
increased in complexity of structure, and as the author has kindly
allowed the use of some of the woodcuts illustrating his memoir,
we have great pleasure in laying before our readers a sketch of this
line of evolution.

In the generalized suborder Sauropoda, which is mainly Jurassic
and died out after the Wealden, we find that the teeth, as in Morosaurus
(Diagram A, Fig. 1), are perfectly simple, having neither serrated
edges, nor carrying ridges on their lateral surfaces. In the generalized
Jurassic Stegosauria the teeth still retain the same simple structure,
but in the more specialised members of this suborder (e.g. Scelido-
saurus, Diagram A, Fig. 2), which occur in both the Jurassic and
Cretaceous, they have developed serrations on the edges, although
not distinct lateral ridges. The next step is presented by certain
members of the Ornithopoda, as Hadrosaurus (Diagram A, Fig. 3),
where a distinct vertical ridge is developed in addition to the
serrated edges. Advancing to the more specialised Ornithopoda-like
Iguanodon (Diagram B), we find that secondary lateral ridges are

‘Lp

Ye

CEE
CUE:
GIES

UF; ng

Ge

Fig.1 Fig. 3 Fig. 2

Dracram B.—F ie. 1. Tooth of Iguanodon Prestwichi; from the enamelled surface.
Fic, 2 in profile. Fic. 3 section from 2 to y, ~. q@ shows the principal
lateral ridge without serrations.

developed; and we may further observe that while in the Jurassic

I. Prestwichi both primary and secondary ridges are simple, in the

Wealden I. Mantelli the former has become serrated. The last step

1 Ann. Soc. Sci. Bruxelles, 1885, pp. 309-338.

276 Notices of Memoirs—M. Dollo—Dinosauria.

but one is afforded by the remarkable teeth from the Upper Cretaceous
(Senonien) described by M. Dollo under the name of Craspedodon
lonzeensis (Diagram C), in which, in addition to antero-posterior

Diagram ©.—Tooth of Craspedodon lonzeensis. Fic. 1 from the enamelled
surface, =; ¢ crown, d f cingulum, the letters @ 6 eg hk 1 indicate the
serrations and ridges. Fic. 2 in profile, 7. Fic. 3 the large and small
serrations more magnified. Fie. 4 section at a y, 7.

serrations, there are primary, secondary, and tertiary lateral ridges,
of which both primary and secondary are serrated. Finally the
American Cionodon simulates the dentition of Ungulate Mammals in
having numerous cheek-teeth in use at one and the same time.

M. Dollo concludes this interesting survey by observing that “it
appears that while the specialization of the dentition in the Ungulata
las taken place either by the development of infoldings in the
enamel (Equide), or by the multiplication of tubercles (Suid), accom-
panied by gradual elevation of the crown, it has manifested itself in
the herbivorous Dinosauria by the development of ridges and
serrations, or by the simultaneous use of numerous teeth. While,
however, the cause of the evolution of the dentition of the Ungulata
is, so to speak, known to us, we can only guess at that of the dentary
system of the great Reptiles which filled their place during the
Secondary epoch.” R. Lypexxker.

Dana, Ford, and Duight—Fossils from the Taconic Series. 277

TI].—Emmons’ OrtGinaAL Taconic SERIES.

1. On Lower Siturtan Fossits FRoM A LIMESTONE OF THE ORIGINAL
Taconic or Emmons. By J. D. Dana.

2. Pretiminary Report or 8. W. Forp ann W. B. Dwicat
upon FossILs OBTAINED IN 1885 From Mreramorpuic LIMESTONES
oF THE Taconic Serres oF EHumons, aT Canaan, New York.
American Journal of Science, vol. xxxi. p. 241—258, pl. vii.
April, 1886.

ROFESSOR DANA points out that the original and therefore
true Taconic system of Prof. Emmons, which this geologist
propounded and described in 1842, ‘lies along both sides of the
Taconic range of mountains, whose direction is nearly north and
south, or, fora great distance, parallel with the boundary-line between
the State of New York and those of Connecticut, Massachusetts, and
Vermont.” Emmons described it as consisting of (1) “Taconic
slates”? in eastern New York, including the Hoosie slates; (2) the
Sparry or western limestone, interstratified with the slates, west of
the Taconic range, and for the most part lying against the west side
of the range; (3) the “talcose” or “magnesian”’ schist, constitut-
ing the Taconic range, and Greylock or Saddle Mountain, the high
ridge between Williamstown and Adams in the north-western angle
of Massachusetts; (4) the Stockbridge Limestone, east of the range
of Taconic schist; (5) Quartzite. Prof. Emmons concluded, on
lithological grounds, that the system was older than the New York
Potsdam Sandstone, and equivalent to the Lower Cambrian of Sedg-
wick. Subsequently, in Washington County, New York, outside the
typical area of the Taconic system, Emmons discovered, in black
slates, some Trilobites, pronounced by Barrande to be Primordial
species. ‘These black shales were regarded as more recent than the
typical rocks, in which no fossils whatever bad been discovered, and
Emmons called them therefore Newer or Upper Taconic.

But now recently fossils have been discovered in the Sparry or
Western Limestone, the oldest limestone of Emmons’ original
Taconic, and in a locality in the typical area of the system. The
fossils are very fragmentary, and can only be examined by means of
thin sections and polished surfaces of the rock. They show, how-
ever, the presence of distinct species of Murchisonia, Pleurotomaria,
and Fenestella, as well as portions of Crinoids, probably of Brachio-
pods, and of a Trilobite. Prof. Dwight and Mr. Ford, who have
studied the fossils, believe that they indicate the Trenton age of the
limestone in which they are preserved.

It follows from this discovery that the age of the typical Taconic
system of Emmons is not Cambrian or Pre-Cambrian, as stated by
him, and that the black shales and limestones with Primordial Trilo-
bites, forming his Newer or Upper Taconic system, really belong to
a period much older than the so-called Lower Taconic. G. J. H.

278 Reviews— Geological Survey of S. Australia.

Ee En Wie a WV

—__—__
GEOLOGICAL SuRvEY oF 8. AUSTRALIA.

Report oN THE GEoLogicaL CHARACTER OF Barosss AND PARA
Wrrra, South AUSTRALIA.

Nores, erc., EXPLANATORY OF PartramEenTARY Paper No. 178, with A
GrotogicaL Map or Prra Wrrra anp Barossa Ruserves.! By
Henry Y. Lyert Brown, F.G.8., Government Geologist, assisted
by Harry Pacr Woopwarp, F.G.8. Folio. (Adelaide, 1886.)

The Barossa and Para Wirra Goldfields.

The Barossa goldfield is situated in the south-west corner of the
hundred of that name; it is separated from the Humbug Scrub gold-
fields only by the South Para River, which latter is also included in
the map. It was discovered in October, 1868, by Job Harris and
mates, who found gold in the gully now known as Spike gully. This
gully is about one mile and a half long—the prospector’s claim being
near the middle.

The depth of sinking was from 5 ft. to 20 ft., and some of the claims
were very rich, yielding as much as £1000 per man.

The general features are a main rocky range, running from north to
south, of which Mount Gawler, near the south end, attains a height
above the sea of 1789ft. ‘This range is flanked on either side by
patches of Tertiary deposits, on the spurs between which the gullies
descend gently into Malcolm’s Creek on the east, and through steep
rocky gorges into the Little Para, Gould’s and Tenafeate Creeks on the
west. The north end of the reserve, in Barossa, is divided from that
in Para Wirra by the deep rough gorge of the South Para River. Here
the main ridge runs north-west and south-east, following the course of
the river, and being capped on its highest part by Tertiary beds, with
its small steep gullies running south into the Para River, and north
down a gentle incline into the Yetti Creek.

The rocks of this district are supposed to be of Lower Silurian age,
from their lithological resemblance to those of the Victorian goldfields,
although from their highly metamorphic appearance, and no fossils
having been found, it is impossible to say decidedly of what age they
are. In several places intrusive granite dykes are met with, and in
one particular line, from Malcolm’s Creek to Mount Gawler, they are
very frequent.

These rocks consist of metamorphic argillaceous and micaceous
schists, slates, sandstones and grits, granite, gneiss, hornblende schists,
mica schist and quartzites with granite, greenstone, and felspathic
dykes. As a rule they have a uniform strike of about 20° east of
north, and dip to the eastward from 35° to 70°; the only exception to
this rule seems to be near the Bismarck diggings, where the dip is 70°
west in two places; but this is probably caused by local agency, as it
does not extend far.

Nearly all the rocks of this district, especially on the ridges, have
so highly weathered an appearance, and are so decomposed, that they
might often be taken for Tertiary cements, particularly some coarse-
grained metamorphic granites, which contain a great deal of iron. The

Reviews—Geological Survey of S. Australia. 279

only place where the rocks are not highly altered is along the Yetti
Creek, where they consist of sandstones and slates.

Pliocene Leads, Deep Leads, or made ground.—During the Tertiary
period, the main range was already elevated considerably and two
main streams flowed, one on each flank, into which small gullies pro-
bably ran. Both these creeks flowed north, as is proved by the level
of their old beds descending in that direction. The one on the east
side seems to have risen somewhere near Mount Gawler, thence flowing
in a northerly direction, its course being now traced by a few out-lying
patches of made ground, and by a general line of low country crossing
the present creeks.

The other had its rise somewhere to the southward, and passed on
the west side of Mount Gawler, and flowed northward towards the
Humbug Scrub, where, at the head of Leg of Mutton Gully, it was
joined by the eastern stream. Thus increased in size, it flowed across
the present river to the Barossa goldfield, and so on in a north-westerly
direction to Gawler, where it discharged itself into the sea. This is
deduced from the position of outlying patches of Tertiary gravel, sand,
and clay (marked yellow on the map), which have escaped denudation.

These deposits constitute the old gold drifts from which a consider-
able amount of gold has been obtained in Barossa, and a small amount
in Para Wirra. As the payable portion of these gold drifts can only
be ascertained by sinking shafts—often through hard conglomerate,
the gold occurring in gutters beneath—a considerable amount of labour
has to be performed before a run of gold is struck; in consequence,
a large area consisting of patches of this Pliocene Tertiary has not yet
been prospected by the gold miner. Here and there a hole has been
put down, but only in a random manner; and the ground still remains
unproved,

The patches of old gold drift, which are known as ‘made hills,”’
are generally characterized by ferruginous sandstone and conglomerate
capping, called cement, which being very hard, has protected the
softer beds of sand, pipeclay, and gravel, from being washed away.

In some cases the lower beds have been cemented, in which case
crushing mills had to be employed to obtain the gold.

Para Wirra Gold Reefs.— General Notes.

The Lady Alice reef has only been worked to a depth of about
160 ft., and is well worth being farther prospected below that level,
considering the richness of the stone already raised and the shallow
depth from which it was obtained.

The various reefs and veins which are at the present time being
prospected on the Young Australian property show good prospects of
gold on and near the surface. They are worthy of a more systematic
and extensive examination by means of shafts.

An examination of the map will show what a comparatively small area
of that occupied by Tertiary deposits of older gold-drift has been
prospected for gold. Shafts have been sunk here and there. Some of
these have not been bottomed, z.e. have not reached the bed-rock ;
others have bottomed on high ground, and the run of gold has not
been immediately struck, consequently operations have been suspended

280 Reports and Proceedings—

forthwith. Some of the gullies between the patches of older gold-
drift should be prospected for gold washed out of the ‘‘lead”’ across
the course of which they have been eroded. Where these gullies are
deeply cut into the bed-rock, an opportunity is afforded of testing the
junction between the bed-rock and the Tertiary drift by drives or
tunnels. In other places, where the country is flat, trial shafts will
be necessary to prove the auriferous nature of these deposits.

The bed of the South Para River should contain payable alluvial
gold, as a large area of Tertiary gold-drift, which at one time was
continuous, from Para Wirra into Barossa, has been denuded by the
river, and the gold it contained sluiced down and re-deposited in its
valley.

Mr. Selwyn, in his ‘Geological Notes of a Journey in South
Australia from Cape Jarvis to Mount Serle,” in 1859, recommended
the testing of parcels of quartz from the reefs, and a search for gold
in the Tertiary gravels of the Mount Crawford district, ten years before
gold was found.

The information referring to the history of the diggings, depth of
shafts, etc., has been obtained from Messrs. Goddard, Barkla, Dawes,
Turner, Trenowden, Smith, and Bayley, residents of the district.
That relating to the yield of gold and copper from the Lady Alice
mine has been supplied by Mr. W. R. Lewis, who was secretary to
the company from 1873 to 1879, and Mr. G. C. Faid.

The Report contains a summary of the results of all the gold work-
ings in both the Barossa Gold-reefs and those of Para Wirra, and is
accompanied by an excellent map, prepared by H. P. Woodward,
F.G.S., Assistant Government Geologist. The Report is dated
December 10th, 1885.

ieee Ole eS AUN) 2 OCD ENG; S=

——>——_
I.—Gerotocgicat Society oF Lonpon.

I.—April 21, 1886.—Prof. J. W. Judd, F.R.S., President, in the
Chair.—The following communications were read :

1. “On a certain Fossiliferous Pebble-band in the ‘ Olive group’
of the Eastern Salt Range, Punjab.” By A. B. Wynne, Esq., F.G.S.

The principal object of this paper was to oppose the views recently
published by Dr. Waagen as to the age of certain boulder-beds in
the Salt Range of the Punjab. By that author these beds had been
considered contemporaneous with each other, and assigned to the
epoch of the Coal-measures, in consequence of the discovery by Dr.
Warth of Carboniferous fossils, especially Australian forms of Conu-
laria, in nodules restricted to a particular layer in the upper part of
a boulder-bed in the eastern Salt Range. Mr. Wynne adduced
evidence to show that the fossils in question occur, not in concretions,
as supposed by Dr. Waagen, but in pebbles evidently derived from
an older series; and consequently there was no proof that the
boulder-bed in question was older than the Cretaceous Olive beds
with which it had hitherto been associated.

The principal boulder-beds in the Salt Range were then briefly

Geological Society of London. 281

noticed; those beneath the Carboniferous Limestone west of the
Indus, those near Amb and Sakesir peak, associated with the “ purple
sandstone,” ‘‘ Obolus-beds,” and “speckled sandstone,” and those in
the eastern portion of the Salt Range, amongst the beds of the
“Salt pseudomorph zone” and “Olive group,” being successively
passed in review, and their relations to overlying and underlying
strata explained. It was shown that boulder-beds and conglomerates
containing pebbles and boulders of the same crystalline rocks are not
confined to one horizon.

In conclusion, the resemblance of the rock, of which the pebbles
containing Conularia, etc., were formed, to that forming some of the
“ magnesian sandstone” and ‘“ Obolus-beds,” was pointed out, and it
was suggested that the pebbles in question may have been derived from
representatives of those beds formerly existing to the southward.

2. “On the Phosphatic Beds in the Neighbourhood of Mons.” By
M. F. L. Cornet, For. Corr. G. 8.

The beds are situate in the province of Hainaut, near the town
of Mons (Belgium) ; the workings have increased of late years, and
in 1884 yielded 85,000 tons of phosphate.

They occur in the Upper Cretaceous, which is exceptionally well
developed in the district, filling a trough in the Carboniferous rocks,
and itself denuded for the reception of Tertiary and Quaternary beds.

Omitting all Cretaceous groups below the middle of the fifth stage,
the following is the sequence of the Cretaceous beds which contain
the phosphatic series :—

C. Tufaceous Chalk of Ciply, with the Poudingue de la Malogne at

its base.

D. Brown Phosphatic Chalk of Ciply.

E. Coarse chalk of Spiennes.

F’. White chalk of Nouvelles.

F is a pure white chalk with some flints and contains Belemnitella
mucronata, Rhynchonella octoplicata, Terebrutula carnea, Ananchytes
ovatus, etc.—an horizon well known throughout North-western
Europe. Series E and D represent one geological horizon, charac-
terized by Ostree, Brachiopoda, etc., in great numbers, but also
containing Belemnitella mucronata, and lying between two distinct
planes of erosion.

The Brown Phosphatic Chalk (D), which forms the Upper division
of the series, is about 70 feet thick, and may be described as con-
sisting of three parts ; the upper is tolerably pure carbonate of lime,
but in its lower portion becomes charged with brown granules mainly
consisting of phosphate of lime; these continue to increase towards
the central or main phosphatic mass, which is also highly fossili-
ferous in places. This central portion constitutes the main phos-
phatic beds, but the amount of phosphoric acid (dry) is not more
than 12 per cent.

Hence, it is necessary to increase the richness in phosphate of
the deposit in order that it may be available for conversion into a
superphosphate. This may be done by mechanical means.

But nature has already partially anticipated this process, and the

282 Reports and Proceedings—

result has been a deposit known as “rich phosphate,” containing
about 25 per cent. of phosphoric acid. This occurs in wide cracks
and holes in the ordinary phosphatic chalk. It usually occurs as
a fine sand-like powder, and is evidently the result of the action
of carbonated waters upon the phosphatic chalk, whereby the
amount of carbonate of lime is reduced. This is especially the case
where the phosphatic chalk is not protected by the tufaceous chalk
of Ciply, but is only covered by Tertiary or Quaternary beds.

The author calculates that each square foot of the phosphatic
basin, which he estimates approximately at five miles by three, contains
355lbs. of tribasic phosphate of lime. Finally he estimates how
the phosphatization of the chalk may have been brought about.

IL—May 12, 1886.—Prof. J. W. Judd, F.R.S., President, in the
Chair.—The following communications were read :—

1. ‘On the Maxilla of Zguanodon.” By J. W. Hulke, Esq., F.R.S.,
F.G:S.

Two fragments, together representing nearly the entire left maxilla
of a species of Jyuanodon, have been found at Cuckfield, the locality
whence the first tooth of the genus was obtained by Dr. Mantell, about
1820. These fragments, measuring together 29 centimetres, and ex-
hibiting 19 alveoli in the dentary border, were described in the paper.
It was shown that the upper jaw in question probably belonged to
Tguanodon Mantelli. In addition to the detailed characters described,
the maxille of Zguanodon and Hypsilophodon were compared, and their
distinctions explained.

2. ‘‘ Notes on the Distribution of the Ostracoda of the Carboniferous
Formations of the British Isles.” By Prof. T. Rupert Jones, F.R.S.,
F.G.8., and J. W. Kirkby, Esq.

Although all the Ostracoda of the Carboniferous formations are not
yet described, there are 170 species and notable varieties known,
belonging to 33 genera of 9 families. About 25 of these species,
not yet described, but determined by the authors, are introduced
into their lists as giving a fuller idea of the value of this manifold
Crustacean group.

In the first place they referred to the classification of the Carbon-
iferous strata in Scotland and in England, according to the local dif-
ferences, taking in succession ‘Scotland West,” ‘Scotland East,”
‘‘England North, with the Isle of Man,” ‘England Central and
South, with South Wales,” as the several districts from which they
have obtained good groups of Ostracoda from different members of the
Carboniferous series.

In Fife, the lowest local Carboniferous strata contain Beyrichia sub-
arcuata; higher up come in Carbonia fabulina, C. Rankiniana, Bairdia
mitida and Leperditia Okeni ; the last, accompanied by other species,
occurs throughout this lowest series, in which the record is more com-
plete than in Midlothian and Linlithgowshire, where the same species
also occur. In Dumfriesshire and Ayrshire Leperditia Okeni and L.
subrecta have been found in beds even lower than the above mentioned,
and are therefore probably the oldest Carboniferous Ostracoda; other
species accompany them higher up, and in Roxburghshire some localities

Geological Society of London. 283

of the Carboniferous-sandstone series are very rich in species. The
Carboniferous-Limestone series of S.W. Scotland has been highly
productive of Ostracoda, particularly the shales of the lower beds; 36
species are common or characteristic. The middle or coal-bearing
portion has yielded but few, chiefly Leperditia Youngiana, one Beyrichia,
Carbonia fabulina, and C. Rankiniana. The Upper-Limestone group
contains many recurrents from below and a few others, including
Youngia rectidorsalis (MS.). The Millstone-Grit equivalents have no
Ostracoda; but the overlying Coal-measures are rich in Carbonie,
with a few others, such as Cypridina radzata.

A great variety of genera and species come from beds at or near the
base of the Scar Limestone and its equivalents in North Lancashire,
Westmoreland, Cumberland, and Northumberland. The Calcareous
shales of the Yoredale have several interesting forms, including Phrea-
tura concinna (MS.); none from the Millstone-Grit.

The Lower Coal-measures give Beyrichia arcuata and Carbonia, sp.
The middle beds have B. arcuata and Carbonia fabulina, common;
rarer, C. Rankiniana, C. secans, C. scalpellus, C. Wardiana (MS.), and
Philomedes elongata. In the Upper Coal-measures B. subarcuata re-
appears; and in the Sprrorbis-limestone Leperditia inflata is the latest
Carboniferous Ostracod in England.

In Northamptonshire the deep Gayton boring (at 730 feet) has given
Kirkbya variabilis, K. plicata, Bythocypris sublunata, Macrocypris
Jonesiana, Cytherella extuberata, and C. attenuata, all but one belonging
to the Lower-Carboniferous series. In Salop, South Wales, and Somer-
set the Carboniferous Limestone has yielded several good species of
Leperditia, Kirkbya, Moorea, Bythocypris, Bairdia, ete. Carbonia
Agnes and C. Eveline belong to the South-Welsh Coal-measures.

The distribution of the Carboniferous Ostracoda in Ireland requires
further work; but the Lower-Carboniferous Shales and the Mountain
Limestone near Cork and elsewhere are very rich, as are also some
parts of the latter in the Isle of Man.

The Ostracoda of the Permian formation were then treated of in
relation to their Carboniferous allies, and the range of the British
Carboniferous Ostracods in Europe and North America was noticed in
some detail.

The results of the examination were shown in two extensive tables.

_ 8. ‘Note on some Vertebrata of the Red Crag.” By R. Lydekker,
Esq., F.G.S8.

This communication contained briefly the results of a re-examina-
tion of the specimens from the bone-bed of the Red Crag in the British
and Ipswich Museums, a series of casts from the latter having been
added to the former. The forms noticed were Hyena striata, with
which H. antiqua and H arvernensis were considered probably identi-
cal; Mastodon, of which the author thought three species, I. arver-
nensis, IL. longirostris and If. Borsoni, were represented ; Sus, of which
two forms, the larger probably S. erymanthius or S. antiquus, the
smaller S. paleocherus, had been detected; a Tapir, which was
probably Zapirus arvernensis or T. elegans rather than TZ. priscus ;
Tipparion gracile; a Rhinoceros referable to the hornless A. enersiwus
rather than to L. Schleiermachert, though the latter probably also

284 Reports and Proceedings—

occurred; a species of Albatross (Diomedea) represented by a right
tarso-metatarsus, and the associated proximal phalangeal bone of the
tourth digit.

4. “The Pleistocene Succession in the Trent Basin.” By R. M.
Deeley, Esq., F.G.S.

The author, after referring to the previous publications on the subject,
proceeded to notice the leading characters of the greatly developed
Pleistocene deposits in the area drained by the Trent river and its
tributaries. He proposed to classify the beds in question under
three divisions, comprising the following stages. The beds of the
lowest division were distinguished from those of the middle and upper
by the absence of Cretaceous rock-débris.

Early Pennine Boulder-clay.
OtpER PLEISTOCENE. | Quarta Sand.
Middle Pennine Boulder-clay.
Melton Sand.
Mipp.E PLEISTOCENE. Great Chalky Boulder-clay.
. ( Chalky Sand and Gravel.

Interglacial River-alluvium.

Nig PROC, { Later Pennine Boulder-clay.

Each of the stages was then described separately, with details of
exposures and sections throughout the area.

The Early and Middle Pennine Boulder-clays, which closely resem-
bled each other, were regarded as composed of materials derived almost
entirely from the Derbyshire mountains, but with a slight admixture,
to the westward, of erratics derived from Scotland and Cumberland.
The latter were probably brought from those counties by an ice-stream,
the main materials of the deposits having been transported from the
Pennine chain by glaciers, and deposited in the partially submerged
valley of the Trent. The intermediate quartzose sand was deposited
in the sea during an intercalated warmer age of considerable sub-
mergence.

The Middle Pleistocene deposits, distinguished from the earlier by
containing large quantities of chalk and flints derived from the north-
east, were apparently formed at a time when the level of the Trent-
valley area was lower than that of the Cretaceous tracts in Lincoln-
shire and Yorkshire. The Great Chalky Boulder-clay was chiefly
a ground-moraine formed beneath an ice-sheet on land, but in places
presented signs of aqueous origin. The Melton sand, below, in which
Cretaceous detritus first appeared in abundance, consisted of stratified
sands with occasional beds of gravel or loam, and indicated a less
extreme temperature. In West Staffordshire the gravels and sands
probably represented the entire Middle Pleistocene deposits, no great
Chalky Boulder-clay being found, and in this area fragments of marine
mollusca were of frequent occurrence. ‘The Chalky Gravel was also
a marine deposit, and, like the Melton Sand, was probably formed when
the temperature was rather milder than it was during the deposition of
the Great Chalky Boulder-clay.

In the Newer Pleistocene epoch re-elevation of the Trent valley and
of the Pennine chain appeared to have again produced a change in the
direction from which the materials of the deposits were derived. The

Zoological Society of London. 289

Interglacial Alluvium was of freshwater origin, but the admixture of
Scotch and Cumbrian detritus with that derived from the Pennine range
indicated that glaciers from the north again reached the Trent area.
A colder age succeeded, during which the Later Pennine Boulder-clay
was formed, partly of local materials, partly of erratics from the
Pennine range, mixed with a few from Cumberland and even from
Wales. This deposit was almost entirely unstratifiel, and consisted
largely of moraine detritus, the ice-sheets having disturbed and re-
arranged the earlier deposits and mixed them with rock-detritus from
the neighbourhood. To this later ice-sheet was attributed the contor-
tion so frequently observed in the Older and Middle Pleistocene deposits.
Reasons were given for the opinion that such contortions were due to
ice- and not to soil-cap motions or their later agencies.

5. “On the Existence of a Submarine Triassic Outlier in the
English Channel off the Lizard.” By R. N. Worth, Esq., F.G.S.

Attention was called to the frequent occurrence of sandstone
fragments in a certain part of the English Channel, brought up by
the fishermen’s ‘‘long lines.’”? The evidence favours the idea that
these rocks are im situ.

A list of the specimens found, with bearings and distances, was
given; they consist of red, and sometimes greyish sandstones, mostly
soft, also marls, ‘‘ potato stone,” and nodules of Triassic trap. The
affinities are with the Keuper of Devon. The position deduced from
the observations is about 10 miles S.K. of the Lizard, and beyond the
30-futhom line. This submarine outlier is larger than any outlier on
the mainland of Devon or Cornwall, and carries the English Trias
nearly 50 miles further to the 8. W.

ZooLoGicaL Society oF Lonpon.

April 20th, 1886.—Prof. W. H. Flower, LL.D., F.R.S., President,
in the Chair.—The following communication was read :—

3. “On the Relations of the Mandibular and Hyoid Arches in a
Cretaceous Shark (Mybodus dubrisiensis, Mackie).” By A. Smith
Woodward, F.G.S. Communicated by the Secretary.

In this paper, the author described the mandibular and hyoid
arches of Hybodus dubrisiensis, as exhibited in a fossil from the
Chalk of Kent, preserved in the British Museum. The cartilages
are all in an admirable state of preservation, and show that the
Cretaceous Hybodont skull made a near approach to the primitive
condition termed “amphistylic” by Prof. Huxley (Proc. Zool. Soc.
1876, p. 41). The fossil jaws are also interesting from their close
resemblance to those of the Notidanide, which are the most
amphistylic of living vertebrates ; and the pterygo-quadrate cartilage
exhibits the facette for a post-orbital articulation with the cranium,
which forms so characteristic a feature of the existing family just
mentioned. The hyoid elements are likewise remarkably slender.
The fossil further shows traces of well-calcified vertebre, which are
astero-spondylic in structure, and are well seen in a second specimen
in the National Collection. The latter fact is of peculiar interest,
since a fossil from the Lias, with teeth generically indistinguishable,

286 Correspondence—Prof. Edward Hull.

affords distinct evidence of a persistent notochord, with the arches
alone calcified; and as three Hybodont pterygo-quadrates of Liassic
and Wealden age appear to be destitute of an articular facette where
contiguous with the post-orbital region of the cranium, there is also
a corresponding indication of progressive development in the
mandibular arch. The author also pointed out that the differences
between the anterior and posterior teeth are more marked in H.
dubrisiensis than in any of the earlier forms of which satisfactory
remains are known, and concluded by suggesting that future research
in regard to structures other than teeth will probably lead to the
generic subdivision of the multitudinous forms hitherto grouped
under the name of Hybodus.

CORRESPONDENCE.

eed
THE SURVEY OF WESTERN PALESTINE.

Str,—Permit me to offer two or three observations as regards
matters of fact in reply to the criticisms contained in the review of
the “ Geological Memoir on Arabia Petrzea and Palestine.” The
reviewer says (p. 229): “ Fossils appear to be rare throughout the
[ Cretaceo-Hocene] series—the Expedition does not seem to have
discovered any in fact.” This is really not so. We brought home
a good many specimens, and I placed them in the hands of Professor
Sollas (who was so good as to describe the Carboniferous forms)
for determination. But owing to causes, doubtless quite sufficient,
I did not receive the specimens back till too late for publication.
Since then Prof. Sollas has informed me that there were no new
forms amongst them, as they had already been determined by Lartet
and others. It is only known to those who have made the attempt,
how difficult it is to collect fossils and specimens when on a journey
on camel- or horse-back, through the desert under a temperature of
80° Fahr. in the shade, and 112° in the sun.

Again, in speaking of the “ Calcareous Sandstone of Philistia,”
the reviewer states, “‘No thickness is assigned to this deposit.” I
have only to say in reply that owing to the extent to which Philistia
is overspread by the deposits of the 220 raised sea-bed—and with
loam—the sections of this sandstone are very rare; nor had we
any opportunity of observing the junction of the sandstone with the
Nummulite-limestone. Both thickness and relations, as they are in-
ferred by me, may be gathered from the horizontal section, No. 1,
across Palestine. It is not improbable the formation has a thickness
of 800 to 400 feet. The reviewer seems to have overlooked the fact
that this sandstone appears to have its equivalent in the series at
Mokattam Hill, near Cairo, described by Schweinfurth.

3. As regards the question, “ What has become of the materials
which have been removed from the surface of the drainage area of
the Dead Sea?” (p. 231). As this basin never had an outlet, there
can be only one answer (which appears to me self-evident) —that
they are either used up in the terraces—or are spread over the floor
of the Dead Sea and Jordan-Arabah Valley. The bottom both of

Correspondence—Prof. Joseph Le Conte. 287

the Dead Sea and of this valley are covered by alluvial deposits.
What the thickness of these may be no one knows; nor can the
question of the depth to the solid rocks below the alluvial materials
be solved except by extensive boring operations. In my opinion the
depth is very great; and if this be so, the answer to the question of
the reviewer is plain,—at least, this is the only answer I conceive
possible.
Dunrannacuy, 12th May, 1886. Epwarp HUtt.

THE DEVELOPMENT OF THE NORTH AMERICAN CONTINENT.

Str,—There are no questions in Geology more important and more
fascinating than those of Palzo-geography. All geologists must be
grateful to Prof. Hull for the light he has shed upon them. But,
also, there are no questions which are more difficult, and the solution
of which is more illusory. I would not again trouble you on this
subject except to correct what seems to me.a grave misconception on
the part of Prof. Hull,’ which lies at the basis of nearly all the
difference between us.

He refers to an ideal section of the Paleozoic rocks on p. 288 of
my ‘‘ Hlements of Geology”’ (being a section from Canada through
New York to Pennsylvania), as indicating continued subsidence of
sea-bottom and retreat of shore-line northward during the Palzeozoic
period. This interpretation is the very opposite of that usually given
by American geologists. Perhaps the mistake, if it be one, is partly
due to bad drawing. In order to bring all the Paleozoic strata
within the compass of a small figure, the southward dip is enormously
exaggerated. In fact, the strata are nearly level, the average dip
being probably not more than 15-20 feet per mile. The successive
appearance of younger and younger rocks as we go southward is
supposed by all American geologists to indicate a gradual elevation
of the Canadian land-mass of that time, and a consequent advance of
the shore-line southward with steady increase of land. This is seen at

once if the section be drawn with smaller dips and leaving out
details (Fig. 1).

\\\
KW
=) WN

Fie. 1.—Generalized N.E. and S.W. section from Canada through New York to

Pennsylvania. A. Archean. P. Primordial. .S8. Lower Silurian.

U.S. Upper Silurian. D. Devonian. §.C. Sub-Carboniferous. abcde
successive shore-lines. 7 J 2” J’ 7” successive sea-levels.

The western shore-line of the eastern land-mass was, on the con-

trary, nearly stationary, and hence the prodigious thickness of Palzo-

zoic sediments in the Appalachian region. Even here, however,

1 See Prof. Hull’s letter, Gron. Maa. April, 1886, p. 189.

288 Correspondence—Prof. Joseph Le Conte.

whatever movement of shore-line there was, seems to have been
westward with increase of land.

Two other points I briefly touch. Prof. Hull thinks that I do not
recognize sufficiently, if at all, his most important point, viz. ‘the
increase of thickness of sediments to the N.E. and E., and their
attenuation and replacement by limestone in the opposite direction.”
If I did not lay stress on this, it was only because I supposed it
generally recognized, although Prof. Hull brings it out in a very
striking way in his figures. No one has emphasized these facts, and
their significance as showing a large land-mass to the north-east and
a wide ocean to the south-west, more than I have.!

Again, in my previous communication * I said, ‘There is no reason
why the eastern land-mass, which sufficed to contribute 30,000 ft. of
Silurian and Devonian sediments, should not have been sufficient to
contribute the much smaller amount of Carboniferous sediments.”
Prof. Hull thinks this a begging of the question at issue. Tor, says
he, “the narrow strip of land allowed by Prof. Le Conte was quite
insufficient to produce 30,000 ft. of conformable sediments.” I can
only say in reply that Prof. Hull’s map of Silurian times led me
astray: for this shows just such a land-mass as I suppose, while his
map of Carboniferous times shows a very much greater land-mass.
I suppose, now, however, that he imagines this land-mass to have
increased on its eastern side through Silurian and Devonian times.
If so, it must have increased very rapidly, for the Silurian alone is
20,000 ft. thick in the Appalachian region. JoszepH Le Contr.

PERMANENCE OF CONTINENTS & OCEAN-BASINS, WITH SPECIAL
REFERENCE TO THE FORMATION AND DEVELOPMENT OF
THE NORTH AMERICAN CONTINENT.

Sir,— Will you allow me to make a correction ? Prof. Chamberlin
has kindly drawn my attention to the fact that in my original com-
munication to you on this subject * I have misrepresented him, and I
wish therefore to acknowledge my error. The map on p. 62 of
Prof. Chamberlin’s work on the Geology of Winconsin was not
intended, as I supposed, as a map of Archean areas, but really
as a map of land during a portion of Archean times, viz. (if I
understand him) at the beginning of the period of Huronian
sedimentation. Iwas misled by its great resemblance to the usually
recognized map of Archean areas. The confusion of thought to
which I referred does indeed exist, but Prof. Chamberlin is not an
example of it.

Let us hope that Prof. Chamberlin will give us more fully his
mature views on this so obscure and yet so important subject. No
one is more competent than he to write with authority on the
subject. JosupH Lr Conte.

BerxeLey, Catirornia, May 3, 1886.

1 Am. Jour. vol. iv. p. 463, 1872. Elements of Geol. p. 289.

2 See Grou. Mac. March, 1886, p. 100.
3 Gzot, Maa, 1886, Dec. III. Vol. III. p. 97.

Geol.Mag.1886. Decade IIL. Vol. I. Pl, VII.

TEAINaeacleexs del,
ATHollick lids ic West, Newman &Co,tmp.

Desmidopora alveolaris. Nicholson

THE

GEOLOGICAL MAGAZINE.

NEWeSERiEoe: DECADE: Il VOL emit
No. VII.—_JULY, 1886.

Ouse AINE 7a SR Oya Gast}

——+—__

I.— On Desuipopora atvrocaris, Nicu., 4 New GENUS AND
SPECIES OF SILURIAN CoRALS.

By H. Atteyne Nicuotson, M.D., D.Sc.,

Regius Professor of Natural History in the University of Aberdeen.
(PLATE VIII.)

DESMIDOPORA, gen. nov.

Gen. Char.—Corallum composite, with an epithecate base, the
corallites subpolygonal, and indissolubly united by the coalescence
of their walls. The corallites are sometimes circumscribed, but they
are for the most part more or less extensively connected by deficiency
of their walls in particular directions, so as to give rise to sinuous
rows of serially-united tubes. The calices, like the corallites, may
be circumscribed, but are mostly in the form of vermiculate grooves
corresponding with the serially confluent corallites. The calices
are not oblique, nor are the corallites reclined. Mural pores are
numerous and well developed. Septa and septal spines are wholly
wanting. The tabule are numerous, being simple and complete in
the circumscribed corallites, but becoming vesicular in the rows of
serially confluent corallites. New corallites are produced by fission.

I have found it necessary to propose the above generic name for
a remarkable coral from the Wenlock Limestone of Dudley, for
specimens of which I am indebted to the kindness of Mr. William
Madeley, whose experienced eye had recognized that they belonged
to an unusual type. In general aspect, the specimens show resem-
blances to the laminar forms of both Alveolites and Chetetes, as also
to Labechia; and it was to the last of these that I was at first dis-
posed to refer them. A microscopical examination has, however,
shown that they are most nearly related in reality to Alveolites ; the
presence of numerous mural pores, quite of the type of these struc-
tures in Favosites itself, proving that they are indubitably referable
to the group of the Favositide. The specimens, however, exhibit
the following structural peculiarities, which preclude our referring
them to any previously-named genus of Favositoid Corals with
which I am acquainted :-—

(1.) The primordial wall of the corallites is entirely wanting,
adjoining visceral chambers being thus separated by an apparently
single wall, as is the case in the genus Chetetes, Fischer.

DECADE I1I.—VOL. III.—NO. VII. 19

290 Prof. H. A. Nicholson—On a New Silurian Coral.

(2.) A certain number of the corallites may have their visceral
chambers definitely circumscribed ; but others are united in serial
rows by deficiency of their walls on corresponding sides. These
rows are sinuous; and the calices assume, therefore, largely the form
of winding labyrinthine grooves (Pl. VIII. Fig. 2).

(8.) No septa or septal spines are present. In examining the
surface of well-preserved specimens one might be easily led to sup-
pose that irregular septa were here and there developed; but these
apparent septa are really only the inward projections of the walls of
the corallites marking the boundaries of the separate tubes in the
serially united rows.

(4.) In the completely circumscribed corallites, the tabule are
simple, and are either horizontal or are curved with their convexities
pointing towards the calices. On the other hand, in the serially
united corallites the tabulee become vesicular by reason of their con-
fluence in adjoining tubes.

(5.) The mode of increase is by fission of the old tubes.

The characters above enumerated form, as before remarked, a com-
bination so peculiar, as to render it impossible to refer the specimens
possessing them to any recognized genus of the Favositide. I there-
fore propose for their reception the new genus Desmidopora. 'The
essential distinction between this genus and all the normal genera of
the Favositidee is the fact that in Desmidopora the mode of growth is
fissiparous, and that many of the corallites are thus confluent in
serial rows. Apart, however, from this fundamental distinction,
there are minor features which separate the present type from the
normal genera of the Favositide. Thus, in Favosites itself there is
a persistent primordial wall to the corallites, and septal spines are
usually present; whereas in Desmidopora the walls of adjoining
tubes are indistinguishably fused together, and no traces of septal
structures can be detected. In Pachypora, Lindstr., again, not only is
there a persistent primordial wall to the corallites, but each visceral
chamber is contracted by the development of a special secondary lining
of sclerenchyma. The genus Alveolites, Lam., is separated by the
minor peculiarities of the oblique form of the calices and the presence
of septal teeth or ridges, while the mural pores are large and
uniserial. Lastly, the genus Laceripora, Wichw., makes a nearer
approach to the present type than is the case with any other known
genus of the Favositide. Apart, however, from the fundamental
point of the fissiparous mode of increase in Desmidopora, the genus
Laceripora, Hichw., is further separated from the latter by the per-
sistent primordial wall of the corallites, the possession of distinct
septa, and the fact that a special secondary lining of sclerenchyma is
developed in the tubes in the peripheral region of the corallum. In
tangential sections of Laceripora the visceral chambers of adjoining
tubes often become connected by deficiency of the intervening wall ;
but this is not due—as might easily be imagined—to fission of the
tubes. On the contrary, it is simply due to the fact that the section
happens to cut at such points across the very large mural pores with
which the corallites are provided.

Prof. H.A. Nicholson—On a New Silurian Coral. 291

Very closely related to Zaceripora, Hichw., if indeed really generi-
eally distinct from it, is the genus Somphopora, Lindstr. (‘‘ Ober-
silurische Korallen von Tshau Tién,” p. 51, pl. vii. figs. 2—5); and
this, therefore, also presents some resemblances to Desmidopora.
In Somphopora, however, the primordial wall of the corallites is
persistent, and well-developed septal structures are present, while
the mural pores are of very large size, points quite sufficient to prove
its distinctness from Desmidopora.

Beyond the limits of the Perforate Corals, the only genus with
which Desmidopora need be compared is Chetetes, Fischer. In
general aspect there is a decided resemblance between Desmidopora
and some of the species of Chetetes; and the fissiparous mode of
increase is a structural feature common to the two genera. There
are, moreover, species of Chetetes (such as C. Htheridgit, Thoms. sp.)
in which the corallites in the process of fission become often laterally
elongated, and the calices are therefore commonly compressed and
sinuous. The presence of numerous well-marked mural pores in
Desmidopora is, however, of itself sufficient to separate the present
genus wholly from Chetetes, Fischer.!

The only species of Desmidopora with which I am acquainted
occurs in the Wenlock Limestone of Britain, and possesses the fol-
lowing characters :—

D&sMIDOPORA ALVEOLARIS, Nich.
Latbechia alveolaris, Nich., Mon. Brit. Stromatoporoids, p. 83 (name only), 1886.

Spec. Char..—Corallum in the form of a laminar expansion, which
may reach half a foot in diameter, and which varies in thickness
from less than a centimetre to two centimetres. The corallum
was attached to some foreign body by a peduncle, and the base is
covered by a concentrically wrinkled epitheca (Pl. VIII. Fig. 1). The
corallites are directed approximately at right angles to the basal
epitheca, and are usually from 2 to 1 millim. in diameter. The
calices are variable in shape, but are never oblique or crescentic in
form. Parts of the surface generally show many of the calices as
as subpolygonal, definitely circumscribed apertures (P1]. VIII. Fig. 8) ;
while in other parts the calices have become more or less extensively
confluent, and have the form of winding and sinuous grooves (PI. VIII.
Fig. 2). The tabule are numerous, mostly convex, with their con-
vexities turned upwards, and generally about half the diameter of
the corallites apart. Very often they are placed at approximately
the same level in adjoining tubes; and in the serial rows of
corallites they become vesicular. Mural pores are numerous, but
not of unusually large size.

' Mr. James Thomson has described mural pores as occurring in Chetetes Ethe-
ridgiv, Thoms. sp., C. septosus, Flem., O. depressus, Flem., and C. hyperboreus,
Nich. and Eth., jun.; and he has therefore referred these species to Alveolites (Proc.
Phil. Soc. Glasg. 1881). I have, however, examined numerous specimens and
microscopic sections of all these species, and am quite satisfied that the walls of the
corallites are in all of them imperforate. Indeed, the figures given by Mr. Thomson
himself show conclusively that the structures which he has described as mural pores
could not possibly be of this nature.

292 Prof. H. A. Nicholson—On a New Silurian Coral.

The structure of Desmidopora alveolaris can be readily made out
by means of thin sections, if these happen to be taken from a
specimen in which the skeleton has not been much altered by mine-
ralization. In tangential sections of such specimens (PI. VIII. Fig. 4),
the walls of the corallites are seen to be of moderate thickness, and
to exhibit no traces of the primordial wall. No traces of septal
structures are to be detected, and the visceral chambers of many of
the corallites are directly continuous in winding series. In vertical
sections (Pl. VIII. Figs. 5 and 6), the mural pores are seen at the
points where the plane of the section happens to coincide with the
walls of the corallites, and their presence is further recognized by
the common occurrence of interruptions to the complete continuity
of the walls. Where the section happens to intersect one of the
rows of confluent corallites in any direction except a directly trans-
verse one, the tabula are seen to be vesicular, but at other points
they are as a rule complete.

In other specimens the skeleton has undergone considerable
secondary change. and the appearances presented in these cases are to
a large extent different to what they are in normal examples of the
species. Thus, in such cases (Pl. VIII. Figs. 7 and 8), the walls of the
tubes are considerably thickened, and in tangential sections exhibit
a peculiar beaded appearance. The same thickening of parts of the
walls of the corallites is shown in vertical sections. The first sec-
tions which I examined were taken from a specimen which had been
mineralized in this peculiar way: and I was led from the phenomena
which they presented to regard the species as being a peculiar form
of Labechia, which I named J. alveolaris, without giving any fignre
or description of it (Mon. Brit. Stromatoporoids, p. 83). Such sec-
tions do, in fact, show a curious likeness to Labechia, and particularly
to certain specimens of LZ. conferta. It need hardly be said, however,
that an examination of sections of a well-preserved example of
Desmidopora alveolaris leaves us in no doubt as to the systematic
position of the species.

Formation and Locality.—Rare in the Wenlock Limestone of
Dudley. I am indebted for all my specimens to the kindness of
Mr. William Madeley, of Dudley.

EXPLANATION OF PLATE VIII.

Fic. 1. Under side of a broken specimen of Desmidopora alveolaris, Nich., of the

natural size, showing the epitheca.

», 2. Part of the surface of the same, enlarged six times. In the portion
figured most of the calices are confluent.

», 8. Another part of the surface of the same, enlarged six times. In this
portion of the surface a good many of the calices are definitely circum-
scribed.

», 4. Tangential section, enlarged six times. The specimen from which this was

taken is but slightly altered by mineralization.

5. Vertical section of the same specimen, enlarged six times.

,, 6. Part of the preceding section, enlarged twelve times, showing mural pores.
7. Tangential section of a mineralized specimen, enlarged twelve times. ‘The
appearances presented in this section are not at all unlike those
exhibited by some forms of Labechia.

», 8. Vertical section of the preceding specimen, enlarged twelve times. Here,

again, the appearances are very like those shown by vertical sections of
Labechia conferta, Lonsd.

Rk. D. Oldham—On Homotaxis and Oontemporaneity 298

II.—Essays on SPECULATIVE GEOLOGY.
1.—On Homoraxis AND CONTEMPORANEITY.

By R. D. Orpuam, A.R.S.M.,
of the Geological Survey of India.

N any inquiry into the history of the earth as a whole, we are met
at the outset by a serious difficulty. In human affairs a general
view of history, not confined to a single country, would be practically
impossible, were we ignorant of the relations of the various eras
from which different races reckon their dates: thus, it would be
impossible to write a connected account of the history of Europe in
the classical period were it not possible to determine the relation of
the Olympian era to that dating from the foundation of the city of
Rome. Yet the supposed case is not unlike that to which the
geologist addresses himself when he endeavours to make a connected
survey of such widely-separated regions as Europe, India, Australia,
and America.

In the supposed case of the Greek and Roman eras, there are
numerous points of contact, principally dates of battles, which,
having been recorded by both nations according to their own system,
enable us to compare the two, and so to determine what would be the
date of any event, recorded by the one, had it been recorded by the
other. But in geology we have no such points of contact; there is
a very general tendency to regard any two series of beds, in which
a few fossil forms specifically identical are found, as of contempora-
neous origin. That this view is erroneous, and that it would be
nearer the truth to say that two widely-separated beds, in which the
same forms are found, could not be of contemporaneous origin, was
long ago pointed out by Forbes and Huxley, the word homotaxis
being invented by the latter to express the relation existing. More
recently, at the Montreal meeting of the British Association, Dr.
Blanford went into the question at length, and fully showed how
erroneous is the assumption, often tacitly made, that similarity of
included organic remains indicates contemporaneity of origin of the
beds in which they are preserved.

Be it understood that I am in no way desirous of depreciating the
value of paleontological evidence; but, for the purpose of what may
be called historical geology, the merely approximate contemporaneity
indicated by homotaxis, however perfect, is by no means sufficient.
What we desire is something approaching to the accuracy of dates in
written history, rather than that vague “homotaxis” indicated by the
Stone or Bronze ages, with which we have to be satisfied in what is
known as the Pre-Historic period of human history. As long as we
are dealing only with the history of a single limited region, no serious
difficulty is likely to arise; but when we try to bring the history of,
say, Australia and Europe, into relation with each other, a doubt may
well arise as to whether beds which would be classed as Lower Car-
boniferous if they occurred in Hurope can be really considered as
of that ace when measured by European standards.

This is a question that paleontology alone can never answer

294 Rk. D. Oldham—On Homotaxis and Contemporaneity.

finally, and we are consequently compelled to search for some other
evidence which will enable us to say, in some cases at any rate, that
the beds are or are not strictly contemporaneous in their origin.
One possible means would be the traces left by a period of cold
similar to the well-known “Glacial period” of Post-Tertiary times.
That there was such a period during which an arctic climate pene-
trated into temperate regions has been amply proved, and we may,
I think, safely assume that this “Glacial” period of cold was con-
temporaneous in both hemispheres; for, whatever may have been
the cause of the colder climate which prevailed during that period,
it must have affected both hemispheres in the same manner at the
same time. .

I am not overlooking the fact that the most probable theory of the
Glacial period, that of Dr. Croll, necessitates the glaciation of one
hemisphere contemporaneously with the prevalence of a mild climate
in the other; but if we take the Glacial period as a whole, which
includes all the minor glacial and interglacial periods, we may say
that the Post-Tertiary deposits which show signs of a colder climate
than now prevails are of contemporaneous origin, wherever they
may be found. By this J must not be understood to mean that any
one particular bed in one place can be declared to be contempora-
neous with a definite bed anywhere else, but that the series as a
whole were of contemporaneous origin, thoughthe actual limits may
not have been the same in both cases.

If we can prove that similar Glacial epochs have occurred during
the sedimentary period, using the term to denote that period of the
Karth’s history which is represented by the sequence of sedimentary
formations, we shall have an important check on the palzontological
timepiece, by which we can determine whether it is fast or slow. To
prove this it will not be sufficient merely to point out that evidences
of glacial action have been detected by various observers in strata of
various ages, and in latitudes lower than those in which icebergs are
met with at the present day; but if it can be shown that, in several
widely-separated regions, and in strata which can on independent
grounds be shown to be, at least, approximately homotaxial, there
are to be found extensive indications of glacial action, which are not
seen in the beds above or below, we may safely and fairly conclude
that they all belong to a single Glacial epoch comparable to that
of Post-Tertiary times.

For this purpose I shall take that Glacial period represented by
the Talchir beds of India, the Eeca beds of Africa, and certain beds
in Australia likewise of glacial origin. I choose this particular in-
stance because the details are more familiar to me than any other,
and moreover I shall be able to place before the readers of this
MaGAzrneE some recent additions to our knowledge of the geology of
these countries.

It must be well known that there have been serious differences of
opinion regarding the age of the Indian and Australian Coal-measures,
and that this difference has practically been between the field geolo-
gists on the one hand and the paleeobotanists on the other. The former

R. D. Oldham—On Homotaxis and Contemporaneity. 295

regarded them as of Carboniferous age, or, at the latest, representing
the interval between the Paleozoic and Mesozoic eras of Hurope,
while the latter, judging only from the plant remains found with
the coal, declared it to be of Mesozoic and even of Jurassic age.

As regards the paleontological relations of these beds to each
other, and to the plant-bearing series of South Africa, the subject has
been so thoroughly treated by Dr. Blanford in his address that it
will be needless for me to enter into a repetition of the subject. I
may, however, remark that both in India and South Africa there is
a series of sedimentary formations which, if identity of fossils were
proof of contemporaneity, would have to be regarded as of contem-
porary and even coeval origin, and in both cases there are at the
lower limit of the series beds whose structure proves that they must
have been deposited through the agency of floating-ice. In Australia
there are some beds (the Bacchus Marsh beds of Victoria) which
similarly show that there must have been ice floating in large
masses on the sea beneath which they were deposited : these beds have
yielded a limited flora composed of three species of Gangamopteris,
of which one is identical with and the other two closely allied to
Talchir species.

Thus we see that in India, in South Africa, and in Australia
there are beds whose nature indicates the existence of ice floating at
or near the sea-level, in latitudes which it does not now reach, and
that, as judged by the fossil plants contained in them and in the asso-
ciated beds, they must be regarded as homotaxial. The conclusion
is well-nigh irresistible that they all belong to a single Glacial epoch,
and are consequently strictly contemporaneous in origin.

So far, I do not think any one will object to my conclusions ; they
have been foreshadowed by Mr. H. F. Blanford,’ and as far as India
and Australia are concerned by Dr. Feistmantel,? who is by no means
disposed to underestimate the value of palzeobotanical evidence, even
where opposed to every other consideration ; and so far I have been
able to accept and summarize Mr. Blanford’s address. But in extend-
ing the same line of reasoning, and in trying to determine even
approximately the true date of this Glacial period, I shall have
to enter on more disputable ground, and to refer to information
acquired since Dr. Blanford’s address was delivered.

The first point to notice is that the Bacchus Marsh beds of
Victoria are not the only instance of Glacial boulder-beds occurring
in Australia; for in New South Wales traces of Glacial action are
abundant in the marine beds below the Coal-measures. I am not
aware of any published record of this fact previous to my own notice
of the fact *; but, as long ago as 1861, the lithological resemblance,
as seen in a collection of specimens from New South Wales, between
the marine beds of the Wollongong district and the boulder-beds of

1 Quart. Journ. Geol. Soc. Lond. vol. xxxi, p. 519,

2 Proc. Geol. Surv. Ind.

3 Proc. Geol. Surv. India, vol. xix. p. 48 (1886). The substance of this paper
and of another in the Journ, As. Soc. Beng. for 1884, is incorporated in the present
essay.

296 R&R. D. Oldham—On Homotazxis and Contemporaneity.

the Talchirs, was noticed by the late Dr. T. Oldham.t. That any
special stress should have been laid on the resemblance was not to
be expected, for when the words were written the Glacial origin of
the Talchir boulder-bed had not been universally acknowledged, the
very idea of a Glacial epoch was still strange, and no one had yet
dreamed of a Palzeozoic Glacial epoch, still less of using such a con-
ception in the correlation of distant deposits. These observations
appear to have dropped completely out of sight, and when I found
that in Mr. W. T. Blanford’s reply to Dr. Feistmantel? no notice was
taken of this resemblance, although Mr. H. F. Blanford’s suggestion
that the Glacial beds of the Permian in England and the Talchirs in
India were contemporaneous is quoted, I concluded that private
information of later date had led to a modification of the views
expressed as to the lithological resemblance of the beds.

Nevertheless, when visiting Australia in 1885, I determined to pay
special attention to this point, and was not surprised, on examining
the section west of Newcastle, to find that the marine beds showed
abundant traces of Glacial action. Blocks of slate, quartzite and
crystalline rocks, for the most part subangular, are found scattered
through a matrix of fine sand or shale, which contain delicate
Fenestelle and bivalve shells with the valves still united, showing
that they had lived, died and been tranquilly preserved where they
are now found, and proving, as conclusively as the matrix in which
they are preserved, that they could never have been exposed to any
current of sufficient force and rapidity to transport the blocks of
stone now found lying side by side with them. These included
fragments of rock are of all sizes, from a few inches to several feet
in diameter, the largest I saw being about four feet across in every
direction as exposed in the cutting, and of unknown size in the third
dimension ; and I was informed by Mr. Wilkinson that in these same
beds he has seen boulders of slate, etc., whose dimensions may be
measured in yards.

It is impossible to account for these features except by the action
of ice floating in large masses,’ and I had the good fortune to dis-
cover, during the course of a short morning’s walk, in the railway
cutting near Branxton, a fragment beautifully smoothed and striated
in the manner characteristic of glacier action, besides at least two
others which showed the same feature, though obscurely. This
seems to show that the ice was of the nature of icebergs broken off
from a glacier which descended to the sea-level.

Beds of similar structure and indicating a similar mode of origin
are also found at Wollongong, south of Sydney, and in the Blue
Mountains. ‘Though these have not been traced into connection with
the marine beds west of Newcastle, the similarity of their position,

1 Mem. Geol. Surv. Ind. vol. iii. p. 209 (1868).

2 Rec. G. S. I. vol. xi. p. 148 (1878).

* Roughly speaking, it may be said to take 26 cubic feet of fresh-water ice floating
in sea-water to float a cubic foot of granite, or 14 cubic yards to float one ton. It
must be remembered that many of these fragments probably came from a distance,

and that the ice was melting all the while. These figures must be reduced by two-
fifths if the rock is supposed to be immersed,

Rk. D. Oldham—On Homotaxis and Contemporaneity. 297

fauna, and physical aspect, all leave little room for doubt that they
are of the same age. Beds of similar aspect have been described by
Mr. R. L. Jack, in Queensland. These beds—also of marine origin,
and indicating the presence of ice floating in the sea by which they
were deposited,’ contain 22 species of fossils, so far as the fauna is
known, of which 15 are also found in the marine beds of New South
Wales, and only seven have not been found to the south.

As the case stands, there are in Australia two sets of beds, both
of which indicate the presence of floating-ice in the water in which
they were deposited. One of these, the Bacchus Marsh group, is
shown by its plant fossils to be homotaxial with the Talchir group
of India; the other has yielded a marine fauna of Lower Carboniferous
facies, as Judged by Huropean standards, and a limited flora which,
however, does not show any direct relation to that of the Bacchus
Marsh beds.

I am not aware of any published attempt to correlate the Bacchus
Marsh beds with a definite horizon in New South Wales before Dr.
Feistmantel in 1880 gave it as his opinion that they were the
equivalents of the Hawkesbury Sandstones. This opinion, so far
as I can glean from his published writings, was based on the so-
called Lower Mesozoic facies of the Bacchus Marsh flora, and was
supposed to be confirmed by Mr. C. S. Wilkinson’s discovery of
glacial action in the Hawkesbury Sandstones. Mr. Wilkinson thus
describes this evidence *—“In the sections exposed in the quarries
at Fort Macquarrie, Woolloomooloo, Flagstaff Hill and other places,
may be seen angular boulders of shale * of all sizes up to 20 feet in
diameter, imbedded in the sandstone in a most confused manner,
some of them standing on end as regards their stratification, and
others inclined at all angles. They contain the same fossil plants
that are found in the beds of shale from which they have evidently
been derived. These angular boulders occur nearly always imme-
diately above the shale-beds, and are mixed with very rounded
pebbles of quartz; they are sometimes slightly curved as though
they had been bent while in a semiplastic condition, and the shale-
beds occasionally terminate abruptly as though broken off.”

It is difficult, if not impossible, to account for these appearances,
except by the action of ice in some form or other; the angular form
of the fragments of shale shows that in some manner they must
have been indurated before disturbance, and it is impossible to
account for this induration of what must then have been recently
deposited mud except by the freezing of the interstitial water. This
supposition would accord with the general nature of the evidence,
which indicates the action of ground-ice, such as is formed during
the severe winters of North America, rather than the presence of
large masses of floating-ice ; and hence does not necessarily indicate
so severe a climate as that afforded by the Bacchus Marsh beds of

1 Report on the Bowen River Coal-field, by R. L. Jack, Esq., F.G.S8., Brisbane, 1879.

2 Notes on the occurrence of a remarkable boulder in the Hawkesbury Rocks, Trans.
Roy. Soc. N. 8. W. xiii. 105 (1884).

* Which is interbedded with the sandstones.

298 Rk. D. Oldham—On Homotaxis and Contemporaneity.

Victoria, which, according to the late Sir R. Daintree, contain
“strata, mainly composed of fine mud, dotted thoughout with
various-sized, generally rounded, pebbles, and those pebbles mostly
unknown in the vicinity, and some not yet seen in place so far as
the Geological Survey has extended a minute examination! ;” further
on he says that “blocks of granite, in some instances over a ton
in weight, are found imbedded in a matrix of soft mud?;” and in
the last progress report by the Secretary for Mines in Victoria, Mr.
Murray states, on the authority of the late Sir R. Daintree, that
some of these granite boulders resemble no granite that occurs as
a rock-mass nearer than Queensland.°

This contrast in the nature of the evidence of glacial action shows
that, if this form of argument is at all admissible, it is with the
Lower Carboniferous marine, rather than with the Hawkesbury
glacial beds that we must associate those of Bacchus Marsh.

Nor can paleontology be said to support Dr. Feistmantel’s hypo-
thesis; for Gangamopteris, the only genus of plants known from
the Bacchus Marsh beds, is found neither in the plant-bearing beds,
interstratified in the Lower Carboniferous marine group, nor in the
Hawkesbury group. It has, however, been found in the intervening
Neweastle group, and one species is identical with a Bacchus Marsh
form; moreover, the only other species of Gangamopteris in the
Newcastle beds is, according to Dr. Feistmantel, closely allied to one
of the Bacchus Marsh species. ‘This fossil evidence would by many
be regarded as sufficient to prove the contemporaneity of the Bacchus
Marsh and Newcastle groups; but the beds of the latter show no
trace of glacial action, so that the former cannot be referred to that
age in face of the existence of evidence of glacial action in the beds
above and below. A reference to Dr. Blanford’s address will show
that whereas a very close relationship exists between the floras of
the Newcastle and Lower Coal-measures, there is next to none between
those of the former and the Hawkesbury Sandstones ; and I may add
that the stratigraphy of the beds appears to point to the same con-
clusion as the paleontology ; so that, as the choice lies between the
two, it is again rather with the Lower Carboniferous marine than
with the Hawkesbury group that we must associate the Bacchus
Marsh beds.

The Bacchus Marsh beds are not known to occur in conformable
contact with any other group; but there is a large tract of country
covered by an upper group of the same series, which is characterized
by the occurrence of Teniopteris Daintreei, a form which occurs in
New South Wales in the beds overlying the Hawkesbury and Wiana-
matta groups. Owing to the large area covered by more recent lava
flows, the exact relation of the two groups is unknown ; but there can
be little doubt that they are unconformable, for the Bacchus Marsh
beds are overlapped by the Teniopteris beds, which rest unconform-

1 Geological Survey, Report on the Geology of the District of Ballan, by Richard
Daintree, p. 10, Melbourne, 1866.

2 Thid., p. 10.

3 Geological Survey, Progress Report by the Secretary for Mines, p. 80, Melbourne,
1881.

L. D. Oldham—On Homotaxis and Contemporaneity. 299

ably on the older Paleozoics. This would imply a greater difference
of age than seems to obtain between the Hawkesbury and overlying
groups in New South Wales. ‘To this I may add the difference in
induration of the two, which is such that when originally surveyed,
the Bacchus Marsh beds were believed to be Devonian, and are
coloured on the original survey sheets as Upper Palzeozoic.

As a further confirmation of the opinion ventured on, I may point
to the relationship that exists between the flora of the Damudas
which overlie the Talchir group in India, and that of the Newcastle
beds, which occupy a similar position above the Lower Carboniferous
marine group in Australia.

To begin with, both floras are marked by the predominance of the
genus Glossopteris, which, in the Newcastle flora, comprises nine out
of 26 species, or 35 per cent. of the total number of species, and 19
species out of 63, or 30 per cent. of the total number of species in
the Damuda flora; of these, one species, G. browniana, is identical
in both cases, and three Newcastle species, G. linearis, G. ampla, and
G. parallela, are represented by the allied Damuda species, G.
angustifolia, G. communis, and G. damudica. The genus Phyllotheca
is represented in both floras, and the Australian form is allied to,
and was long considered identical with, the P. indica of the Damudas.
Vertebraria is found in both series, and is only known elsewhere
from the “Jurassic” beds of Siberia. Sphenopteris alata, Brong., is
another species represented by allied forms in the Damuda flora, and
Gangamopteris angustifolia, M‘Coy, is common to the two floras.
Besides these the genus Noeggerathiopsis is represented in both floras,
so that we have in all six genera and two species common to the
two floras, besides five species represented by allied forms. In other
words two-thirds of the genera and more than a quarter of the species
of the Newcastle flora are represented in that ot the Damudas.

Taking all these points into consideration, I think we may safely
affirm that the Talchirs of India, the Ecca beds of South Africa, the
Bacchus Marsh beds in Victoria, and the Marine beds below the New-
castle Coal-measures in New South Wales, were all deposited con-
temporaneously, and that during their deposition there prevailed
a Glacial epoch comparable to, if not even more severe than, that of
the Pleistocene period.

This conclusion brings out the contradictory nature of the Paleon-
tological evidence even more strongly than it was possible for Dr.
Blanford to do in his address, for it shows that the coexistence of
a Jurassic flora with a Carboniferous fauna was no mere local phe-
nomenon, but that the Jurassic flora had established itself over nearly
half a hemisphere, while the Carboniferous Mollusca were still
inhabiting the seas.

In the face of this contradiction, it may be allowable to doubt
whether either form of paleontological evidence can be regarded as
absolutely trustworthy, and to question whether the beds containing
the Lower Carboniferous marine fauna may not have been deposited
synchronously with the deposition of the Permian Boulder-beds of
England, and with certain Boulder-beds which are known to exist

300 LR. D. Oldham—Probable Changes of Latitude.

in North America at about the same horizon. It is, however, at
present impracticable for me to follow up this question for want of
access to books of reference; but this is of comparatively minor
importance, as my purpose has merely been to show that there have
been glacial epochs comparable to that of the Post-Tertiary period ;
and having shown that such a glacial epoch did at one time affect
a large portion of the Earth’s surface, it becomes easy to acknowledge
that similar periods of cold have occurred before and since, and that
we must not attempt to ascribe every occurrence of Glacial beds of
Tertiary or Pre-Tertiary age to some merely local cause. And
having acknowledged this, we at once obtain what was wanted, a
check on the paleontological timepiece, a time-signal on the chrono-
graph of the world.

Notr.—A month ago I would have appealed, as proof positive of
the contentions stated above, to the discovery in the Salt Range of
the Punjab of marine fossils identical with those of the Australian
Carboniferous beds. These are derived from beds which exhibit
ample proofs of glacial action, and were on that ground assumed
by Dr. Waagen to be of the same age as the Talchirs, which he
agreed with most of the members of the Geological Survey in
regarding as of Paleozoic age. The pebbles in which the fossils
were found might in hand-specimens be taken for concretionary
nodules, and an imperfect description of their mode of occurrence
would support this idea; moreover the coincidence of the fauna and
physical conditions with those of the Australian beds is very striking.
There was every temptation for me to accept Dr. Waagen’s con-
clusions, but a careful examination of the beds, and of the mode
of occurrence of the fossils, has convinced me that this is a mere
coincidence, and that the fossils, which occur as transported pebbles,
can consequently be of no use in determining the homotaxis of the
beds from which they are derived. The stratigraphical relations
of these beds are such as to associate them with the Nummulitics;
and as boulder beds, presumably of glacial origin, have been re-
corded by Mr. Lydekker as conformably underlying the Nummulitics
of Ladak, there is no difficulty in finding a horizon to which the
beds can be referred.

IJJ.—Essays on SPECULATIVE GEOLOGY.
2.—PRoBABLE CHANGES oF LATITUDE.
By R. D. OtpHam, A.R.S.M. ete.
Parr I.—Guacrtat Periops 1x Low LatirupsEs.

N my last essay I had occasion to refer to the former existence of
icebergs in localities which now lie in latitudes lower than those

in which glacial action is known to have reached, even during the
last Glacial period. But, surprising as it may be to find evidence of
glacial action within a few degrees of, and, as in the case of the
Bowen River Coal-field, a few degrees within, the tropics, this sinks
into insignificance in the face of the evidences of repeated Glacial
periods that may be found in India, and especially in the Himalayas.

R. D. Oldham—Probable Changes of Latitude. 301

In Kashmir Mr. Lydekker has described! a group of beds com-
posed of a fine-grained matrix, through which are scattered boulders
of crystalline rock; these were considered to be of glacial origin,
and indeed it is difficult to conceive of any other satisfactory explana-
tion. This group, the Punjal Conglomerates, has not yet been iden-
tified with certainty in the Simla region of the Lower Himalayas ;
but there is a group of beds whose position and appearance render
it probable that they are of the same age.

Above this group, which may represent the Punjal Conglomerates
of Kashmir, but separated from them by a considerable though
undetermined thickness of beds and an unconformity, comes the
Blaini group,? which is so unique in its character, and so constant
over a large area, that it is most important in unravelling the structure
of the hills. It consists of a band, seldom over 30 feet thick, of thin-
bedded limestone resting on a “conglomerate,” the matrix being
usually a fine-grained slate, through which pebbles and boulders of
slate and quartzite are scattered. The aspect of the rock is decidedly
glacial, and my colleague Mr. C. 8. Middlemiss has discovered a
pebble scratched in a manner very suggestive of ice action.

Yet higher in the series there is the Mandhali group, which, though
it has so far yielded no scratched pebble, is even more conspicuously
glacial than the Blaini Conglomerate ; and, yet newer, there are at the
base of a quartzite series, provisionally known as the Bawars, some
beds originally composed of fine sand, through which rounded frag-
ments of quartzite sometimes over a foot in diameter are scattered ;
these beds are associated with a very coarse-grained arkose, itself
indicative of a more severe climate than now prevails in these Jati-
tudes, even at an altitude of 15,000 feet. These last two groups have
not yet been proved to be distinct ; but there is no reason for doubting
their distinctness, or suspecting their identity.

All these beds are conspicuously of subaqueous origin, and if we
except the Bawar beds—which have so far been identified in one
locality only—too widespread in their distribution and too constant
in their characters to render it probable that they are of other than
marine origin. There are, besides, very good reasons, which it is
needless to enter on here, for supposing that all the sedimentary
beds of the Lower Himalayas are of marine origin.

In the Lower Himalayas no pre-Tertiary glacial beds of later date
than the Bawars have yet been determined; but in Ladak Mr.
Jiydekker has described a group of beds which he considers of glacial
origin, as conformably underlying the Nummulitics.®

Leaving the Himalayas, we find in the Salt Range proofs of glacial
action at more than one horizon. The newest of these is in the
“Olive group,” which was originally described as Cretaceous, and
lately, on the strength of some Oonularig, identical with species
found in Australia, which were supposed to be derived from con-

1 Memoirs Geological Survey of India, vol. xxii. p. 247.

2 First described by Mr. H. B. Medlicott, Memoirs Geological Survey of India,
vol. i. pt. 2, p. 30.

3 Memoirs Geological Survey of India, vol. xxii. p. 104.

302 R. D. Oldham—Probable Changes of Latitude.

cretionary nodules formed in situ, has been declared to be Carboni-
ferous and contemporaneous with the Talchir group of the peninsula.!
This last supposition may or may not be true; but, as I have already
explained, there can be no manner of doubt that the fossils occur in
transported pebbles, and are consequently valueless for determining
the homotaxis of this group.’

Besides the Olive group, Mr. Wynne has described glacial boulder
beds in the Speckled and Purple Sandstone groups of the Salt Range,’
and in the Trans-Indus extension of that range glacial boulder beds*
crop out from below a limestone of Upper Carboniferous age.

In the peninsula we know of but a single group of glacial beds,
but it is not difficult to account for the difference; for, while the
extra-peninsular area has yielded an extensive and fairly complete
series of marine sedimentary beds, these are conspicuously absent in
the peninsular area. The limestone of the Vindhyan series and the
Talchir group of the Gondwanas may be of marine origin ; but, apart
from them, the rocks of the peninsula, where not of volcanic or meta-
morphic origin, are almost entirely river deposits; so that the absence
of any trace of more than a single glacial period is more than
possibly due to their records having been destroyed.

These facts are in themselves sufficiently striking and difficult to
reconcile with some of the generally accepted hypotheses of geology,
but they are emphasized by a detailed examination of two of the
instances. ‘To take the Olive group of the Salt Range, boulders and
pebbles showing glacial striz are abundant, and it is by no means
unusual to find an irregular-shaped mass of hard crystalline rock
with one, and occasionally more than one, of its surfaces ground into
a flat facet, smoothed, polished, and striated with nearly parallel
strize.

In the case of the Talchir boulder bed of the peninsula, it has been
usual to ascribe its origin to winter coast ice; but the flattened
boulders of the Olive group indicate a more prolonged wearing, a
greater pressure and a greater constancy of direction of motion than
can be accounted for on this supposition. We are consequently
driven to the hypothesis that they have been ground by a glacier
which descended to the sea-level and gave off icebergs there.

Now the majority of these boulders consists of rocks of recog-
nizably peninsular types, not a few are of a very highly siliceous
felsite porphyry, which is at present only known in the Rajputana
Desert, and not a single fragment has yet been found which can be
declared to be derived from a Himalayan source. Besides this, the
pebble band from which the Conularia referred to above were obtained
exhibits certain peculiarities of distribution, which indicate that
the source from which the pebbles were derived lay to the south-
wards.°

1 Records Geological Survey of India, vol. xix. p. 22.

2 Ibid. p. 127, e¢ sequel.

% Memoirs Geological Survey of India, vol. xiv. pp. 87, 98, 214, ete.
* Thid. vol. xvii. p. 239.

5 Records Geological Survey of India, vol, xix. p. 129,

R. D. Oldham—Probable Changes of Latitude. 303

The boulder bed of the Olive group has not yet yielded any fossils
of contemporaneous origin, but it appears to be perfectly conform-
able to beds of undeniably marine origin, and every argument from
analogy is in favour of the supposition that it is itself either of
marine or estuarine origin. But, as I have shown above, the land
surface of whose waste it is composed lay to the south, so we arrive
at the rather startling conclusion that when the beds of the Olive
group of the Salt Range were being deposited, there were glaciers
which descended to the sea-level in a region which now lies within
04 degrees of the Equator.

In that great and almost unknown tract lying between the
Aravalli Mountains and the Indus, which is comprehensively
entitled “Desert”? on the maps, there may be found near the town
of Pokran, in N. latitude 26° 55’, an old land-surface showing
glacial groovings and striz. These might be ascribed to the action
of winter coast ice formed on the margin of a lake or sea; but, in the
boulder beds which occur in the neighbourhood, and are without
doubt of the same age as the glaciated land surface, there may be
found facetted blocks which, like those of the Salt Range, could not
be ascribed to anything but glacier action. Moreover, this land-
surface is covered in places by a boulder bed with a hard intensely
tough matrix, differing from the stratified boulder beds of the neigh-
bourhood in much the same manner as the “till” of Scotland differs
from the marine boulder-clays of the Midland Counties; if the
hypothesis that the toughness of the former is due to its being a
“Grundmoraine ” be accepted, it follows that the same explanation
will account for the toughness of the boulder beds of Pokran, and
we have yet another proof of the existence of glaciers on this old
land-surface.

The boulder beds in the Desert have been traced for sixty miles
north-east of Pokran; in the vicinity of the old land-surface the
boulders are almost exclusively of porphyry and syenite derived from
it, but further north blocks of gneiss of the peninsular type become
common; and in N. latitude 27° 30’, Hast longitude 72° 30’, there is
a block of very coarse-grained granite, of which 10 feet x 74 feet
x 3 feet is exposed above ground. The nearest source from which
this block could have been derived is in the Aravallis full 150
miles away. The age of these boulder beds appears to be the same
as that of the Talchirs; the reasons for this conclusion are of a
purely inferential nature, but their extent, combined with the dis-
tance from which some of the blocks have been transported, as well
as their position on the western margin of the peninsular area, point
to the conclusion that they are of marine origin ; so that here again we
have evidence of glaciers having descended to the sea in a district now
less than 27 degrees from the Equator.

Part IJ.—Gernerat ConsIDERATIONS.

It has long been known that there were ample proofs of the former
existence of mild, even subtropical climates within the Arctic circle ;
but the continuity of this climate, and the absence of any signs of

304 R. D. Oldham—Probable Changes of Latitude.

the extreme cold which now prevails in that region, was never fully
understood till it was described and emphasized by Baron Norden-
skiéld. Ina lecture of his published in this Magazin», after review-
ing the evidence of the fossil flora and fauna, he remarks on the
favourable nature of the country for geological investigation, on the
completeness of the series extending one may say from the Silurian
to the Tertiary, and emphasizes the fact that, in all the sections he
had examined, he never saw a boulder “even as large as a child’s
head” in any rock of Tertiary age or older.’ Various hypotheses
have been propounded to account for these warm climates in the
Arctic regions without involving a shifting of the earth’s polar axis ;
the most ingenious and captivating of these is doubtless Mr. Wallace’s
modification of Dr. Croll’s theory, according to which the mild
climates of the polar area were due to the warming effects of currents
of heated water, from the equatorial regions, which have been cut off
by a gradual development of the continental areas. Looked at from
the polar point of view, this hypothesis was legitimate and competent
enough to account for the facts it was intended to explain; but an
hypothesis is only acceptable as long as nothing directly incompatible
with it is known, and however competent the hypothesis may be to
account for the mild climates of what are now the Arctic regions, it
is absolutely incompatible with the evidences of repeated glaciation
in low latitudes which I have referred to above.

Mathematicians forbid us to explain the circumstances by a shift-
ing of the axis of revolution of the earth. Whether in this they are
right or wrong is immaterial, for it seems to me that there is an
equally satisfactory hypothesis open to us. Mr. Fisher, in his
«« Physics of the Harth’s Crust,” has given good reasons for supposing
that there is a fluid or semifluid layer intervening between the solid
core and the solid crust of the earth,—in other words, that the latter
has a power of shifting its position on the former ; if this theory be
accepted, it is quite conceivable that the portion of the earth’s crust
which now occupies the polar circle may once have lain under the
Equator and vice versa ; indeed I find in Mr. Fisher’s* book an asser-
tion of the probability of this shifting of the polar and equatorial
areas based on reasons quite different from and independent of those
I have given for the same conclusion.

The known facts of stratigraphical geology, more especially the
existence of regions which can be proved to have undergone com-
pression to the extent of two or more times their present dimensions,
in immediate proximity to others in which the beds have suffered
little or no compression, show that to some extent this shifting of
the crust of the earth over its core must take place, and almost the
only argument that can be produced against an extension of the same

1 Grou. Maa. 1875, p. 531, and 1876, p. 266. I cannot help contrasting this
with my own experience in the Himalayas, where the series is well exposed in
numerous deep valleys, where there is an extensive series of beds extending from even
before the Silurian to the Tertiaries, and where evidences of pre-Tertiary glacial
action met me, I might almost say at every turn.

2 Physics of the Earth’s Crust, p. 184. But earlier still see ‘‘ On a Possible Cause

of Climatal Changes,” by Dr. John Evans, F.R.S., F.G.8., Guou. Mae. 1866, p.
171.—Eprr.

R. D. Oldham—Probable Changes of Latitude. 305

reasoning would be derived from the doctrine of permanence of con-
tinents. It is, however, by no means inconceivable that the two
hypotheses might be quite consistent ; were the differences between
the continental and oceanic areas entirely due to differences in the
structure of the crust, the latter might sbift its position relative to
the core to any extent without interfering with the relative positions
and forms of the continental and oceanic areas.

But is this doctrine so well established that it can be used as an
argument against any hypothesis which is fairly supported by known
facts? I think not. It is unnecessary to refer to the fact that the
“Oceanic” island of South Georgia has been found to consist of
clay-slate,? and not of volcanic rocks, as ex hypothesi it should, for
there are certain peculiarities, in the paleontology of India and
South Africa, which indicate the former existence of direct land com-
munication between the two countries. This was first pointed out
by Mr. H. F. Blanford, whose paper is somewhat contemptuously
dismissed by Mr. Wallace with the remark that “the notion that a
similarity of the productions of widely separated continents at any
past epoch is only to be explained by the existence of a direct land
connexion, is entirely opposed to all that we know of the wide and
varying distribution of all types at different periods, and is no less
opposed to what is now known of the general permanency of the
great continental and oceanic areas.” * This, however, implies a mis-
conception of the nature of the evidence, which is far from being
based merely on a “similarity of the productions” of the two
countries. There are in Africa two distinct floras of different ages ;
one of these, that of the Beaufort beds, has a flora consisting of five
distinct species, of which one is identical, two are closely allied to,
forms found in the Damuda beds of India, and if we accept Dr.
Feistmantel’s* opinion, all belong to Damuda genera; associated
with these plants is an extensive and peculiar reptilian fauna, of
which the most prominent genus is Dicynodon, a genus at present
unknown elsewhere except from the Panchet beds which overlie the
Damudas, and another form, Micropholis Stowei, is a near ally of
Brachiops laticeps from the Kamthi beds of Mangli.*

At a higher horizon in South Africa, in the Uitenhage formation,
there is a flora consisting of 12 distinct forms, all generically different
from any of the Beaufort species. Of these, one is identical with,
four are closely allied to, species from the flora of the Rajmahal group
in India. The difference between the flora of the Rajmahal group
and of the Danudas is almost as great as in the case of the two cor-
responding African groups, for there are only three species in the
Rajmahal flora which are in any way allied to any of the Damuda
plants. We have then a close and continuous similarity between the
fauna and flora of two countries lasting through a period long enough
to allow of a complete specific, and almost complete generic change.

A similar but even more conclusive argument may be derived

1 Nature, March 27, 1884, p. 509; Gon. Mac. Dec. III. Vol. I. p. 225 (1884).

2 Island Life, p. 398. ’ Paleontographica, 1878, p. 114.
4 Manual of the Geology of India, vol. i. p. 123.

DECADE III.—VOL. III.—NO. VII. 20

306 Rk. D. Oldham—Probable Changes of Latitude.

from the relations of the Marine Cretaceous rocks in India and other
parts of the world. Both in Southern India and Southern Africa
there are marine deposits of Cretaceous age, with regard to
which Dr. W. T. Blanford writes in the Manual of the Geology of
India as follows :—“ Before quitting the subject of the Trichinopoly
Cretaceous beds, it is necessary to notice the very remarkable re-
semblance between a portion of their fauna and the species found in
certain strata in Southern Africa, In the description of the Gond-
wana system, and again in the account of the Upper Jurassic beds
of Cutch, the remarkable affinities between Indian fossil plants and
animals, and the forms found in South African beds, were repeatedly
noticed, and there is a similar connexion between the Cretaceous
formation in the two regions. In some deposits found resting upon
Karoo beds on the coast of Natal, out of 35 species of Mollusca and
Echinodermata collected and specifically identified, 22 are identical
with forms found in the Cretaceous beds of Southern India, the
majority bemeerichimopoly species. Wiley Cele et saint) siereeetees
The South African beds are clearly coast or shallow-water deposits,
like those of India, and the great similarity of forms certainly sug-
gests continuity of coast-line between the two regions, and thus
supports the view that the land connection between South Africa
and India, already shown to have probably existed in both the Lower
and Upper Gondwana periods, and of which important indications
are afforded by the Marine Jurassic beds, was continued into Cre-
taceous times. It is very surprising to compare the Middle Cre-
taceous fauna of Southern India with that of the distant beds of
Natal, and then with the widely differing forms found in beds of
the same age in Central India and Southern Arabia.” *

Speaking of the latter he says, ‘Some of the species have a wide
range in time among the Cretaceous rocks of Europe, but all occur
in the Upper Greensand (Cenomanian), many being characteristic
forms, and the Cretaceous rocks of the Narbadda valley must in
consequence closely correspond to the Utatur group of Southern
India. It is curious to note that, so farasis known, only one species,
Pecten (Vola) quinquecostatus, is common to both, and even in this
case the identification depends upon a question as to which palzon-
tologists are not thoroughly agreed . . .

In strange contrast with the wide difference between the known
fauna of the Bagh beds and that of the Southern India deposits
is the similarity between the fossil remains of the Narbadda
valley and those found in two localities on the south-east coast
of Arabia. The collections examined from both localities are small,
and were obtained in each case during a short visit; but although
the united Arabian collections only comprise 13 species and the
Bagh 12, three of these .... are common to the two countries.
The Cretaceous beds of the lower Narbadda valley are about
750 miles distant from those of Southern India, and twice as far
from the Arabian localities. 'The marked contrast between the
fossil faunas in the one case, and the similarity in the other,

1 Loe, cit. p 292.

R. D. Oldham—Probable Changes of Latitude. 307

tend to suggest the probability that a land barrier interposed
in Middle Cretaceous times between Southern India with Assam and
Arakan on the one side and the Western Narbada region with the
south coast of Arabia on the other. We have thus another argument
presented to us in favour of the Indian peninsula being portion
of an ancient land-area; and taking into consideration the marked
connexion between the faunas of the South Indian and South African
Cretaceous deposits, and the circumstance that both appear to be of
littoral origin, it is probable that this land-area extended to Africa.” ?

These facts indicate that the permanence of continents is a hobby
which some of its admirers have ridden too hard, and at any rate
prove that it cannot be used to stifle a plausible hypothesis.

Another group of facts which are in favour of the suggestion I
have made above is the observational evidence in favour of a change
of latitude in some of the principal European observatories. In
the American Journal of Science for March, 1885, Professor Asaph
Hall gives, on the authority of S. Fergola, the following table of
latitudes of the principal observatories of Europe and America :—

Washington 1845 cce-ee 38° 53’ 39"-25
do. 1863 Bondoc 38”-78
Paris IEE Asboon 48° 50’ 13”: 0
do. Ife} “aconan 11”: 2
Milan ISI’ Gooeoe 45° 27’ 60": 7
do. STL eonten Bers)
Rome HSI pecooe 41° 53 547-26
do. 1866 600000 54”-09
Naples 1820 002000 40° 51’ 467-63
do. NEE ogo <6 45/41
Kénigsberg 1820 codc09 54° 42’ 50°71
do. 1843) s.soe 50"°56
Greenwich 1838 =p9000 51° 28’ 38”°43
do. 1845 sass 38°17
do. 135 ORmneecinn's iro ae

Besides this there are the Pulkowa observations which give the
following results :—

Pulkowa 1848 ..... 59° 46’ 18-73 + 0-013
do. TeGge Were 18”-65 + 0”-014
do. nD) ey 18”-50 + 0-014

I am aware that the most recent investigations of the Greenwich
observations by the present Astronomer-Royal have shown that there
is no proof of continuous change of latitude; but it is surely some-
thing more than a coincidence that the change in every case is in
the same direction ; had the change been due merely to imperfect
observation or the vagaries of refraction, it would hardly have ex-
hibited these strange coincidences. There is, however, more than
one way of explaining these slight variations of latitude, and, seeing
that the observations extend over a comparatively short period of
time, it would not do to attach too great importance to them in this
connexion.

A more important argument is to be derived from the careful
measurements of the pyramids of Gizeh which have been made by

1 Loe. cit. p. 297.

308 Rev. W. Downes—A Section near Honiton, Devon.

Mr. Flinders Petrie. The orientations of the sides and passages of
the great and second pyramids vary not more than 30” from each
other, but they both agree in varying rather than 5’ west of north ;*
it is inconceivable that this close approximation of the orientation of
the sides and passages of these pyramids should be due to accident,
nor is it conceivable that the builders would deliberately have
introduced a variation of some 5’ west of north. A far more pro-
bable explanation is that owing to a shifting of the earth’s crust on
its core, or of the axis of revolution, there has been a variation of
that amount in the direction true north since the pyramids were built.

Such, briefly stated, are the conditions of the problem. We have
first a group of facts inexplicable, unless we grant the possibility of
a shifting of the earth’s crust on its core, or of the axis of revolution
of the earth; secondly a group of facts inconsistent with the only
hypothesis that could be urged against the first supposition, and
thirdly a group of facts directly confirmatory of the latter.

In conclusion I must apologize for any injustice I may have—un-
intentionally —committed ; an official geologist in India has to
contend with many difficulties, not the least of which is the impossi-
bility of keeping abreast of current literature, and a want of leisure
for pursuing independent investigations. It had been my intention
to work out this problem more thoroughly during the current year ;
but having been deputed to accompany an embassy to Tibet, the
Opportunity is gone, and not likely to recur for some years. I am
consequently induced to put my notes on the subject together, some-
what hastily I confess, as it has been my good fortune to meet with
a number of facts which cannot be ignored in any discussion of the
problem of geological climates, many of them having either never
been published at all, or only in a form not generally accessible to
Huropeau geologists.

IV.—On tHe Tunnet Section nEAR Honiton, Drvon.
By the Rev. W. Downss, B.A., F.G.S.

HE writer has for some time hesitated to seek in the pages of the
GrotocicaL Magazine a publication of his experiences upon
the above subject. He fell last year into a grievous mistake with
regard to it, and suffered that mistake to be published in the
‘Transactions of the Devonshire Association for the Promotion of
Science, Literature, and Art.” It will be his duty, when the oppor-
tunity comes round (as shortly it will), to call attention to that
mistake in the pages of the same periodical. In the meantime he
thinks that the subject, and even the mistake associated with it, may
be of something more than local interest. Atleast the recantation of
a published error cannot be too widely circulated.

The tunnel on the L. & S. W. Railway about a mile east of the
town of Honiton pierces a hill in a EH. and W. direction. The cut-
ting on the W. of the tunnel exposes the Red Marl of the Trias.
That on the H. of the tunnel exposes some black or grey beds, mostly

1 The Pyramids and Temples of Gizeh, by W. M. Flinders Petrie, p. 126.
(London, 1883.)

Rev. W. Downes—A Section near Honiton, Devon. 309

arenaceous, which are now to be discussed. Both the Red Marl and
the dark-coloured arenaceous beds above them have the same easterly
dip of about 5°.

About a mile to the eastward of the tunnel is a north and south
fault, and the tunnel beds are on the downthrow side of it.

Mr. H. B. Woodward and Mr. Ussher had in the work “ Geology
of England and Wales,” p. 237, by the former, expressed an opinion
that the beds EH. of the tunnel were Gault, and the present writer
approached the subject with a decided predisposition in favour of
that view. He did not perhaps attach the weight to their opinion
that he ought to have done, for he had somehow arrived at the
impression that their opinion was but a conjecture, and did not
profess to be more. Nevertheless, he would have much hesitated to
call it in question, were it not that a piece of entirely new evidence
was presented to him.

In the course of correspondence with the railway officials, he was
informed that at the Engineer’s office of the Railway Company there
was a detailed diagram of the tunnel on a large scale. He went to
see it, and was brought face to face with a dilemma. Hither the
black beds were Rheetic, or the diagram was wrong.

Could the latter be wrong? The unknown engineer who con-
structed it had had exceptional facilities for accuracy. Shafts had
been sunk at frequent intervals, and the position, thickness, character,
and colour of every bed was given with great exactness. Many
thousands of pounds had depended upon the general accuracy of the
section, and though the uppermost beds did not affect the tunnelling,
it was but reasonable to suppose that they also would be correctly
given. And in them was represented an unconformity exactly like
that which exists between the Trias and the Greensand in all the
country round about, the Trias (or Rhetic) dipping eastward, the
Greensand above it being horizontal.

A great unconformity in the midst of the Cretaceous series was
not to be thought of. If then the diagram was right, the lower beds
could be nothing else but Rhetic. And such the present writer con-
sidered them to be until, after a persevering search for fossil evidence,
he at last found it; but lo! the fossils were Cretaceous !

They were :—

Inoceramus concentricus (Park.) (abundant). Mytilus.
Tornatella (Acte@on) affinis (Sow.) Tellina.
Pecten quadricostatus (Sow.) Exogyra.
Modiola. Pectunculus,

The above occurred in a black marly clay bed about six feet thick,
which comes in the middle of the series.

The diagram, which—tested by the exposed beds at the base—
must be accurate in the main, is certainly inaccurate as regards the
uppermost beds. As before remarked, they did not affect the tunnel-
ling, and were perhaps carelessly added. Perhaps the designer was
in part inspired by the analogy of the surrounding country, with
whose geology he was presumably to some extent acquainted. But
as his very name is unknown, and he cannot answer for himself, it
is useless to discuss his responsibility for the error.

310 Rev. W. Downes—A Section near Honiton, Devon.

But independently of the diagram, there was a certain balance of
other improbabilities which had to be weighed. It was improbable,
as urged by Mr. Ussher, that the Rheetic beds should attain so great
a thickness,—about 160 feet. It was improbable, as urged by Mr.
H. B. Woodward, that they should locally assume an arenaceous
character (though, as already mentioned, the beds in question are not
arenaceous throughout). But on the other hand, it was improbable
that the marked unconformity, usual between the Trias and the
Greensand, should be absent in this one spot, that the Trias should
have in this particular spot no proper dip whatever, but should
acquire just about its normal dip abnormally through the downthrow
of a fault, and should exactly share that dip with Cretaceous beds
above it.

Again, it was antecedently most improbable that Gault-like rock
should reappear in this locality. At Lyme Regis, 25 miles to the
S.E., black marl with Lima parallela occurs, but this appears to be
approaching extinction westward, and is there only about 20 ft. thick.
At Uplyme, Trinity Hill, Shute Hill, and Dalwood Down, eminences
in a straight line from Lyme Regis to Honiton Tunnel, along the
line of dip no Gault is found. And we seek for it equally in vain
along the line of strike. Yet at Honiton tunnel something of the
nature of Gault is found.

It would seem that to connect these Honiton beds with the Lyme
Regis bed, a curved line must be drawn southwards and passing out
to sea. Traces of dark grey beds,—all however arenaceous—are
seen in the cliff-section at Whitecliff and at Seaton. Further out to
sea there might once have been an areno-argillaceous bed connecting
the 20 ft. bed of Lyme Regis with the 6 ft. bed of like character at
Honiton. It is a conjecture with at least some probability about it.

But when we compare these so-called Gault beds of the West
with the typical Gault of Folkestone (Quantum mutatus ab illo!),
what have they in common? The argillaceous character has been
almost entirely supplanted by an arenaceous one. The fauna has
undergone many modifications. Zima parallela still lingers on in
the attenuated bed at Lyme Regis, but has not yet been found at
Honiton, where the semi-argillaceous bed is still more attenuated.
Hiven the colour gets washed out as we go westward. Olay merges
into sand. Black merges into yellow. In a word, between Upper
Greensand and Gault boundary there is none in the West of England.

With the exception of the unconformity represented in the upper
beds of the section, the diagram in the possession of the L. & 8. W.
Railway is no doubt mainly correct. It gives the following thick-
nesses to the several beds :—

Clay with Chert passing into Cherty Greensand, bedded ... 58 feet.
Greyr Sand ee? TART Oe Be ie EL, OATS IG &
WellowmpSandyidiare Wiehe Weed J2.) ated ieee Meee ot Mass cerned Sleep
Manipated Marly Clay, 6) a:+ Piste loos fine baeeaqen wield op
BAU Sand hes ais. ve by te cscs mts pea a ew ee oie
Wilice Sander tear eae aces aca! Asoc rete beeee ieee tee comme anes
Greenishisandy!Clays® BE. Sa RI Te Oe, ATO
215 ft.

Red Marl.

A. J. Jukes-Browne—On the term Neocomian. 3811

There are thus shown to be 215 feet of beds of various kinds
above the Red Marl, but it is difficult in the absence of unconformity
to say where the Trias ends. Probably the 10 ft. of “greenish
sandy clay” belongs to the Trias. Similar beds occur in the same
position in the same locality. The geological age of the “ white
sand” and the “black sand” is “‘not proven,” but probably they are
Cretaceous, though there is no visible unconformity to show it.
The “variegated marly clay” is certainly Cretaceous, as proved by
the fossils quoted above.

DLL DIET TRE

Sa

SSs7

¢ She Sieie Ca - G ( chaans eS SSS
1. Red Marl. 5. Yellow Sand.
2. Greenish Sandy Clay. 6. Grey Sand.
8. Black Sand. 7. Cherty Greensand.
4, Dark grey marl and black clay. 8. Clay, with chert.

* The place where the fossils were found.

V.—On tHe APPLICATION OF THE TERM NEOCOMIAN.
By A. J. Jukes-Browne, B.A., F.G.S.

UCH confusion and difference of opinion appears to exist with
regard to the classification and nomenclature of the strata
which form the lower part of the Cretaceous system, and the chief
element of this uncertainty and confusion is the misconception which
prevails respecting the proper signification and application of the
term Neocomian. The object of the present paper is to explain the
continental usage of this name, and by showing its inapplicability
to any. of our English strata, to prepare the way for a more satis-
factory grouping of our Cretaceous rocks.

For many years English geologists were content with the nomen-
clature employed by the earlier students of the Cretaceous system—
Webster, Murchison, Mantell and Fitton. In 1864, however, the
French term Neocomian was introduced by Prof. Judd,' who adopted
it for the Cretaceous portion of the Speeton Clay, and Sir Charles
Lyell subsequently used it as a synonym for the whole Lower Cre-
taceous series in England as distinct from the Upper Cretaceous
series or the beds lying above the Lower Greensand. Consequently
in many text-books we find the following arrangement of the Cre-
taceous groups :—

1 Quart. Journ. Geol, Soc. vol. xxiv. p. 218.

312 A. J. Jukes-Browne—On the term Neocomian.

Southern Area. Northern Area.
Chalk White Chalk.
Upper Cretaceous. Upper Greensand
oho \ Red Chalk.
er OM aA glen era ei ccdin ean.
Lower Cretaceous Wealden Lower Neocomian.

Now in order to ascertain whether this use of the name Neocomian
was in any way desirable or justifiable, it is necessary to make some
inquiry into the history of the name and its usual acceptation by the
majority of geologists on the continent.

The primary groups or divisions of the Lower Cretaceous series
usually recognized in France and Switzerland are those proposed by
D’Orbigny, namely :—(1) Neocomien; (2) Urgonien; and (38) Aptien,
and the history of these names is as follows. Previous to 1835 the
rocks included in the first two groups were known as the “ Jura-
Cretacée” group, and in that year Thurman proposed to call them
Neocomien, from their development in the neighbourhood of
Neuchatel; this name was adopted by Marcou and others, but it is
important to remember that this Neocomien series did not include
the beds now known as Aptien ; thus we find Prof. Marcou in his
“Lettres sur les roches du Jura” writing in 1856 of Lower, Middle,
and Upper Neocomien, but the summit of his’ Upper stage is the
white limestone of Neuchatel (Urgonien).

Meantime D’Orbigny had been making his paleontological investi-
gations, and had in 1848 described a series of beds lying between the
Gault and what was then called “‘Neocomian” in the south-east of
France ; these beds he proposed to call Aptien from Apt in Vaucluse.
The relation of the Neocomian as understood by Thurman and
Marcou to the Aptien and Lower Greensand is clearly stated by
Marcou in his first letter on the rocks of the Jura (p. 14) thus, “It
is clear in fact that the Lower Greensand of England is in no way
the equivalent of the Neocomian, and is hardly perhaps to be corre-
lated with the upper part of the Neocomian ... The blue marls
which I have called the Marnes d’Hauterive, and which contain so
many fossils, the Calcaire jaune inferieur, etc., that is to say, the
Lower and Middle Neocomian, have no marine representatives in
England.”

He appends a table showing that these Neocomian strata are the
marine representatives of the English Wealden, with possibly the
lowest beds of the Lower Greensand, and he recommends the adop-
tion of the name as indicating the normal marine type to which the
freshwater Wealden is an exception.

Marcou, however, does not look with favour upon D’Orbigny’s
name of Urgonien, which was proposed in 1850, D’Orbigny then
suggesting a new classification for the whole series, separating the
upper half of the beds called Neocomian by Marcou under the name
of Urgonien (from Orgon, Bouches des Rhone), and thus limiting
the name Neocomian to the lower half of Marcou’s series, that is,
from the horizon of the yellow stone of Neuchatel downwards.

A. J. Jukes- Browne—On the term Neocomian. 313

Lastly, in 1854, Prof. Renevier, of Lausanne, described certain
beds, which had previously been called Lower Aptien, as a separate
subdivision under the name of Rhodanien, and in 1856 he published
a brief note “On some points in the Geology of England,” in which
he announced the results of a visit he had made to England for the
purpose of comparing the Swiss and English beds. The results are
that the Lower Greensand is not the equivalent of the Neocomian,
but corresponds exactly with the Aptien, and that the fauna of the
Atherfield beds of the Isle of Wight has the strongest analogy with
that of these Lower Aptien or Rhodanien beds. Marcon, writing in
1858, says that he willingly adopts these conclusions and opinions of
M. Renevier.!

Meanwhile, a further modification had been proposed by MM.
Coquand and Leymerie, who found a difficulty in separating the
Urgonien and Aptien groups in the Pyrenean district, where accord-
ing to their account the rocks contain a mixture of the fossils which
elsewhere occur in the Urgonien and Aptien ; they therefore proposed
to combine these two groups, calling the division thus formed the
Urgo-Aptien, and admitting a Neocomian division below. This
suggestion has been adopted by Prof. Renevier, who published the
following arrangement in 1874 (Tableau des Terrains Sedimentaires) :

Aptien
Urgo-Aptien Rhodanien
Urgonien.

Hauterivien

Neocomien 2s
Valanginien.

The facts upon which this scheme is founded require confirmation,
and the nomenclature proposed does not seem to have found much
favour, D’Orbigny’s names being still generally employed by French
geologists.

Having now explained the origin of this nomenclature, I proceed
to give the succession of the strata in question at some of the typical
localities.

The most complete sections are to be found in the S.E. of France
(Departments of Vaucluse, Drome and Isere), where the succession
is as follows, according to MM. Cornuel and Lory.

Greenish sandstones.
Marls with Belemnites semicanalicutus, Ammonites nisus, Martini and

Jissicostatus.
Marls with Orbitolites and other fossils.

Aptien.

Limestone with Caprotina (Requienia) Lonsdalet.
Urgonien. { Marls with Orditolites and Heteraster oblongus.
Limestone with Caprotina (Requienia) ammonia.

Marls with Touzaster complanatus.

Marly limestones with Ancyloceras Duvalit.

Glauconitic limestones with Bel. dilatatus.

Red limestone with Ostrea Couloni and Pygurus rostratus.
Limestone of Fontanil.

Marls with Bel. latus and Am. neocomiensis.

Argillaceous limestones with Am. astierianus.

Limestones with Zerebratula diphyoides.

Neocomien.

1 Sur le Neocomien dans le Jura, Zurich, 1858, p. 63.

314 A. J. Jukes-Browne—On the term Neocomian. ©

The basement beds are only found at and south of Chambery,
while north of that place the Calcaire de Fontanil is the lowest bed,
resting on Coral Rag. M. Lory remarks that all the limestones
thicken northward toward Savoy and the Jura, while the marls in-
crease to the southward, and Prof. Hébert ' states that the argillaceous
hydraulic limestones with Ammonites Astierianus attain a thickness
of 500 metres (1600 feet) near Chambery, the aggregate of the rest
of the Neocomian above these limestones having an equal thickness,
so that the total depth of this division here is at least 3300 feet.
There is some doubt whether the lithographic limestones with Ter.
diphya (ganitor), which underlie those with T. diphyoides, should
not also be classed as Neocomian.. Renevier refers them to the
Portlandian, but Hébert places them in the Neocomian (thickness
3d0 feet). Near Grenoble the Urgonien is said to be 900 métres
(nearly 3000 feet) thick, but nowhere else does it reach more than
1300 feet. The Aptien is about 60 feet thick at Grenoble, but at
Bedoule it is as much as 650 feet, and in the Gard about 300 feet.*
At Perte du Rhone, farther north, the section is given as follows by
Prof. Renevier :—

Greensand with Ammonites mammillaris.

Hard greenish sandstone, with Plicatula placunea and Am.

Cornuelianus.

Sands without fossils.
Greenish sandstone with Ostrea aquila. —
{ Marly sandstones including a thin layer fal of Orbitolites lenti-
culata (88 feet).
Clays without fossils (10 feet).
Rhodanien, 56 feet.< Marls with Heteraster oblongus, Trigonie and Aporrhais Robi-
naldina, etc.
Red Limestone with Heteraster oblongus, Pterocera pelagt, and
| Caprotina Lonsdalet.
White friable limestones and grey compact limestones in
Urgonien, 340 feet. alternating beds, and containing Caprotina (Requienia)
ammonia: base not seen.

Aptien, 20 feet.

By Pictet and Campiche the beds are differently grouped; they
place the red limestone in the Urgonien, and class the overlying
marls and clays as Lower Aptien, the Upper Aptien here being very
thin. Sandy limestones with fossils of true Neocomian species occur
at a lower horizon, the above section only extending as far as the
confluence of the Rhone and Valserine.

In the Jura and near Neuchatel the succession is given as follows,
the thicknesses of the lower beds being those given by Marcou :—

Aptien and ( Greensands of Presta with Plicatula placunea.
Rhodanien. Yellow marl with Heteraster oblongus and Orbitolites.
Urgonien, White limestone with Requienia ammonia.

150 feet. { Yellow limestone with Goniopygus peltatus.

Yellow stone of Neuchatel.
Neocomien, ) Marls of Hauterive with Am. radiatus.
250 feet. Limonite de Metabief with Pygurus rostratus.
uagsiom of Auberson with Touxaster Campichei.

1 Bull. Soe. Geol. de France, ser. 2, vol. 28, p. 142.
2 For this and other information I am indebted to Dr. Ch. Barrois.

A. J. Jukes-Browne—On the term Neocoman. 315

The two lowest Neocomian groups have been termed by some
Valenginien and the two upper Hauterivien; the lowest rests on
beds of Purbeck age, containing Planorbis Loryi, and other freshwater
shells.

Dr. Barrois informs me that the total thickness of the three
divisions in the Jura is from 200 to 300 métres (650 to 990 feet).

In the north of France there is only one locality where anything
like a complete section of the series is found, and this is at Vassy in
the north-eastern department of Haute-Marne. ‘The succession here
as described by M. Cornuel is as follows :—

Greensand with Ostrea arduennensis (? base of Gault), 28 feet.

Sand and Sandstone with Ostrea aquila and O. arduennensis.
Plicatula clays—in three divisions, the middle containing Ammonites

Aptien. nisus and fissicostatus, the lower Ostrea aquila and Ter, sella,
97 feet. besides Plicatula placunea.
Red marl with Orbitolites lenticulata, Heteraster oblongus and other
fossils.
Oolitic ironstone and ferruginous sandstone, with Unio and fresh-
Urgonien, water fossils.
118 feet. Mottled clays and sands (freshwater).
Clay with Ostrea Leymeri.
Yellow marly clay.
: Spatangus limestone (Zoxaster, etc.)
Neocomien, White sand.

34 feet. Ferruginous sands and ironstone.

Dark marly clay.

Prof. Hébert prefers to group the Oyster-clay as Neocomien, and
to place the red marl at the top of the Urgonien, commencing the
Aptien with the Plicatula-clays.

In passing westward from the Haute Marne, the Neocomien and
Urgonien beds appear to thin out, and are overlapped by the Aptien,
which in Ardennes is reduced to a few feet of glauconitic clay with
marly ironstone at the base containing fossils and pebbles derived
from Paleozoic rocks like the “pebble beds” of Godalming and
Faringdon (Barrois, Terr. Cret. des Ardennes, pp. 252, 263).

It is interesting to notice that in the Vassy section the marine
Neocomian beds are succeeded by a group the greater part of which
consists of freshwater beds resembling our Wealden strata. More-
over, the fauna of the overlying red bed has been identified by
Renevier as that of his Rhodanien, and he finds the same fossils in
the Atherfield beds of the Isle of Wight; here therefore we seem
to have a basis of correlation, and it becomes important to decide
whether this Rhodanien horizon should be grouped with the Urgonien
or the Aptien, for it is nowhere of sufficient stratigraphical impor-
tance to rank as a separate primary division.

Two of the best modern authorities on the Cretaceous rocks of
France, namely, Prof. Hébert and Dr. Ch. Barrois, agree in placing
the “couche rouge de Vassy ” in the Urgonien, but the difference of
opinion which exists on this point may be held to prove that the
Rhodanien is really a passage group, and that no very decided line
can be drawn between the Aptien and Urgonien divisions of the
continental series.

316 A. J. Jukes-Browne—On the term Neoconian.

It is now time to examine the succession exhibited in our southern
counties, where, as is well known, the series consists of a thick mass
of freshwater strata (Wealden beds), overlain by marine clays and
sands which are known under the name of Lower Greensand. These
marine beds are everywhere divisible into three stages, the fossils of
which are to a certain degree different. In the Wealden area there
are :—

3. Folkestone and Sandgate beds, with Rhynchonella Gibbsii, Rh.
sulcata, Thetis Sowerby, Corbula elegans, etc. (150 feet).

2. Hythe beds, with Plicatula placunea, Exogyra sinuata, Ammo-
nites Martini, Am. furcatus, Ancyloceras gigas, A. Hillsii (200 feet).

1. Atherfield Clay, with Trigonia caudata, Tr. dedalea, Perna
Mulleti, Holocystis elegans, etc. (90 feet).

In the Isle of Wight the corresponding series is very much thicker,
but may be divided as below :—

3. Shanklin Sand, sands and clays down to the sand with ferru-
ginous concretions (256 feet).

2. Walpen Sands and Crioceras beds, with Am. Martini, Ancylo-
ceras gigas, An. Hillsii, Exogyra sinuata, and Ter. sella (400 feet).

1. Atherfield Beds, with Trigonia caudata, T. dedalea, Perna
Mulleti, Corbis corrugata, and Aporrhais Robinaldina (150 feet).

Now as the Atherfield Clay is certainly not older than the Rhoda-
nien of Renevier, there can be little doubt that the two higher groups
form an expanded equivalent of the French and Swiss Aptien. The
Urgonian facies of the Atherfield fauna was recognized long ago
by M. Cornuel, but he remarks in 1874 that “no clear separation
between the Neocomien (i.e. Urgonien) and Aptien can be traced in
the Isle of Wight, on account of the mixed assemblage that occurs
in the Crackers, which form a passage from one to the other.”’ It
is evident therefore that here, as in the south of France, there is a
complete passage between the representatives of the Urgonien and
the Aptien.

It is only necessary to add that the lower marine beds have a
limited extension, and that the uppermost beds (Shanklin sands)
overlap them and spread northward over the Jurassic rocks, all the
so-called Lower Greensand of our midland counties belonging to
this group, the range of which is probably continuous beneath the
Gault as far as Norfolk, where they pass into the upper beds of the
northern Cretaceous area.

In Lincolnshire and Yorkshire beds older than the Aptien once
more make their appearance, and in this area we appear to have a
much more complete marine series than that of the southern counties.
The Yorkshire succession has been well described by Prof. Judd
some twenty years ago, and descriptions of the Lincolnshire beds
will shortly appear in the Memoirs of the Geological Survey. The
grouping adopted by Prof. Judd, however, does not appear to be
entirely satisfactory, and his correlations with Neocomien, Urgonien,
and Aptien have not been accepted by French authorities, so that I

1 Bull. Soc. Geol. de France, 1874, p. 390.

A. J. Jukes-Browne—On the term Neocomian. 317

feel justified in subjecting them to some slight criticism. First,
therefore, as to the grouping of the zones; there does not seem any
very good reason why the zone of Ammonites speetonensis should be
classed with the lower zones rather than with the middle group.
Prof. Judd identified twenty-six species from this zone, and of these
only eight occur in the zone of Am. noricus, while thirteen species
(50 per cent.) range up into the Pecten cinctus beds : again in Lincoln-
shire the only determinable Ammonites obtained from the clays
overlying the Tealby ironstones with Pecten cinctus were the varieties
of Am. speetonensis (concinnus and venustus). I am inclined, there-
fore, to think that a part at any rate of Prof. Judd’s speetonensis zone
should be grouped with his Middle division rather than with the
Lower. The noricus zone does not appear to have any equivalent
in Lincolnshire, and it is quite possible that the masses of clay
which form the noricus and speetonensis zones in Yorkshire did not
extend into Lincolnshire, no contemporaneous deposits being formed
in the latter area.

In the next place it does not appear to me so very clear that the
fauna of the Upper division has a closer analogy with that of the
Atherfieid Clay than that of the Middle division has. There is no
very marked correspondence between any part of the northern and
southern series, the areas in which they were deposited were evi-
dently to a great extent separated from one another, many species
common in the one area do not occur in the other, and the time
range of some of those species which do occur in both series appears
to be different, thus Perna Mulleti is abundant in the Atherfield Clay
of the south, while in Yorkshire it is only quoted from the Upper
division. It occurs, however, in the middle clays of Donington in
Lincolnshire, and it is these clays both in Yorkshire that I am
inclined to regard as the homotaxial equivalents of the Atherfield
Beds, the abundance of Meyeria (though the species are different)
and of Exogyra sinuata are features in common.

If these views be accepted, the Yorkshire and Lincolnshire series
can be brought into greater harmony, and both may be correlated
with the southern type as follows :—

Yorkshire. Lincolnshire. Isle of Wight.

150 | Co tele absent’ } Shanklin Sands.

Pecten cinctus beds \ Donington Clay { Walpen Sands, etc.
250 feet Ancyloceras beds and Tealby Beds \ Atherfield Clay.
ain Speetonensis zone VWiniting: Part of the Wealden

Zone of Am. noricus pa ie ales { Beds.
100 feet «oe .

{ Zoneof Am. Astierianus Spilsby Sands

Unconformity — Hastings Sands.

This view finds support in the opinion expressed by M. Coquand,!
that the only part of the Speeton Clay series which can be correlated
with the Neocomien of the south of France is the zone of Am. astieri-
anus, and that all above it must be referred to the Urgonien and
Aptien divisions. The zone of Am. astierianus is acknowledged by

1 Bull. Soc. Geol. de France, 2nd ser. vol. 26, p. 211.

318 A. J. Jukes-Browne—On the term Neocomian.

all authorities to be homotaxial with the Hauterivien marls and
Spatangus limestones, and the oldest Neocomian rocks which under-
lie these are not therefore represented in the Yorkshire area. I see
no reason however why the zone of Am. noricus should be excluded
from the Neocomian, since that Ammonite is probably only a variety
of Am. neocomiensis.

Coming now to the question of general nomenclature, I cannot
but think that Prof. Judd’s proposal to apply the name Neocomian
to the whole Lower Cretaceous series was a very unfortunate one.
It would appear that at the time of writing his paper on the Speeton
Clay, Prof. Judd was under the impression that this series had a
claim to be regarded as a distinct system, both on stratigraphical
and paleontological grounds ; now if subsequent investigation had
confirmed this belief, and had led to the establishment of a Neocomian
system distinct from the Cretaceous system, but of equal palzeonto-
logical importance with the other systems which are recognized
in geology, no objection could now be taken. But this is not the
case: the thickness of the Neocomien, Urgonien, and Aptien rocks
in the south of France appears to be very great (from 1000 to 6000
feet), but the mere thickness of a group of strata does not justify
the creation of a new system unless they contain a sufficiently
distinct assemblage of fossils, and in this case the fauna is neither so
large and varied or so peculiar as to entitle them to be separated from
the Cretaceous system: they are regarded by all who have studied
them as forming the lower portion of this system, just as the Gault
and Chalk form the upper portion of it, and their separation would
be no more justifiable than that of the Lias from the Jurassic system.

This being so, the proposal to call the lower series Neocomian
ceases to be logically defensible, unless a new name is found either
for the Upper Cretaceous series or for the whole system which
includes both. Prof. Judd’s nomenclature, with the belief he then
entertained, was a logical one, but I must maintain that the manner
in which it has been subsequently employed is entirely illogical.
There is an inclination in certain quarters to adopt the name
Neocomian for the lower division, and to limit the application
of Cretaceous to the upper division; this plan would certainly
secure logical uniformity, but those who suggest it are bound to
propose a new name for the system which includes these two
divisions, otherwise it would only “make confusion worse con-
founded.” There is really no necessity for any such innovation,
or for any alteration of the general scheme of nomenclature to
which we are accustomed. The Cambrian and the Carboniferous
systems are simply divided into lower and upper series, why
therefore should we not be content to treat the Cretaceous system
in the same way, and to speak simply of Lower and Upper Cre-
taceous series ?

Further, it must be remembered that the majority of French and
Swiss geologists use the term Neocomian in its special application as
limited by D’Orbigny, and its employment in any other sense, except

1 See Quart. Journ. Geol. Soc. vol. xxiv. p. 228,

Prof. C. Lapworth— Cambrian Rocks at Nuneaton. 319

on the strongest grounds of expediency. is therefore to be deprecated.
Tam fully aware that Prof. Hebert is one of those who has adopted
Prof. Judd’s nomenclature, but Prof. Hébert appears to shrink from
proposing a new name for the Lower (Neocomian) beds, though he
employs D’Orbigny’s names for the other groups; consequently he
has only succeeded in introducing an element of confusion which did
not previously exist in the French nomenclature.

The height of incongruity is reached when, by retaining the name
of Wealden for the fresh-water beds and adopting that of Neocomian
for all our marine beds, we have a Neocomian overlying the Wealden !
and consequently applied to the very beds Marcou and Renevier have
so clearly and carefully distinguished from those strata which were
originally called Neocomian in Switzerland and the south of France
(see ante). I trust that I have now made it clear that to continue
the use of Neocomian, either as a synonym for Lower Cretaceous
or as a substitute for Lower Greensand, would be productive of
immense confusion, and would entirely stultify the work of two
of the principal authorities upon the beds in question. Neither does
it seem desirable to introduce the term Aptien into British nomen-
clature, partly because of the difference of opinion which exists in
France as to the relative extension of Aptien and Urgonien, and
partly because there is not sufficient continuity between the French
and English areas to make any correlation so safe and certain as it
is in the case of the Upper Cretaceous groups. The Cretaceous rocks
of England are now undergoing revision by the members of the
Geological Survey, and the desirability of formulating a new nomen-
clature will be considered when the work is farther advanced: the
merits of the name (Vectian) which I have already proposed as a
substitute for Lower Greensand will then be discussed ; at present I
am content to let it remain in abeyance. For my present purpose
the local names used for the groups in the Wealden area will serve
as a means of comparing the beds of southern England with those
of northern and southern France so far as is possible under the cir-
cumstances ; this is done in the following table :—

South England. NV.E. France. S.E. France.
Folkestone and Sandgate Beds. ; Sands and Sandstones. Aptien
Hythe Beds. Plicatula Clays.
Atherfield Clay. The red band. Rhodanien.

Freshwater Beds.

| The Oyster Clays. Urgonien.

Waals (Oley < Yellow Marl.

| Spatangus Limestone Sands Upper )

L and Clay. Neocomien.
Hastings Sands. (Absent). Lower

VI.—On tHE Sequence anp Systematic PostTIoN oF THE CAmM-
BRIAN Rocks oF NUNEATON.
By Prof. C. Larwortu, LL.D., F.G.S.
N the Grotocican Magazine for December, 1882,' I published a
brief note upon the “ Discovery of Cambrian Rocks in the
1 Lapworth, Grou. Mac, 1882, Dec. II. Vol. IX. p. 563.

3820 Prof. C. Lapworth—Cambrian Rocks at Nuneaton.
Neighbourhood of Birmingham,” in which evidences were adduced
demonstrative of the fact that the oldest sedimentary strata of the
Lickey Hills. and of the neighbourhood of the town of Nuneaton,
previously referred to the Llandovery and Carboniferous respec-
tively, are, in reality, of Cambrian age. Since that date these
Cambrian areas have been in part mapped by the members of the
Field Geology Class of the Mason College, and many confirmatory
and interesting points of detail have been detected by myself and
others. Some of these will be found incorporated in Mr. Jerome
Harrison’s valuable paper on the “ Pre-Carboniferous Floor of the
Midlands,” published in the Midland Naturalist for 1885.1 My friend
Mr. T. H. Waller, B.Sc., kindly undertook the microscopical
examination of the igneous rocks associated with these Cambrian
strata, but the results of his observations are as yet unpublished. I
hope to treat of the subject as a whole at the forthcoming Meeting
of the British Association, but as I have recently had to prepare a
general account of the Cambrian rocks of the Midlands for the local
“ Association Guide Book,” I have thought that a summary of my
conclusions as there laid down respecting the main fossiliferous area
of Nuneaton may be of present interest to other geologists working
among these rocks, and may serve as a point of departure for further
discussion and investigation.

The largest area of Cambrian rocks in the Midlands is that of
Nuneaton and Atherstone in Hastern Warwickshire. It extends
from the neighbourhood of Bedworth on the south to a point beyond
Merivale Park near Atherstone on the north, a distance of about
eight miles, and has a maximum width to the north of the hamlet of
Oldbury of about a mile and a quarter. On the eastern margin of the
Cambrian area its beds are overlain unconformably by the basement
beds of the Keuper Sandstone, around and to the south of the town
of Nuneaton. To the north of that town they are generally faulted
against the Keuper Marl, but are locally overlapped by some of its
basal beds. On the western side the Cambrian rocks are overlain
unconformably by the lowest sandstones of the East Warwickshire
Coalfield, but there appear evidences of faulting between the two
systems in some localities.

The sequence of the rocks of this Cambrian area is as follows :—

A. Caldecote Volcanic Rocks.

(1) A thin series of volcanic ashes, beautifully stratified, shown
in an old cutting (The Tunnel) a few yards to the north-west of
Caldecote Lodge, and forming the lowest rocks exposed in the
Nuneaton district.

(2) Quartz-felsite and diabase-porphyrite, seen in an old quarry
about a quarter of a mile south-east of Caldecote Lodge. The quartz-
felsite is often brecciated in character, and is doubtfully intrusive in
the Caldecote ashes. The diabase-porphyrite is subsequent in age to
the quartz-felsite, resting upon it, making its way into it in veins
and strings, and including fragments of the quartz-felsite caught up
in its flow.

1 Harrison, Midland Naturalist, 1885, vol. viii. pp. 38—69 et seg.

Prof. C. Lapworth—Cambrian Rocks at Nuneaton. 321

B. Harishill Quartzite.—Thick-bedded quartzite, with intercalations
of sandy shales. This formation extends from Tuttle Hill to Harts-
hill, and is exposed in many large quarries. The basement beds of
the quartzite contain abundant fragments of the Caldecote volcanic
rocks. At Mr. Boon’s quarry, between Caldecote Lodge and Tuttle
Hill, its lowest zone is laid bare, and is almost wholly made up of
this derived volcanic material.

Along a straight line ranging from the Midland Railway Station
at Nuneaton to the village of Hartshill, near Atherstone, the highest
zone of the quartzite is succeeded by the

C. Stockingford Shales.—A thick group of purple, green, grey and
black thin-bedded shales, which are separable into two main
divisions :—

(1) Purple and Green Shales (Obolella Beds).

The lowest zones of this division are stained of a deep purple
colour, and were formerly worked for manganese. Higher up the
purple shales pass up into green and grey beds, but the red beds
re-appear at intervals to the summit of the division. At Marston
Jabet, Camp Hill, and in many localities beyond Hartshill, fossils
occur, which are, however, limited to very thin seams. The com-
monest forms may be provisionally referred to:—

Lingulella pygmea, Salter. Protospongia fenestrata, Hicks.
Obolella sagittalis, Salter. Acrotreta socialis, You Seebach.
Orthis lenticularis, Dalm. Obolella Salteri, Holl.

(2) Gray shales with bands of intensely black carbonaceous shales
(Agnostus Beds).

These are divisible into two main zones :—

(a) Zone of Agnostus sociale, Tullberg.

The characteristic fossil of this band is the well-marked variety
of Agnostus pisiformis (Linn.), which gives its name to the zone.
It has been met with in these beds at Chilvers Coton, Stockingford
Cutting, and Oldbury Reservoir.

Another very characteristic fossil in the band is Beyrichia Angelini,
Barr., a well-known Swedish species. Its associated forms are a
species of Lingulella, apparently identical with Lingulella Nicholsont,
Callaway, and a species of Obolella.

(b) Zone of Spherophthalmus alatus, Beck. (?= Zone of Peltura
scarabeoides, Wahlenberg).

The characteristic fossil of this zone is the well-known Scandi-
navian species S. alatus (S. humilis, Phill.), already known from
ee British Upper Cambrian rocks of North Wales and the Malvern

ills.

It is associated with abundant specimens of an Obolella of the type
Obolella sagittalis, Salt., but with strongly-marked concentric lines
of growth (var. concentricus). Species of Agnostide occur more
rarely, together with carbonaceous remains resembling the Hymeno-
caris vermicauda of Salter, ete.

The examples of Sphzrophthalmus are locally abundant but poorly
preserved, head, body-rings, and free cheeks. They are confined,

DECADE III.—yOL. I1.—NO. VII, 21

322 Thos. H. Waller— Volcanic Rocks, Nuneaton.

as in the Malverns, to a single seam which is very difficult of
detection.

This zone is the highest band of the Cambrian visible in the
Nuneaton District, occurring immediately to the east of the uncon-
formably overlying Carboniferous. Fossils have been obtained from
it in the quarries to the south-west of Merivale Park, and in the
Stockingford railway cutting.

No recognizable fossils have been met with in the Hartshill quartz-
ite, but those enumerated above from the various zones of the Stock-
ingford shales allow us to assign the Cambrian rocks of Nuneaton
to their approximate position in the general succession of Cambrian
deposits. These Stockingford shales fall apparently into the same
systematic position as the well-known Upper Cambrian shales of the
Malvern Hills—representing the grey and black shales which there
lie between the Hollybush Sandstone below and the Dictyonema bed
above. Lingula pygmea and Obolella Salteri occur in the lowest
shale zones of the Malvern Hills, Spherophthalmus alatus and Agnostus
pisiformis ave among the characteristic fossils of the black shales
above, In other words, the Stockingford beds come into the place
of a part of the Lingula Flags of North Wales—possibly ranging to
the Upper Dolgelly. With the Scandinavian succession the agree-
ment is even closer; the zones of Agnostus sociale, Beyrichia Angelini
and Spherophthalmus alatus (= zone of P. scarabeoides) occurring in
the same order in the Midlands, in Scania and in Norway.

Although the underlying Caldecote Volcanic Group has distinctly
afforded the material of which the basement bed of the Hartshill
Quartzite is composed, it is doubtful if the systematic break between
the Caldecote and Hartshill formations is of great moment. The
Caldecote ashes have the same general strike and amount of inclina-
tion as the overlying quartzite, and are equally unmetamorphosed.

Both the Stockingford Shales and the Hartshill Quartzite are
pierced by intrusive dykes of Pre-Carboniferous diorite. This rock
has been already described by Mr. Allport, F.G.S., in a memoir which
has become classic in the history of British Petrography.

A preliminary notice of the petrographical characters of the
Caldecote igneous rocks by Mr. Waller will be found in the paper
which follows the present communication.

VII.—Pretiminary Note on THE Votcanic AND AssocIATED Rocks
oF THE NEIGHBOURHOOD oF NUNEATON.

By Tuos. H. Wattsr, B.A., B.Sc.

HE relations of the various rocks of the district lying to the
North and South of Nuneaton have already been discussed by
Prof. Lapworth from the data afforded by investigation in the field.
He put into my hands many specimens of the different rocks for the
purpose of microscopical examination. I have also received specimens
from Mr. W. J. Harrison, and have collected some myself. Mr. J.
J. H. Teall has also placed at my disposal a number of slides which
he has had prepared from material of his own collecting.

Thos. H. Waller—Volcanice Rocks, Nuneaton. 323

From these I have prepared a considerable number of thin sections,
and I propose to give here a summary of the chief conclusions at
which I have arrived as to the following rocks :—

The Ashes.

The Quartz-Felsite.

The Basic rock which is seen in contact with the Quartz-Felsite.
The Quartzite.

The Diorite in the latter.

The Ashes from the ‘‘Tunnel” at Caldecote are distinctly
bedded, and contain, where they are coarsest, angular grains of quartz
and felspar ; ; but in most parts the dust has originally been so fine,
and subsequent changes have so much veiled the components, that
not much can be made out as to their constitution. A light-coloured
specimen from this locality has an appearance and texture very
similar to those of a tuff from the Pentland Hills, of which I pos-
sess a specimen. It contains a number of rather darker grains,
which are not evenly distributed all over, but are gathered up into
a sort of network with irregular meshes, the open spaces being nearly
free from them.

A few of the felspar grains are much larger than the majority of
the fragments of which the rock is made ips ane well-defined and
pretty perfect orgie. measuring about 3'5 of an inch, another of
orthoclase measures ;3> of an pal. There are occasional fragments
of apparently a fine-grained basalt, and in some of these large felspar
crystals are included, showing that the basalt was porphyritic. I
have seen no well-defined augite, but a few green patches give
rather the impression of an altered pyroxene. The quartz fragments
are not very frequent, and the general character of the mass is
decidedly basic.

In the coarse conglomerate at the base of the quartzite, blocks of
ash are found, and those which I have examined are made up of
much larger fragments than the specimens from the Tunnel. The
fragments present a considerable variety of aspect; a few of them
look like pieces of a very vesicular lava—basic apparently : others are
pale green, like some of the Welsh felsites of the Snowdon district,
and have the peculiar curdled or damascened appearance which has
been often described in these.

2. The Quartz-Felsite.—It is only sparingly that specimens occur
which have the appearance of typical unaltered quartz-felsites. In
them the quartz and felspar occur in large grains and crystals, the
ground-mass forming as usual inclusions and indentations in the
former. In the ground-mass itself the fluidal texture is very marked,
and it shows the usual indeterminate polarization of the felsites.

The felspar is much clouded by products of decomposition, but
there is a good deal left which allows the twinning to be made out.
Both orthoclase and plagioclase occur; in the latter, frequently with
very fine and sharply-distinguished lamellee.

The greater number of specimens which have a general look of
quartz-felsite, seem to me to have much more of the character of a
felsite brecciated and recemented with probably but little disturbance.

Fe ted at ee ae

824 Thos. H. Waller—Volcanie Rocks, Nuneaton.

The quartz grains, instead of having mostly rounded outlines, are in
very large proportion angular, and have a very fragmentary look.
The felspar grains, on the contrary, are very frequently rounded, and
the whole of the crystalline constituents are packed closely together ;
touching, in the majority of cases, as if they had been loose
grains. This peculiarity of aspect naturally varies in different
specimens, and in one or two I think I have detected a quartz grain
in the act of breaking up. It is of irregular shape, and at one side
is covered over with a network of strings of minute fluid cavities,
which divide it into roughly polygonal portions ; as we pass to the
other side of the crystal, however, these become lines of an infil-
trated green mineral, and at the extreme edge a few of the polygonal
fragments are quite detached, and separated from the main mass by
portions of the ill-defined ground-mass which occurs in this particular
specimen. Here the alternative lies between considering the fluid
cavities as the remaining indications of cracks which originally
divided the crystal, or looking upon the strings of cavities as original,
and as giving direction to the separation by being planes of weakness.
It is rather in favour of the former assumption that the reticulated
arrangement of the cavities is, so far as my observation goes, more
frequent in the specimens which have the greatest appearance of
disturbance. Where the crystalline grains of quartz are indented
with intrusions of the ground-mass, there is very frequently a line of
cavities following the outline of the indentation. One specimen
shows very well the care needful in deciding that an apparent inclusion
is not in connection with the exterior. A quartz grain has a row of
four roundish apparent inclusions. The plane of the section, how-
ever, has fallen just within the neck connecting one of these included
masses with a little indentation of the margin, so that there is a very
faintly visible cloud observable showing the actual connection.

In various places in this rock there are green patches and a few
black and brown ones. These are not so sharply defined micro-
scopically as they appear in hand-specimens. In some cases they
seem to have their margins indented with a quartz grain, or to
inclose a bit of felspar ; but occasionally they seem quite free from
any but microscopic crystals. The black patches, so far as I have
examined them, have the look of green serpentinous alteration
products, and some of the browner ones have much the appearance
of the neighbouring fine ashes, but others seem more filled with
minute lath-shaped crystals, which have much of the character of
telspar microliths.

8. The Dark Basic Rock which is in contact with the quartz-
felsite in one little disused quarry has undergone great alteration—in
some parts to the complete obliteration of any original structure, in
others the components are very fairly preserved. Close to the
junction with the quartz-felsite, and running into it in strings and
tongues, the appearances strongly suggest a rock originally glassy,
which has been subsequently devitrified, like the glassy base of many
felsites. In some specimens the structure is markedly porphyritic ;
felspar crystals of considerable size occurring in a ground of crystals

Thos. H. Wallier—Volcanic Rocks, Nuneaton. 325

apparently of felspar of very small dimensions. In others the
crystals of felspar are larger and of more uniform size. Extremely
little augite has escaped, but it is curious that those which are pre-
served show, in addition to the twinning with the orthopinacoid as
the plane of composition, which is common, the unusual cleavage
parallel with the basal plane described by Mr. Teall as occurring in
the prevailing pyroxene of the Whin Sill of the North of England.
One section approximately in the plane of the clinopinacoid shows
the cleavages forming obtuse angles meeting in the plane of com-
position ; the angles were measured as 66° on one side, and 65°
on the other, and the extinctions 40° and 41° from the dividing line.
Where the colour of the augite can still be seen, it is very pale.

The larger porphyritically-developed felspars give extinction
angles such as indicate one of the more basic plagioclases, probably
labradorite. Some yellowish hornblende and a green chloritic or
serpentinous mineral are apparently products of alteration.

The manner in which this rock, which seems to agree in characters
with Rosenbusch’s diabase porphyrite, runs in among the quartz
and felspar grains of the quartz-felsite previously mentioned, the
presence of detached angular quartz grains in its mass, and the
appearance of flow which it has, lead me to believe that it flowed as
a lava over a broken disintegrated surface of quartz-felsite or of
a bed of sand derived from it.

4. The Quartzite——The quartz sand which has formed the founda-
tion of the quartzite shows in some of the lower beds its derivation
from such a rock as the quartz-felsite previously described, by the
survival of canals and inclosures of the felsitic ground-mass, and
indeed, in the conglomerate, quite at the base, little pebbles of felsite
occur along with angular fragments of the fine ashes. In the normal
quartzite the grains of primary quartz are well rounded, and contain
in many cases a great number of minute fluid cavities. The secondary
cementing quartz is much more free from cavities or inclusions
of any sort. It is an optical continuity with the primary quartz,
so that in polarized light the impression is given of polygonal areas
of colour. The appearance is markedly different where, as is quite
frequently the case, a grain of felspar, or of felsite, or of the ashes,
occurs. On these no quartz is deposited, but they are simply
enveloped in that which has crystallized on adjoining grains.

d. The Diorites which occur in the quartzite are in an advanced
state of alteration, and often not much more than the shapes of the
old crystal forms can be made out. Calcite is developed in them to
a considerable extent.

In a specimen from Tuttle Hill, collected by Mr. Teall, and kindly
lent to me by him, the hornblende is in the form of long and com-
paratively slender crystals, with frequent cross-divisions. A similar
structure occurs in a specimen from Merivale Church, kindly given
to me by Mr. W. J. Harrison.

326 Reviews—Dr. Max Schlosser on the Ungulata.

SEVER) eee Ni Se

—_—_——_-
I.—Dr. Max Scutosser on tHE UNGULATA!

HE author of this memoir, which aims at giving a complete
pedigree of all the Perissodactyla and Artiodactyla, is to be con-
gratulated on the amount of information he has brought together, and
the strong thought characterizing the whole of it. The pedigrees
are indeed given as though they were certain, but we have no doubt
that the author himself would admit that they must be regarded as
indications only of the way in which the line of evolution may have
advanced, rather than the absolute line itself. The author’s American
experiences render his observations as to the probable identity of
many American and European genera of especial value.

The Condylarthra the author regards as the primitive stock from
which both the Perissodactyla and Artiodactyla have originated, and
points to Phenacodus as being very closely allied to Hyracotherium.
Instead of the nine or ten families into which the Perissodactyla are
usually divided, Dr. Schlosser proposes to reduce the number to four.
Thus the Lophiodontide gives its type genus to the Tapiride, while
Hyracotherium and its allies, together with the Paleotheriide, are
included in the Hquide. That there is very much to be said in
favour of the inclusion of the Paleotheriide in the latter is perfectly
true, since the division between them is but an arbitrary one; and
there is an equal transition from the Paleotheriide through Pachy-
nolophus to Hyracotherium. It seems, however, hardly consonant
with the usual acceptation of the term to include in one family such
widely different forms as Hyracotherium and Equus, even although
the one be the ancestor of the other; and the total separation of the
former from Lophiodon, to which it seems to us to be more nearly
allied than is that genus to Tapirus, appears decidedly inadvisable.
Dr. Schlosser appears, indeed, to think it necessary that all the
members of one line of evolution must be included in a single
family; but we would point out to him that since he admits the
descent of the suborder Perissodactyla from the suborder Condylar-
thra, there is no objection against adopting the same view in the
case of families, and regarding the Equide as descended from the
Paleotheriide, and the latter from the Lophiodontide, which may
have also given rise to other groups. The Chalicotheriide forms the
third family, which is taken to include both the Mesodontide and
Macraucheniidz; and we confess we should like more conclusive
evidence in favour of this view, as the dentition of the latter appears
to indicate affinity with Palgotherium. 'The Rhinocerotide includes
the true Rhinoceroses, Hyrachyus and Elasmotherium.

We may here be permitted to express some surprise that while the
author so reduces the number of families, he follows the example of
Gray in retaining a vast number of genera; and we regret (even if
it be only on the lowly ground of pity to the power of memory of
average mortals) that he did not follow the excellent example of

1 “ Beitrage zur Kenntniss der Stammesgeschichte der Hufthier, etc.,’’ Morphol.
Jahrbuch, yol. xii. pp. 1-136, pls. i.-vi. (1886).

Reviews—Dr. Max Schlosser on the Ungulata. 327

Prof. Flower in including all the recent Rhinoceroses and most of
the fossil ones in a single genus, as well as in uniting Paloplotheriwm
with Palceotherium. We are glad to see the identity admitted of
Orohippus with Hyracotherium, and the suggestion that Hohippus may
also be the same; but we are surprised at the retention of Pliolophus
(with which Orotherium is coupled) as distinct from Hyracotherium.
Mesohippus and Miohippus are rightly shown to be indistinguishable
from Anchitherium, and Protohippus from Hipparion. Some confusion
appears to exist in the author’s mind with regard to Pachynolophus,
since he separates it widely from the so-called Propalgotherium,
which Gaudry has shown to be identical. The confusion may be in
part accounted for by the retention in Hyracotherium of the so-called
Hi. siderolithicus, which is really a Pachynolophus ; but it is difficult
to understand what forms Dr. Schlosser regards as the representatives
of the latter genus. The genus Yapirulus, which has been very
generally regarded as an Anoplotheroid, is referred to the Tapiride,
but we could wish for stronger evidence on the point.

In the Artiodactyla the same “lumping” of families is observ-
able. Thus the author proposes (1) the Anoplotheriide, (2) the
Dichobunidz, which is subdivided into the Dichobunidz proper, the
Cznotheriide, Xiphodontide, Tragulide, and Gelocide, (3) the
Tylopoda, (4) the Oreodontide, (5) the Anthracotheriide, and (6)
the Suid. We are not quite clear as to the author’s views with
regard to the Giraffide, Cervide, and Bovide (which is split
into Bovide, Antilopide, and Ovide) ; but they are all regarded as
descendants of the Gelocide, and it is apparently intended that
they should be considered merely as subdivisions of that sub-
family,—a view which will hardly commend itself to the Hng-
lish school of zoology. The comparatively wide separation of
Xiphodon from Anoplotherium is in opposition to the view of Prof.
Riitimeyer, which is based on the resemblance presented by the
former to the undoubted Anoplotheroid genus Dacrytherium; and
we are inclined to give more weight to the remarkable resemblance
existing between the molar dentition of the three genera and
the affinity of their general carpal and tarsal structure, than to
the features of carpal and tarsal reductions respectively known as
adaptive and inadaptive. Xiphodon does, however, undoubtedly
show strong indications of affinity with the Czenotheriide and the
Dichodontidee (Gelocide), and thus indicates a transition from the
Anoplotheriide to the Tragulide. The author adopts the recent
view of not separating Eurytherium from Anoplotherium. Lophio-
meryx, which was placed by Riitimeyer between Dichodon and
Gelocus, is referred to the Tragulide, which also contains Bachithe-
rium ; Lophiomeryx Gaudryi, we regret to see, has been made the
type of another new genus—Cryptomeryx. The Anthracotheriida
are taken to include Merycopotamus, and also the bunodont Elother-
ium (Entelodon), which is classed by Prof. Flower together with
Cebocherus and Cheropotamus in the Cheropotamide. The Suidee
is taken to comprise the two latter genera, together with the Dicoty-
lida, Phacochceride and Listriodontide, and the peculiar genus

328 Reviews—Dr. C. Depéret’s Pliocene Vertebrata.

Acotheridum, which, although presenting dental characters allied to
Cebocherus, yet in other respects is so like Dichobunus that it is
difficult to think that it is not nearly allied. Both Palgocherus and
Cheromerus are retained as distinct from Hyotherium.

We venture to think that the plan of taking one very large family
like the Dichobunide and subdividing it into several subfamilies
(all of which have the same termination), and the apparent sub-
division of one of these subfamilies into sub-subfamilies is not ad-
visable, and is sure to lead to confusion;! and we should have
thought it better to rank such subfamilies as families, since it is
quite impossible to attempt to make all families or other divisions
of precisely the same relative value. That the author himself has
not succeeded in this we think is evident, when he sees reason to
place Anthracotherium and Cheropotamus in juxtaposition, while
Cenotherium and the closely allied Dichobunus are made the types of
separate subfamilies ; but this is still more glaringly the case if the
Dichobunidz is to include all the Pecora (as a subdivision of the
Gelocidz), and yet not to have higher rank than the Oreodontide.

It is, however, hardly to be expected that any two persons can
entirely agree on such points, and in concluding this notice we beg
to congratulate the learned writer on this decidedly valuable contri-
bution to morphological zoology. R. LypekkKer.

IJ.—Dr. C. Depiret on tHe PuioceNE VERTEBRATA OF FRANCE.”

HIS memoir will be welcomed by all students of the Pliocene
Mammalia of the South of France, as it throws much light on
many of the forms imperfectly described many years ago by Croizet
and Jobert, and Aymard. The work consists of three parts: Ist, a
geological description of the Rouisillon basin ; 2nd, a description of
the Vertebrates; and, 3rd, a survey of the Pliocene Vertebrates of
Europe. In the Pliocene the author includes all the strata from the
Norfolk Forest-bed to the Montpellier and Casino beds, and follows
the usual French view of classing the Pikermi and Mont Lebéron
beds with the Upper Miocene instead of at the base of the Pliocene.*
The only new species of Mammal described is Viverra Pepracti,
which appears intermediate between V. civetta and Ictitherium; but
there are several interesting forms which may be briefly mentioned.
The so-called Antilope boédon is referred to Palgoryx, while A. torti-
corns, Aymard, which has been shown in an earlier memoir to be

1 We have already been obliged to quote such subfamilies in the same rank with
families.

* Théses Présentés 4 la Faculté des Sciences de Paris, sér. A. No. 67, pp. 1-268,
pls. iv. (1885). The writer of this notice regrets that the work did not come into
his hands in time to incorporate some of its information in the British Museum
Catalogues,

3 In arecent memoir (Bull. Soc. Géol> France, sér. 3, vol. xiii. pp. 287-94 [1886]).
Prof. Gaudry defends the former view. Since the:learned Professor admits the inter -
calation of Pliocene marine strata in the Pikermi beds, all his reasons appear to us
(be it said with all respect) to present a strong savour of the kind of argument known
as ‘‘ begging the question.”

Reviews—Cumberland and Westmoriand Association. 3829

intermediate between Palgoreas and Tragelaphus, is referred to the
latter genus, although classed by M. P. Thomas with the former ;
the occurrence of these Antelopes allied to those of modern Africa
at such a recent epoch is of much interest. Sus arvernensis is con-
sidered indistinguishable from S. provincialis, and closely allied to
the existing African S. (P.) africanus. The Hipparion is identified
with H. crassum, Gerv., and regarded as distinct from H. gracile ;
and it is suggested that the Montpellier form may also be the same.
The Rhinoceros is referred to R. megarhinus (leptorhinus), but (apart
from the evidence of the imperfect cranium) it appears to us almost
certain that the dentition represented on pl. i. belongs rather to R.
etruscus—the teeth being apparently brachydont, the upper pre-
molars showing the strong horizontal cingulum and the third costa
characteristic of that species, and the lower molar also exhibiting the
distinctive cingulum at both extremities. Among other interesting
forms we may mention Testudo Perpiniana, which is as large as T.
elephantina, and a spine indicating the occurrence of a Siluroid which
it is suggested may be allied to Clarias.

Almost the only point with which we can find fault is the reten-
tion of names like Macherodus Sainzelli and M. pliocenus, which, if
not mere synonyms, are from the want of figures of no possible
value. The work, with other memoirs by the same author, will be
indispensable to all future students of the Fossil Mammalia of
France. R. LyDeKkKer.

TI].—Transactions oF THE CUMBERLAND AND WESTMORLAND ASSO-
CIATION FOR THE ADVANCEMENT OF LITERATURE AND SCIENCE.
No. X. 1884-85.

OUR papers of geological interest are contained in this volume.
Mr. W. G. Collingwood discourses ‘On Lake-basins of the
neighbourhood of Windermere,” observing that those which do not
lie in anticlinal or synclinal breaks coincide with faults. He has
failed to find any evidence of ice-erosion in the minor lake-basins,

although ice may have helped to free them from detritus. Mr. J.

Postlethwaite contributes a paper on “Trilobites of the Skiddaw

Slates,” which is illustrated by four plates. The paper simply deals

with the general characters of the specimens and with their localities,

but few names being given. Great interest however attaches to
them as many of the forms are new. These have been named by
the author and Mr. J. G. Goodchild in a paper lately read before the

Geologists’ Association. Mr. H. W. Schneider communicates an

article “ On the Hematite Iron Mines of Low Furness,” from which

the total production of pig-iron amounts annually to about 550,000

tons; and Mr. J. D. Kendall replies to a previous paper by Mr. T.

V. Holmes “On the Best Locality for Coal beneath the Permian

Rocks of North-west Cumberland.”

We took occasion when noticing’a former Part of these ‘“ Trans-
actions” to observe that the plan of the Cumberland Association
might well be adopted in other counties, where more than one Natural
History Society exists. A very proper rule is to print only those

330 Reports and Proceedings—

papers which are local and original. We regret to learn that on
account of this rule, the Whitehaven Scientific Association has
severed its connection with the Cumberland Association. Surely
unity is strength, and surely there are members of the Whitehaven
Association who could aid in the progress of science without
departing from the salutary rules framed for the benefit of the many.
The multiplication of local “Transactions ” is a serious evil.

ceva @ ieee SS) ZAG ee @ Car Shee

——$>———__
Grorocicat Society oF Lonpon.

I.—May 26, 1886.—Prof. J. W. Judd, F.R.S., President, in the
Chair.—The following communications were read :

1. “ Further Proofs of the Pre-Cambrian Age of certain Granitoid,
Felsitic, and other Rocks in North-western Pembrokeshire.” By
Henry Hicks, M.D., F.R.S., F.G.S.

In this paper the author gave the results obtained by him during
a recent visit to N. W. Pembrokeshire. He stated that he had
further examined some of the sections referred to in his previous
papers, as well as others not therein mentioned, and that he had
obtained many additional facts confirmatory of the views expressed
by him in those papers. The Lower Cambrian conglomerates and
grits, he said, contained pebbles of nearly all the rocks in that area
which he had claimed as of pre-Cambrian age; and the fragments
of the granitoid rocks, the felsitic rocks, the hialleflintas, and of the
various rocks of the Pebidian series which he had found, showed
unmistakably that those rocks had assumed, in all important particu-
lars, their peculiar conditions before the fragments were broken off.

Moreover, he stated that there was abundant evidence to show
that the very newest of the pre-Cambrian rocks of the area had been
greatly crushed, cleaved, and porcellanized, before any of the Cam-
brian sediments were deposited ; hence he maintained that there
was in the area a most marked unconformity at the base of the
Cambrian. At Chanter’s Seat, near St. David’s, he found that the
Lower Cambrian grits and conglomerates were, in parts, almost
wholly made up of fragments of characteristic varieties of the
Granitoid rocks which form the Dimetian ridge near by.

The so-called granite of Brawdy, Hayscastle, and Brimaston, he
said, there was good evidence to show, was probably of the age of
the Granitoid rocks of St. David’s. The mass of so-called granite
near Newgale, he stated, was composed of rhyolites and breccias,
undoubtedly of pre-Cambrian age.

The Roch Castle and Trefgarn rocks, he stated, could not possibly
be intrusive in Cambrian and Silurian strata, but belonged to a
series of pre-Cambrian rocks. He referred to the important evidence
bearing on the age of these rocks given in a paper communicated to
the Society, since his last paper was read, by Messrs. Marr and
Roberts. These authors showed that in a quarry near Trefgarn

Geological Society of London. 331

Bridge a Cambrian conglomerate, overlain by Olenus-shales, is to be
seen resting on the eroded edges of the Trefgarn series. The author
examined this section lately, and obtained from the Conglomerate
some very large pebbles of the characteristic rocks called hilleflintas,
and of the ash-bands, both of which are found in situ in the quarry.
He therefore maintained that there was the most ample evidence to
show that there was a great group of pre-Cambrian rocks exposed in
N.-W. Pembrokeshire, and hence that he had proved conclusively
that Dr. Geikie’s views in regard to these rocks, as given in his
paper and more recently in his text-book, are entirely erroneous.

2. “On some Rock-specimens collected by Dr. Hicks in North-
western Pembrokeshire.” By Prof. T. G. Bonney, D.Sc., LL.D.,
F.R.S., F.G.8.

The author stated that he had examined microscopically a series
of specimens collected by Dr. Hicks, and compared them with those
described by Mr. T. Davies, in vol. xl. of the Quarterly Journal, and
with some in his own collection. He agreed with Mr. Davies’s
conclusions in all important matters.

The Chanter’s-Seat conglomerate contained many grains of quartz
and felspar, curiously like those minerals in the so-called Dimetian,
together with numerous small rolled fragments, about a quarter of
an inch in diameter, exactly resembling the finer-grained varieties
of that rock, besides bits of felsite, similar to some which occur in
the St. David’s district, quartzite, a quartz-schist, and an argillite.

The rocks in situ in the Trefgarn quarry were indurated trachytic
ashes, together with the curious flinty rock which was the most
typical of the so-called hiilleflintas. One of the pebbles from the
overlying conglomerate perfectly corresponded with the last-named
rock, others appeared to be most probably from an altered trachytic
ash, differing only varietally from those in situ.

After prolonged examination of this “halleflinta” of Trefgarn
and the similar rocks from Roch, he was of opinion that while it was
possible that some specimens might be altered ashes, most of them
were originally rhyolites or obsidians, devitrified, and then silicified
by the passage of water which had contained silica in solution.
The Trefgarn group obviously could not be intrusive in the Lower
Cambrian, and it was extremely improbable that the Roch Castle
series was newer than the basement conglomerate of that district.

The Brawdy granitoid rock might be a granite, but at any rate it
presented considerable resemblance to the ‘‘ Dimetian.”

It was therefore evident that the Cambrian conglomerate of St.
David’s was formed from a very varied series of rocks, some of them
much older than it, and that the Dimetian could not be intrusive in
it. Moreover, even if the Dimetian should be proved ultimately to
be a granite, and the core of a volcano which had emitted the rhyo-
lites, sufficient time must have elapsed after its consolidation and
prior to the making of the conglomerate to remove, by denudation,
a great mass of overlying rock. Hence, whatever its nature, it was
pre-Cambrian.

3. “On the Glaciation of South Lancashire, Cheshire, and the

O32 Reports and Proceedings—

Welsh Border.” By Aubrey Strahan, Esq., M.A., F.G.S., H.M.
Geological Survey. By permission of the Director-General.

Part J. Soutra LancasHIRE AND CHESHIRE.

The average direction of the large number of glacial strize: which
have been observed in the neighbourhood of Liverpool is N. 28° W.
Further up the Mersey there is a slight deflection towards the east.
Two instances only occur of striz having a totally different direction,
namely H.N.E. The striz themselves seldom furnish any evidence
as to the direction in which the ice travelled, but the edges of the
strata have in many cases been bent back from the north-west.
The materials of which the drift is composed, both matrix and in-
cluded boulders, have also travelled from the north-west. The sands
and gravels also are arranged in long banks, trailing away from the
south-west sides of the rock-hills, in such a way as to show that
they were distributed by currents from the north-west. The striz
are found in connexion with the Boulder-clays, in which the actual
presence of ice is abundantly proved. Presumably the same agent
that distributed the Boulder-elay also striated the rock-surface and
moved from the north-west.

Part II. Tae Weusu Borper.

The striations within the Welsh Border also show a general
parallelism, but in a direction E.N.E., the few exceptions that occur
being close to the Border. The direction in which the drift has
been transported shows a corresponding change ; though analogous
in arrangement to the Lancaster drift, it has all travelled from
W.S.W. to E.N.E. The boundary between the northern drift of
the English side and the western drift of the Welsh runs approxi-
mately along the coast, bending inland here and there, and cutting
inland across parts of South Flintshire and Denbighshire. The
transportation of the Welsh drift has taken place across the lines of
the principal hill-ranges and valleys. Occasionally the two drifts
shade one into the other, or are mixed together; but as a general
rule the far-travelled northern drift overlies the more local deposit,
and is easily distinguishable by its different materials and by its
being comparatively stoneless.

It may be concluded that :—

1. The striz on the English and Welsh sides respectively, while
showing variations among themselves, by a marked preponderance
in one quarter of the compass, indicate a direction of principal
glaciation, this direction being on the English side from about
N.N.W., and on the Welsh from about E.S.E.

2. The direction of glaciation in both districts agrees very closely
with that of the transportation of the drift, but is only locally
influenced by the form of the ground.

3. The striz are by no means universal, but are found almost
exclusively in connexion with those beds in the drift which contain
evidence of the actual presence of ice.

Geological Society of London. i315)

Part III. Or1iGIn oF THE STRIZ.

The striz are not such as can have been produced by valley-
glaciers; they go across and not down the valleys, nor are there
any moraines. The question resolves itself into (1) the hypothesis
of two ice-sheets moving in different directions in the two areas ;
(2) that of floating-ice. The first is opposed by the facts that the
rock-surface is not moutonnéed ona large scale, and that the striz and
terminal curvature are far from universal ; that the drifts associated
with the stris are marine deposits; that strie having different
directions are found on the same slab. The well-known occurrence
of gravel-ore in the drift at the outcrop of a vein is also against this
hypothesis. The marine origin of the drifts is indicated by their
well-marked stratification as a whole, by the alternations of well-
washed sands and gravels with the Boulder-clays, and by the occur-
rence through all the beds of marine shells. A lower or basement-
clay is seen in places under this marine drift, but it is always the
latter with which the striz are associated. The great development
of undoubted marine beds and comparative rarity of moutonnéed sur-
faces constitute the principal differences between this region and
the north, where the existence of an ice-sheet has been strongly
advocated. Anglesey is considered by Sir A. Ramsay to have
received its configuration by the action of an ice-sheet from the
north; but its physical features appear to be due rather to its geo-
logical structure, and to have existed in more or less their present
form in pre-glacial times.

The arrangement of drifts in this district presents an analogy with
that of the Norfolk drifts, and probably results from a similar
sequence of events.

The marine drifts, from their great variability, seem to have been
distributed, and the striations produced by floating-ice, driven by
tidal or oceanic currents, during the time of submergence. During
this time Snowdon and the surrounding hills must have stood well
above water, forming an island-group, and by such a group the pre-
vailing currents from the north would be deflected to the south-west
over Anglesey on the one side, and to the south-east over the plains
of Cheshire and Shropshire on the other, while within the limits of
the group a local circulation might be maintained.

Il.—June 9, 1886.—Prof. J. W. Judd, F.R.S., President, in the
Chair.—The following communications were read :—

1. “On the Volcanic Rocks of North-eastern Fife.” By James
Durham, Esq., F.G.S., with an Appendix by the President.

After describing the general distribution of the volcanic rocks of
Old Red Sandstone and Carboniferous age in the counties of Forfar
and Fife, the author called attention to a fine section exhibited
where the Ochil Hills terminate along the southern shore of the
Firth of Tay. In immediate proximity to the Tay Bridge, a series
of the later volcanic rocks, consisting of felstones, breccias, and
ashy sandstones, are found let down by faults in the midst of the

834 Reports and Proceedings—Ceological Society of London.

older porphyrites (altered andesites) which cover so large an area
in the district. The breccias contain enormous numbers of blocks
of ared dacite (quartz-andesite), and inclosed in this rock angular
fragments of a glassy rock, resembling a “ pitchstone-porphyry,” are
found, everywhere, however, more or less converted into a white
decomposition-product. The youngest igneous rocks of the district
are the bosses and dykes of melaphyre (altered basalt and dolerite),
which have been often so far removed by weathering as to leave
open fissures.

In the Appendix three very interesting rocks were described in
detail. The rock of the Northfield Quarry, which is shown to be
an augite-andesite, has a large quantity of a glassy base with felted
microlites, and contains large porphyritic crystals of a colourless
augite. The rock of the Causewayhead Quarries is described as an
enstatite-andesite ; it has but little glassy base, being made up of
lath-shaped felspar crystals (andesine), with prismatic crystals and
grains of a slightly ferriferous enstatite; there are no porphyritic
crystals, but the enstatite individuals are sometimes curiously agere-
gated. ‘The red porphyritic rock from the breccias near the Tay
Bridge was shown to be a mica-dacite, and the glassy rock asso-
ciated with it to be the same material with a vitreous in place of a
stony base. This glassy base exhibits very beautiful fluidal and
perlitic structures. The crystals of first consolidation in this rock
are oligoclase and biotite, often showing marks of injury in trans-
port; those of the second consolidation appear to be orthoclase. In
conclusion, the successive stages by which the andesitic rocks of the
area were altered, so as to assume the characters distinctive of por-
phyrites, were fully discussed, as well as the change of the glassy
rock into its white decomposition-product.

2. “On some Eruptive Rocks from the Neighbourhood of St.
Minver, Cornwall.” By Frank Rutley, Esq., F.G.S.

The rocks described in this paper were derived from Cant Hill,
opposite Padstow, and from a small quarry about half a mile from
Cant Hill, near Carlion. At the former locality the volcanic rocks
are much decomposed, but from their microscopic characters they
may be regarded as altered glassy lavas of a more or less basic type.
No unaltered pyroxene, amphibole, or olivine is to be detected in the
specimens described, but there is a considerable amount of secondary
matter which may include kaolin, serpentine, chlorite, palagonitic
substances, etc. There is evidence of fluxion-structure in some of
the sections ; others are vesicular, and the vesicles are usually filled
with siliceous or serpentinous matter. The relation of these lavas
to the underlying Devonian slates was not ascertained. The rock
occurring near Carlion contains numerous porphyritic crystals of
augite, in which the crystallization is interrupted by the co-develop-
ment of small felspar crystals, which appear, as a rule, to have been
converted into felsitic matter. Ilmenite is also present in patches
which indicate a similar interrupted crystallization to that shown by
the augite. The rock has the mineral constitution of an augite-
andesite; but since it is a holocrystalline rock, exception would be

Oorrespondence—Ur. S. J. B. Skertchley. 300

taken by many petrologists to the employment of the term andesite.
The lavas of Cant Hill were also probably of an andesitic character,
so that, so far as original mineral constitution is concerned, there is
some apparent justification for the mapping of both of these rocks
as “ greenstone” by the Geological Survey.

3. “The Bagshot Beds of the London Basin.” By H. W.
Monckton, Esq., F.G.S., and R. 8. Herries, Esq., B.A., F.G.S.

The authors stated that their object was to describe more fully the
Lower Bagshot beds, and to disprove the view lately advanced by
Mr. Irving that, in certain places, the Upper Bagshots overlap the
Lower and rest directly on the London Clay. ‘They described or
referred to a number of sections all round the main mass, beginning
at St. Ann’s Hill, Chertsey, where they considered that the mass of
pebbles and associated greensands must be referred to the Middle
Bagshot. The outliers near Bracknell and Wokingham were shown
to consist of Lower and not Middle Bagshot, which does not appear
in the valley north of Wellington College.

The Aldershot district was explained, and it was shown that the
beds there resting on the London Clay were Lower and not Middle
Bagshot, and the occurrence of fossils in the Upper Bagshot of that
district was recorded.

The conclusions that the authors came to were, that a well-marked
pebble-bed was almost always present, marking the division between
the Upper and Middle Bagshots, but that there were other pebble-
beds of a less persistent character occurring both in the Middle and
Lower Bagshot ; that the Lower Bagshots generally consist of false-
bedded sands with clay lamine and no fossils except wood, whereas
the Upper Bagshots are rarely false-bedded, and are characterized
by the absence of clay bands and the presence of marine fossils ; and
that the Middle Bagshot is a well-marked series consisting of green
sands and clays.

They claimed, in conclusion, that there was no reason for dis-
turbing the old reading of the district, and that there was no evidence
of an overlap of the Lower Bagshots by the Upper.

CORRES PON Daw C=.

——

SLICKENSIDED SURFACES OF CHALK.

Srr,—Mr. H. Hutchins French, F.G.S., and I have discovered
widely spread surfaces of chalk slickensided horizontally in the
neighbourhood of Sutton, Surrey. There seems to be abundant
evidence that these markings are really due to friction, and they are
associated with a remarkable cleaved structure at a high angle to
the bedding. This cleavage is very striking, and we should be
glad to receive any notices of similar phenomena in the Chalk.

We also find the Thanet Sand to extend further west than was
supposed to be the case, it being some 15 feet at Leatherhead, where

3836 Correspondence—Rev. O. Fisher—Mr. J. S. Gardner.

it was supposed to have died out, or to have been overlapped by the
Woolwich Beds.

We have prepared some interesting new sections in the Lower
Tertiaries around Epsom, which we hope to publish shortly.

CARSHALTON, SURREY, Sypney B. J. SKERTCHLY.
May 10th, 1886.

MEMORANDUM FOR GEOLOGISTS VISITING WEYMOUTH.

Str,— Driving from Weymouth the other day, I noticed some
magnificent blocks of the cherty flint of Bincombe Down,! placed to
be broken up for mending the road. This shows that the part of the
Lower Eocene bed there is now open which contains these blocks.
I would strongly advise any geologist visiting Weymouth, who is
conversant with the Cretaceous series, to examine these blocks. If
I am not mistaken, they represent some horizon which has entirely
disappeared from the area. It does not seem to me quite certain
whether they are flints, altered in texture, or whether they are
chert. In shape and size they are like those which are and have
been worked for implements at Brandon; but in texture they are
quite different, being grey throughout and opaque, with many casts
of fossils. Similar flints, containing similar fossils, occur in the
extraordinary flint bed resting upon the Greensand of Haldon Hill,
near Hxeter: and there is a collection of the fossils in the Hxeter
Museum ; as there is also a small collection of the Bincombe fossils
at Dorchester.

The observer must not be deceived by certain flints to be seen in
walls, etc., along the Weymouth road, which are not chalk flints,
but come out of the Portland beds at Bincombe. ‘They are usually
nearly spherical in shape, and black inside. O. FisHEr.

DOES TEREDO INHABIT FRESH WATER?

S1r,—I have found an account by Dr. E. P. Wright of a new Teredo
which he names Nausitoria from the Ganges, in the Linnean Soc.
Trans. 1864, p. 451. It is found in the river Comer, a loop which
runs separately from the Ganges for 80 miles, when it rejoins the
main river at Mandarapore, 70 miles from the sea. The water for
30 miles below Mandarapore is perfectly fresh, when it becomes
slightly brackish at full tide; but in the Comer it is always quite
fresh and soft and used for drinking, washing, etc. Trees and boats
are however attacked by a Teredo in it, and hence Dr. Wright be-
lieves that at all events this species does live in perfectly fresh
water. J. S. GARDNER.

* See Damon’s Geology of Weymouth and Portland, 2nd edition, p. 143,

THE

GEOLOGICAL MAGAZINE.

NEW) SERIES. ~DECADE. [lls VOL.) Il.
No. VIII.—AUGUST, 1886.

On eae Ase, (ASE sate @ dase Se

——— —

I.—Notr on Hopryrton ? expLtanvatTum, Hicks, anp on HyaLosTeLia
(PreirovEMA) FAscicuULUs, M‘Coy, sp.

By Georce Jennincs Hinpz, Ph.D., F.G.S.
R. W. CARRUTHERS, F.R.S., lately called my attention to

the resemblance between some drawings I was showing to him
of Hyalostelia fasciculus, M‘Coy, sp., and the supposed fossil plant,
described and illustrated by Dr. Henry Hicks, F.R.S., in the
GrotocicaL Macazine for 1869, Vol. VI. p. 584, Pl. XX. Figs. la-e,
under the name of Hophyton ? explanatum.

The following is the description given by Dr. Hicks of this fossil :
“A raised moderately convex stem about four lines in breadth;
widening however and becoming somewhat compressed at the joints.
The surface is ribbed and furrowed along its whole length. At the
lower joints, the ribs bend outwards, evidently to form a branch.
The joint is obliquely placed, widened out, and its course distinctly
marked by a deep sulcus. The cortical substance is very thin, and
can be removed to show the internal structure. The internal struc-
ture is made up of compressed columns, running the whole length
from joint to joint, evidently of a tubular nature, and bound together
by very thin tissue.”

Owing to the fact that no structure had been discovered in the
type forms of the genus Hophyton, Dr. Hicks placed this fossil only
provisionally under the genus, but he at the same time stated that
there could be no reasonable doubt of its vegetable nature, and that
its affinity to the vascular cryptogams was most clearly shown.

Its plant-characters, however, were not acknowledged by Mr.
Carruthers, who wrote respecting it: “It is very doubtful whether
this fossil belongs to the Vegetable Kingdom. The large-sized
continuous tubes of which it is composed are unlike plant-structure ”
(Seemann’s Journal of Botany, vol. viii. p. 138).

Subsequently, in the Quarterly Journal Geol. Soc. for 1881, vol. 37,
p- £90, Dr. Hicks again refers to the same fossil in the following
paragraph: ‘Of Hophyton ? ecplanatum, which I found in the Tremadoe
rocks of St. David’s, I fear the evidence is scarcely sufficient to ally
it with land-plants. Its strong tubular structure renders it unlike
any known land-plant; and the only other fossil found yet, to which
it can be compared, is the Pyritonema of Prof. M‘Coy, placed by him

DECADE III.—VOL. III.—NO. YIII. 22

038 Dr. G. J. Hinde—On a Paleozoic Sponge.

amongst the Zoophytes, though its true nature is still a matter of
much doubt.”

Being desirous of ascertaining the true character of Hophyton
explanatum, I applied to Dr. Hicks, who very kindly at once for-
warded to me the original specimen, as well as two microscopic
sections which had been prepared from it, and these very distinctly
showed that Dr. Hicks was quite correct in his later comparison of
the fossil to the Pyritonema of M‘Coy. I have also been enabled to
compare it with the type specimen of Hyalostelia (P.) fasciculus, M‘Coy,
belonging to the Cambridge Woodwardian Museum, which was kindly
lent to me by Prof. T. McKenny Hughes, and also with examples of
the same species in the British Natural History Museum, the Jermyn
Street Museum, and others kindly forwarded to me by Mr. G. H.
Morton, F.G_S., from Pont Ladies, Llandeilo.

Dr. Hicks’s specimen is shown on the fractured surface of a slab of
hard black shale, which, judging from the distorted forms of the
Brachiopods in it, must have been strongly compressed. It has the
appearance of an elongated, slightly convex band with delicate longi-
tudinal strie or ribs. The band, which is about 5:5 mm. in width
and 15 mm. in thickness, can be traced continuously in a nearly
straight direction throughout the slab ; in one place it is slightly bent
and traversed obliquely by an incomplete fracture, which was sup-
posed by Dr. Hicks to be a joint in the stem, but which probably
arises from compression in the rock. The band, for some distance,
is enveloped by a thin coating of the shaly matrix, supposed to have
been a cortical tissue; where this is absent, the constituent spicular
rods are clearly exposed.

Fig. 1. Hophyton ? explanatum, Hicks = Hyalostelia fasciculus, M‘Coy, sp. Trans-
verse section of the bundle of spicular rods. From Dr. Hicks’s type-specimen.
5, 1a. The same, showing longitudinal sections of some of the rods.
», 2. A single spicular rod of Hyalonema mirabile, Gray. The figures are all
drawn to the same scale of eight diameters.

The apparent band is, in fact, a bundle of solid, elongated, cylin-
drical spicular rods, disposed parallel to each other, and for the most
part in close contact, but without any organic connection with each
other. In some instances the rods are compressed together so as to
become partially flattened, but originally they appear to have been
circular in transverse section. The minute interspaces occasionally
intervening between the rods are filled by the rock-matrix, and there

a

Dr. G. J. Hinde—On a Paleozoic Sponge. 339

are no traces of any enveloping structure inclosing the bundle. The
rods vary from 15 to ‘5 mm. in thickness, they are now of chalce-
donic silica, and for the most part solid throughout, in only a single
instance did J see an indication of an axial canal. Delicate wrinkled
lines cross the rods transversely and apparently represent the slight
projecting frills met with in other specimens.

In all important characters, Dr. Hicks’s specimen so closely re-
sembles the typical example of Hyalostelia (Pyritonema) fasciculus,
M‘Coy,! that there is no reason to regard it as specifically distinct.
The individual rods do not reach the maximum thickness of some of
those in the typical form of the species, but the differences are not so
great as to be of specific value.

Having established the similarity between these forms, it is desir-
able to point out that the relationship, indicated by M‘Coy, of Pyri-
tonema fasciculus to the glass-rope of Hyalonema mirabile, Gray, is of
a genuine character. This has been called in question, amongst others,
by Prof. G. Lindstroém,* who states that M‘Coy’s species ‘is nothing
but a silicified and consequently somewhat altered Heliolites. It
must be confessed that the purely diagrammatic figure given by
M‘Coy (Brit. Pal. Foss. pl. i. B, fig. 18a) might readily give rise to
this conclusion. Prof. F. Roemer? also states that the systematic
position of the genus, in which species allied to the present one are
placed, is very uncertain. JI also found the specimens of this species
in the Jermyn Street Museum, placed with the Annelida of the
Llandeilo group, probably on account of their close resemblance to
Hyalostelia (Serpula) parallela, M‘Coy, sp., from which they can
hardly be distinguished.

At the time when M‘Coy compared Pyritonema fasciculus with the
rope of Hyalonema mirabile, Gray, the true sponge nature of this
latter form was stoutly denied by Dr. Gray, who then regarded the
rope as the skeleton of a Zoophyte, and M‘Coy also adopted this
opinion. It is now well known that ropes or tufts of long spicular
rods are common appendages in many of the deep-sea hexactinellid
sponges, and the resemblance of these to the fossil forms is very
striking.

In both recent and fossil examplesthere is asimilar form and arrange-
ment of the spicular rods in bundles; the rods correspond in dimen-
sions, in their siliceous composition, and, when the fossil forms are well
preserved, in the possession of axial canals, and even the concentric
layers of the rods can be seen. In some species, though not in the
present one, some of the fossil rods terminate in four recurved hooks,
precisely as in the recent examples. In another structural feature
also, which has not hitherto been particularly noticed, there is a
well-marked correspondence between Hyalostelia fasciculus and the
recent Hyalonema mirabile. 'This is the occurrence, on the surface
of some of the rods, of minute annular or spiral projecting ridges
or frills, which look like so many wrinkled lines crossing the rods.
The frilled rods are irregularly interspersed in the same bundle with

1 Brit. Pal. Foss. p. 10, pl. i. B. fig. 13.

2 Bih. till K. Svenska Vet. Akad. Handl. Bd. 8, No. 9, 1883, p. 13,
3 Lethea Palzozoica, 1880, p. 318.

340 Prof. P. Martin Duncan—A New Oolitic Coral.

others having smooth, even surfaces, in some cases most of the rods
are provided with frills, whilst in others there is only about one in
ten or.twenty with them. In the recent Hyalonema mirabile some
of the spicular rods are also provided with projecting spiral fringes
of a similar character to those in the fossil form, but when perfect
the frills are armed with minute spines.

At present, definite hexactinellid spicules have not been found in
the same strata with H. fasciculus, but this negative fact can hardly
be employed as an argument against the sponge-character of the
spicular bundles. As these latter were, in the life-time of the sponge
itself, imbedded in the muddy bottom of the ocean, they were not
liable to be disturbed and dispersed after the death of the animal, in
the same manner as those of the body of the sponge, and this same
fact will also account for the preservation of the ropes or bundles of
spicules with their constituent spicular rods in their natural positions.

The specimen discovered by Dr. Hicks in the Tremadoc rocks of
Wales thus establishes the presence of siliceous hexactinellid sponges
with anchoring appendages of bundles of spicular rods, at this
horizon, and the same species also occurs at Trefil and at Pont Ladies
in the Llandeilo rocks.

Allied species of Hyalostelia are recorded by Nicholson’ and
Etheridge from Ordovician strata in the Girvan area; by Prof. Ferd.
Roemer? from Lyckholm strata (= Bala) in Esthland, and in the drift
of Sadewitz;* and they are very abundant in Lower Carboniferous
beds in Scotland, Ireland, and Yorkshire. i

The genus Hyalostelia, in which the Pyritonema fasciculus, M‘Coy,
is now placed, was proposed by Zittel* to include sponges, with an
upper portion of regular hexactinellid spicules and an anchoring
appendage of elongated spicular rods.

In conclusion mention may be made that Dr. Hicks has presented
his original specimen to the British Natural History Museum.

II.—On a New Sprrcres or Axosmizia (A. ELONGATA) FROM THE
Pra Gait or THE INFERIOR OoLitE or ENGLAND.
By Professor P. Marin Duncan, M.B. (Lond.), F.R.S., ete.

wet years since, Mr., now Prof., Ralph Tate gave me a small

slender coral, which he had obtained from the Pea Grit of the
West of England. I had just completed the Supplement to the
British Fossil Corals, Pal. Soc., so the fossil has remained undescribed.

It has lately been determined to publish a new edition of the late
Prof. J. Morris’s Catalogue of British Fossils, and therefore, in order
to render the Madreporarian part of that work as complete as is
possible, I have studied and now describe the species.

The specimen is well preserved, except in the calice, but the
deficiency is compensated by an excellent section close below.

The narrow peduncle of the form has been broken from its attach-
ment, and there are no structures which denote that the form was
1 Mon. Sil. Fos. Girvan, fase. ii. p. 289, pl. xix. figs. 1-10.

2 Letheea paleeozoica, 1880, p. 318.

3 Foss. Fauna von Sadewitz, p. 55, pl. vii. figs. 7a, 75.
4 Handbuch der Pal. vol. i. p, 185.

Prof. P. Martin Duncan—A New Oolitic Coral. 341

otherwise than a simple, tall individual, attached, like many simple
corals, to a foreign body. The epitheca is strong, and, as is usual in
the genus, is remarkably ringed with bourrelets d’accroissement, or
growth-rings, so that the surface is tumid and constricted consecu-
tively about thirteen times in the height of 37 mm. No abrasion of
the epitheca has occurred, and there are therefore no septa to be seen
on the flanks of the coral from wearing in. The inside of the coral
is filled with a brown homogeneous calcite, and the septa and
columella are white in colour. The condition of preservation is
very fair, but it appears that some destructive action proceeded,
for a septum of the fourth order is missing here and there, a fifth
being present.

Axosmilia elongata, sp. nov., Pea Grit, West of England. 1. Transverse section
(enlarged five times). 2. Interior (natural size).

Azosmilia elongata, sp. nov.—Corallum simple, tall, straight,
cylindrical, with a small peduncular attachment which leads upwards
to a conico-cylindrical stem, terminating in a cylindrical top; diameter
one-fifth of the height.

Epitheca strong, marked with narrow rings and alternate swellings
and constrictions. Wall merging into the epitheca, epithecate wall
thin. Calicular section nearly circular in outline.

Septa well developed, eight long and stout reaching the small,
essential, styloid, slightly compressed columella. Six of these are
primaries and two are secondaries, the other secondaries being
smaller. Tertiary septa long, slender, and often having a paliform
knob at the inner end, not always straight. The higher orders are
small and somewhat irregularly developed (unless absorption of some
others has taken place). The bases of the septa at the thin wall are
large, and the laminz become slender towards the columella. Pro-
bably the correct cyclical arrangement is four systems with four
cycles, and two systems with three cycles and part of a fourth, but
the following can be seen.

Two systems with three cycles of septa and one septum of the
fourth order in each. Two systems with four cycles complete, the
fourth and fifth orders of the fourth cycle being placed as is usual in
other Madreporaria. A system with three cycles and two members
of a fourth cycle, but in one half-system there is a septum of the
fourth order, and in the other half-system there is no septum of the

9

342 J. Starkie Gardner—Mesozoic Angiosperms. —

fourth, but there is one of the fifth order; this being anomalous, it is
probable that the fourth order of the half-system has been lost.

A system with three cycles complete and the fourth cycle repre-
sented by septa of the fourth and fifth orders in one half and by a
septum of the fourth order only in the other half-system.

Endotheca scanty. Coste absent. Height 87mm. Breadth of
section 6 mm.

The distinctness of the species from Awosmilia Wrighti, Hd. & H.,
is evident ; but the incomplete cyclical arrangement of the septa allies
the species to A. extinctorium, Mich., sp. The tertiary septa of this
last species are said by Hd. & Haime to unite with the secondaries
close to the columella; this does not occur in the new form, which
moreover has little knobs resembling paliform lobes at the inner
ends of some septa as seen in the section.

The question arises almost of necessity, Was this coral a solitary
or simple form? The straight shape, the absence of lateral adhesion
markings, and the deficiency of any gemmation, indicate the simple
nature ; moreover, there are no signs of continuity between the base
of the specimen and a parent stem. Nevertheless, it must be re-
membered that certain fasciculate corals might present pieces of a
shape similar to the new form; but no one has been found with the
special characters of the calicinal section described above. It appears
that Milne Edwards and Jules Haime were correct in placing
Axosmilia amongst simple corals; but the present species is more
elongate and less expanded superiorly than their type. The new
form differs from all others, and from all parts of forms which have
been described from the Lower Oolite series.

The specimen is now in the British Museum.

IIJ.—Mrsozo1c ANGIOSPERMS.
By J. 8. Garpyer, F.G.S.
(PLATE IX.)

ieee the article on Mesozoic Angiosperms was written,! a very
important Sketch History of “Paleobotany,” by Lester F.
Ward, has appeared in the Fifth Annual Report of the U.S. Geol.
Survey, a brief outline of which cannot fail to prove of interest in
connexion with this subject. The object of the sketch is to collate
and reduce the fragmentary and desultory mass of information col-
lected by previous writers into a system that will enable geologists
to use the testimony of fossil plants, in the same way that they
habitually use that of fossil animals. The author laments that:
botanists and palzobotanists have worked and classified almost
wholly independently of each other, the former having consequently
missed such important data for classification as the order in time in
which each type appeared, while the latter have failed to harmonize
their work with the more elaborate and best botanical systems, and
hence greatly lessened its practical value. “Every candid paleo-
botanist must admit that he can understand fossil plants only as
they resemble living ones, and that the botanist, studying the per-

1 See Grou. Maa., May, 1886, pp. 193-204.

GEOL. Mac. 1886. DECADE III. Vout. II. Pu. IX.

|

| |
Fre. 1. Palmwood from the Gault, Folkestone.
Fie. 2. Palmwood from Antigua, W. Indies.

a. transverse section. 6. longitudinal section.

a
l
: ue

|
i

————

iF

| ]
| | y

i= VE
2 YZ

ai A,
TR LZ
FLL iL |
lt

i)

SS

<>

——$=<<$——

—<$<$<—
SSS

=|_=—
—

Wit Mit
i 7 mM ! ne
Wy Pyrat

—S

LL

S—_=

—
S

——=—=—=>
———

SS

faxaeses

i Md Il 1)

z Ml) I \
pean HMO ea Ah y N
Tio TALE ee
; ee a

SSS

———~
—

Ws
4,
WGN

Wy

BE

SE SY aj

SS —
TS——
SSS

Fic. 3, Stem of the so-called Calamites Beanii, Bunbury,! trom the
Inferior Oolite near Scarborough, ‘‘ one of the Arborescent Graminex ’’
(Williamson).

1 This is the figure referred to on p. 202, Gron. Mac. May, 1886, as having been lost.—Enrv.

i, oat

Seabee
4 ne ht

iCoabtekathss

i is

oe hn

J. Starkie Gardner—Mesozoic Angiosperms. 343

fect specimen with all its organs of reproduction as well as of
nutrition, can alone declare with absolute certainty upon its identity
or affinity.” This mutual dependence requires recognition at the
hands of scientific men.

The interesting collection of biographies of eminent paleobotanists
is a feature of the work which can be but briefly alluded to here.
The names that stand out prominently, and to whom half the litera-
ture is credited, are Brongniart, Goppert, Unger, Lesquereux, Heer,
Massalongo, Ettingshausen and Saporta; but the biographies are 22 in
number, and include the names of our countrymen Witham, Binney,
Bunbury, and our eminent and yet living contemporaries Williamson,
Dawscn, and Carruthers. Of Prof. Williamson, he says: “Of the
merits of this work, as of all this author’s investigations, it is
certainly unnecessary to speak here.” Of Dawson: “A geologist
rather than a botanist, he has done excellent service, not only in
elucidating the important problems of Acadian geology, but also in
demonstrating the value and legitimacy of the evidence furnished by
vegetable remains.” The value of Carruthers’ work also receives
due acknowledgment, his investigations with regard to fossil fruits
having especially “ widely expanded this field of knowledge.” That
Mr. Ward has gracefully acknowledged our indebtedness to these
authors no one will dispute, but some may think the praise in other
cases has been a little indiscriminate, and that a more critical ex-
amination into the quality, as well as the bulk of the work produced,
would have rendered greater service to botanists who may require
to have recourse to it.

It appears that Walch (1769) was the first to offer anything like
a nomenclature of fossil plants, though a few terms such as Litho-
cylon had for some time previously been in use. Calamites is the
only one of his names, except Carpolithes, that has survived, and
this was applied under the misconception that the plants in question
were large reeds. Steinhauer (1818) was the first to apply specific
names to fossil plants. Schlotheim soon afterwards’ introduced,
among others, two terms which specially interest us, Palmacites
and Poacites, describing respectively 15 and 4 species. Sternberg’
established the genus Flabellaria (I am purposely omitting all re-
ference to Cryptogamic and Gymnospermous genera, in order to con-
centrate attention on the successive steps by which our knowledge
of fossil Angiosperms has been arrived at), and assumed three periods
of vegetation, that of Coal-plants, that in which Cycadean types pre-
dominated, and that of fucoids and dicotyledons, corresponding of
course with the three ages of geology. The system of Martius, which
should be interesting, is unfortunately passed over, and we are
brought down to Brongniart’s first memoir,’ in which the only
genera that interest us are Hxogenites and Endogenites, to include
stems whose internal organization is recognizable. Many Angio-
spermous fruits, leaves and stems had been figured, and more or less
described, before this time, for example by Parkinson and Mantell,
but none scientifically. In 1828 Brongniart’s “ Prodrome ” ap-

1 Petrafactenkunde, 1820. 2 Flora der Vorwelt.
3 Mém. du Musée d’hist. Nat., Paris, 1822, vol. viii. pp. 209-210.

344 J. Starkie Gardner—WMesozoie Angiosperms.

peared, in which he discards his previous artificial classification, and
adopts a botanical one. The Gymnospermous were separated from
the Angiospermous Phanerogams, the former being considered inter-
mediate between the Cryptogams and true Phanerogams, a proposi-
tion which, though placed every year on a firmer basis, is not yet
adequately recognized by botanists. Brongniart’s system was ac-
cepted by almost all writers on the subject, with the notable excep-
tion of Lindley and Hutton, who included Cycads and Conifers
among Exogens or Dicotyledons, a method still followed, unfor-
tunately for paleontologists, by some of the ablest botanists of the
day. ‘They further included Stigmaria, Annularia and Asterophyllites
among true JDicotyledons, Noeggerathia is placed among the
Palms, and Calamites is attached to Juncus. ‘One of the most
remarkable aberrations of the book,’”? Mr. Ward remarks, “is the
pertinacity with which the authors contend for the existence of
Cactaceous and Euphorbiaceous plants in the Coal-measures.” They
in fact utterly ignored the principles laid down by Brongniart
and previous writers, and entirely dissented from the theory of
progressive development. Cotta’s important treatise on fossil wood
was followed a year later, in 1833, by Witham’s work on the same
subject, and by Zenker’s! description of Cretaceous plants from
Blankenburg in the Harz district, the first attempt to treat dicoty-
ledonous fossils systematically. In 1840, Rossmissler proposed ? to
modify Sternberg’s method of classifying all fossil dicotyledonous
leaves as Phyllites, substituting a compound from it and the genus to
which the leaves seemed to belong, as Daphnophyllites, etc. Thence-
forward the plan of naming and describing fossil as if they were
real plants, became definitely adopted. The terms Carpolithes,
Phyllites, ete., are still employed where there is absolutely no means
of assigning a fossil to any definite group in the vegetable kingdom,
but the tendency is far greater towards unwarrantably assimilating
leaves with living genera which they resemble, than the employ-
ment of any termination, such as ‘‘ites,” e.g. Pinites, to suggest that
the resemblance may be only apparent.

Passing on to the question of classification, the result of palzeo-
botanical research so far has been to necessitate certain modifications
in order to bring the botanical system into accord with the succes-
sive appearance of classes of plants in time. The grouping that best
meets this requirement is according to Mr. Ward:

Cryptogams
{ Gymnosperms Cycadaceze
Coniferz
Gnetacez
Phenogams < Monocotyledons
| Angiosperms Apetalee
Dicotyledons Polypetalze
L Gamopetale

The chief modification introduced is the elevation of the Gym-
nosperms to the rank of a class, while the Monocotyledons and
1 Beitrage zur Naturgeschichte der Urwelt, Jena, 1833.

® Beitrage zur Versteinerungskunde, vol. i. die V. des Braunkohl. aus der Gegend
von Altsattel in Bohmen.

J. Starkie Gardner—Mesozoie Angiosperms. 345

Dicotyledons are reduced to sub-classes. This is done because the
distinction between open and closed ovaries is regarded as a class
distinction, and Gymnosperms are not dicotyledonous, but have a
variable number of cotyledons ranging from 1 to 15. The conclusion
that Gymnosperms form a natural transition from Cryptogams to the
higher flowering plants has been arrived at by Sachs and others
quite independently of the evidence of fossils.

Valuable statistics have been collected as to the actual numbers
of species described, and we find, so far as Angiosperms are con-
cerned, the result to be as follows: For the Carboniferous 8 or
0-5 °/,, Permian 3 or 0-9°/,, in the Bunter 4 or 18-2°/,, Keuper 1 or
2-4°/,. For the Jurassic we have 1 or 0.8°/, in the Rheetic, 5 or
37 °/, in the Lias, 9 or 2:1 °/, in the Oolite, and inexplicably enough
only 1 or 0-8°/, in the Wealden. The absence of flowering plants
in this formation is one of the mysteries of the Geological Record
which Mr. Ward does not elucidate. Vast delta deposits, such as
these, composed of most varied kinds of sediments, spread over
many and wide areas, in places teeming with plant and other remains
of terrestrial life, would appear in every way fitted to have preserved
fair representative examples of the vegetation of the period; yet,
though monocotyledonous flowering plants must have been far from
uncommon then, only a solitary one has been met with. To the close
of the Jurassics only monocotyledonous Angiosperms are found,
but with the Cretaceous Dicotyledons join them, and the per-
centage gradually increases until in the Laramie it reaches 37:5 °/,,
a figure only surpassed in the so-called Paleocene. The Eocene
would appear the age of Monocotyledons, judged by the 16:8 °/,,
though the Miocene possesses no less than 272 species. Mr. Ward’s
tables have a statistical value, and enable us to see how far we
are advanced ; but it is needless to say that even the revision of
Mesozoic Angiosperms in the preceding pages of this Macazine has
profoundly modified the per-centages of the group in the Jurassic.
The supposed Carboniferous and Permian Monocotyledons rest on
wholly unsatisfactory material, and Angiosperms cannot at present
be traced with any approach to certainty farther back than the
Mesozoic period. The value of such a table is again lessened by
the possibilities of error in correlating the formations of the two
hemispheres. If, for instance, we took the Lower Cretaceous of
Europe, we should have a complete absence of Dicotyledons; but if
we take the supposed equivalent of the Gault in America, we have
“many of our most familiar forms, the poplar, the birch, the beech,
the sycamore, and the oak;” “the fig tree, the true laurel, the sasa-
fras, the persimmon, the maple, the walnut, the magnolia, and even
the apple and the plum.” ‘That the American correlations of the
Cretaceous and Eocene deposits of the Western hemisphere with
ours, are faulty, becomes more and more apparent, and that many of
the Dakotah plants actually belong to the genera quoted is still
more open to question. Destructive criticism will, for a long time to
come, do more to advance this study than any additions to species,
and it is sincerely to be hoped that Mr. Ward or some other com-
petent palzobotanist will devote himeelf to this side of the problem.

346 J.J. Harris Teail—Hornblende-Bearing Rocks.

IV.—Nores on Some Horneirnpr-Brarinag Rocks FRoM
INCHNADAMPF.

By J. J. H. Teaur, M.A., F.G.S.

N the present communication I propose to describe the petro-
graphical characters of some hornblende-bearing rocks which
occur as intrusive sheets and bosses in the limestones and quartzites
of the Assynt district. These rocks have been referred to under
various names by the different writers on the geology of the district.
Prof. Nicol speaks of them as greenstone! and trap,’ and Sir R.
Murchison, as syenitic greenstone. Mr. Hudleston*‘ indicates their
character more definitely by speaking of them as a “kind of diorite.”
Prof. Bonney, in an appendix to Dr. Callaway’s paper “‘On the
Newer Gneissic Rocks of the Northern Highlands,” describes the
microscopic structure of a specimen from the Traligill Burn near
Inchnadampf, and designates the rock a hornblendic porphyrite. Dr.
Heddle ° gives some valuable information as to the distribution of
the rocks, and calls attention to the perfection of form exhibited by
the hornblende in certain varieties. He gives a figure of the horn-
blende which shows the forms (110), (010) and (011). With regard
to the relations of the rocks to the associated strata he speaks some-
what doubtfully, but evidently inclines to the view that they are
intrusive. That this is the case seems proved by the absence of
vesicular structure and associated tuffs, and by the fact that although
they keep as a rule parallel with the bedding, cases occasionally
occur in which they can be seen to move from one horizon to another.
Mr. Hudleston has remarked on the fact that the igneous sheets
_ have been involved in the earth-movements which have folded and
faulted the stratified rocks, so that the date of intrusion must lie
between the formation of the limestones and the production of the
earth-movements which have produced such striking effects in this
district.

The specimens on which the following observations are based were
mainly collected by myself during the years 1883 and 1884. I am,
however, indebted to Prof. Judd for the loan of some which he
collected. Those collected by myself were partly obtained from the
limestone and partly from the quartzite. Those from the limestone
came from the bed which is so well exposed in the Stronchrubie
escarpment about three-quarters of a mile south of Inchnadampf,
and from the low ground to the north of Inchnadampf, where the
rock is exposed in many places. Those from the quartzite came from
two localities; one at a point where the 500-feet contour-line crosses
the southernmost of two small burns which run into the Calda Burn
(Alt 4 Chalda Mor) near the most southerly portion of its course,
and the other near the base of Beinn an Fhurain, rather more than a
mile H.S.E. of Inchnadampf. Prof. Judd’s specimens came from the
neighbourhood of Inchnadampf, and from a point on the Allt nan

1 Q.J.G.S. 1856, p. 25. 2 Ibid. 1860, p. 97. 3 Tbhid. 1859, p. 220.
4 Guou, Maa. 1882, p. 392. 5 Mineralogical Magazine, 1888, p. 188.

=

J. J. Harris Teall—Hornblende-Bearing Rocks. 347

Uamh, south of Stronchrubie, at a height of about 700 feet above
the sea.

CHARACTERS OF THE Rock-Forminc MINERALS.

Hornblende.—As this is the mineral which especially characterizes
the rocks in question, it will be well to describe it in the first place.
It must be remembered, however, that this does not imply that horn-
blende is always the most abundant mineral. In almost all cases it
occurs in well-formed crystals. The larger ones are found in the
rock associated with the quartzite. They form short stout prisms,
which, however, so far as my observations go, are not terminated by
clinodomes (011) as in Dr. Heddle’s figure, but by the positive hemi-

pyramid (111) and the basal plane (001). The forms in the prismatic
zone are (110) and (010). The smaller crystals occur usually in
elongated prisms, and can only be studied in a satisfactory manner by
the use of the microscope. Cross-sections sometimes show the
ortho- (100) as well as the clino-pinacoid (010).

The larger crystals may sometimes be completely detached from
the rock-mass, and are of such a size that their angles may be measured
with a contact goniometer. In all cases the hornblende is green
when examined in thin sections. The pleochroism is fairly strong ;
a =pale-green or yellowish-green, 8 and y = deep-green, with
only slight differences. One of the most interesting features is the
presence, in certain varieties of the rock, of a marked zonal banding,
due to a variation in depth of tint in the successive zones. In some
crystals a very large number of zones may be detected; in others
only two, and in others the crystal appears homogeneous, All these
variations may be seen in one and the same rock-section; a fact
which seems to show that the crystals have not been simultaneously
developed. The zones are in all cases parallel with the external
boundaries of the hornblende, except where an original crystal has
been obviously fractured and a fragment only is present.

Twinning is frequently present, and the most common type is that
in which the orthopinacoid (100) is both twin-plane and face of
composition. Sometimes repeated twinning on this plan occurs, so
that a crystal is made up of three or four lamelle.

The alteration of the hornblende is accompanied by the formation
of chlorite, epidote, and opacite. In some of the more altered rocks
the hornblende is entirely represented by a green chloritic aggregate,
in which specks of opacite are abundantly scattered. In these cases
the form of the original hornblende is perfectly preserved. In other
cases granular epidote is associated with chlorite, and in others
epidote occurs to the exclusion of chlorite. In the last-mentioned
cases the original form is often lost.

Felspar.—In some of the rocks two generations of felspar may be
recognized. The larger porphyritic felspars possess sharply-defined
crystalline outline. They occur in moderately thick tables, with con-
spicuous development of the clinopinacoid (010), and often show a
most beautiful zonal banding due to variation in the optical characters

348 J. J. Harris Teall—Hornblende-Bearing Rocks.

of successive layers. Twinning according to the albite, pericline
and probably also the Carlsbad laws occurs ; but it is not very con-
stant or uniform. These felspars also evidently possessed inclusions
arranged in a more or less zonal manner ; but the original nature of
these inclusions is difficult to make out in consequence of alteration.
It is a noticeable fact that the angles of the inner zones are mostly
rounded, although the external faces of the crystals meet in perfectly
sharp angles. In some specimens in which the felspars of the first
consolidation have been so altered as to have lost to a very great
extent their definite optical characters, irregular scales of a vividly
polarizing mineral are seen to be scattered through the crystals.
These scales often have their long axes arranged in a zonal manner,
evidently corresponding with the original structure of the crystal.
When examined with a high power, they are seen to possess one
strongly-marked cleavage, and to extinguish parallel with this cleavage,
so that they may be referred with confidence to a white mica, pro-
bably paragonite. The felspars of the ground-mass form together
with quartz a microcrystalline aggregate.

In a large number of rocks only one generation of felspars can be
detected. When this is the case, the individuals occur as irregular
grains, sometimes of considerable size. Mutual interference appears
to have prevented the development of definite form. Twinning on
the albite plan is sometimes present and sometimes absent. In all
cases the felspar-aggregate plays the réle of ground-mass, and horn-
blende crystals lie in it, without any regard to the orientation of the
individual grains. The coarseness of this aggregate varies between
wide limits, sometimes it is so fine as to merit the term microcrystal-
line, at other times it is so coarse as to remind one of the structure
of a medium-grained granite. In some of the thin intrusive sheets
the felspars tend to assume the form of small columnar crystals,
which give narrow lath-shaped sections, but even in these cases the
outlines are not well defined.

Pyroxene.—This mineral is not constantly present. It is pale green
when examined on a fractured surface of the rock, but perfectly
colourless in thin section. It occurs in somewhat imperfect crystals
and also as grains and granular aggregates. The forms of the
crystals appear to be those characteristic of the common rock-form-
ing augites. The maximum extinction in the prismatic zone is about
40°. The only cleavages recognized are those of the prism. The
mineral has been especially noticed in the rocks which are intrusive
in the dolomitic limestone; but it varies very much in quantity even
in these, sometimes being absent altogether, and at other times occur-
ring more abundantly than the hornblende. In some of the coarse-
grained rocks in which the hornblende attains a considerable size it
occurs as inclusions in this mineral. Asa good deal has been said
about the secondary origin of the rock-forming hornblende, it may
be as well to state that no doubt whatever can exist as to the dis-
tinctness of the hornblende and the augite in these rocks. Fractured
erystals of beautifully-zoned hornblende occur in the porphyritic
varieties, and this must be regarded as absolutely conclusive in favour

J. J. Harris Teali—Hornblende-Bearing Rocks. 349

of the view that this mineral was a product of the consolidation of
the original magma.

Apatite-—This mineral occurs in the form of limpid hexagonal
crystals, which are usually four or five times longer than broad.

Magnetite.—A small amount of original magnetite occurs in grains
and crystals. The opacite (secondary magnetite?) which occurs
associated with the chlorite has already been referred to.

Calcite occurs in the form of fine dust thickly scattered through
some of the more altered specimens, and also as large crystalline
plates in sections which contain the colourless pyroxene. It is pos-
sible that the portions of crystalline calcite may be fragments of the
limestone caught up by the igneous magma at the time of its intrusion.

Epidote has already been referred to in describing the alteration of
the hornblende. It is difficult to say whether all the epidote has
been formed in this way.

Quariz is present as a secondary and probably also as a primary
constituent in some varieties of the rock.

Mica arises in connection with the alteration of felspar, and it is
sometimes found associated with ill-defined aggregates of epidote.

DESCRIPTION OF THE ROCKS.

Macroscopic examination shows that the above minerals occur in
very different proportions in the different varieties of the rock. In
some the hornblende is very abundant, and these asa rule have a
granular aspect; in others it is comparatively scarce. The latter
usually contain two generations of felspar and have a marked por-
phyritic aspect. For the purpose of description we will term them
hornblende porphyrites, and the former diorites. It must be remem-
bered, however, that the diorites tend to become porphyritic by the
conspicuous development of hornblende; such varieties will be termed
porphyritic diorites. The diorites also present us with varieties of
texture depending on the coarseness of the grain. In some the con-
stituent minerals may be easily recognized, in others they are so
small as to require the microscope for their determination. The
latter occur in the thin sheets and at the margins of the intrusive
masses.

In the porphyritic diorite near the base of Beinn an Fhurain con-
cretionary patches occur which are more coarsely crystalline and
richer in hornblende than the main mass of the rock. In these
patches as in the main mass an ageregate of felspar individuals plays
the rdle of grourid-mass. As a rule the outlines of the inclusions are
smooth and curvilinear, but sometimes the large hornblende crystals
project for a short distance into the main mass of the rock. It is
clear that we have here phenomena similar to those described by Mr.
Phillips’ in the case of the granites. The inclusions in the rock
now under consideration agree with those described by Mr. Phillips,
(1) in form; (2) in being more basic in composition than the main

‘«*On Coneretionary Patches and Fragments of other Rocks contained in

Granite,’ Q.J.G.S. vol. xxxvi. p. 1; and ‘‘ Additional Note on Certain Inclusions
in Granite,’ Q.J.G.S. vol. xxxviii, p. 216,

300 J. J. Harris Teall—Hornblende-Bearing Rocks.

mass of the rock; and (8) in the fact that large crystals sometimes
project from the inclusion into the ground-mass.

The following analyses will give some idea of the variation in the
chemical composition of these rocks.

L Il. TI

sigulw (1.04 Csi eee Bool! au 52-47
‘AlsOs0h DUE 16:90 Wl) ust 160201). al! 12°15
RG, Osu h nesses 2 6ittly aih. Ac. gla 3°47
OM uae BROAN acon BiG, ashe 5-23
(Hake paar AO) ol TDW le one 9°71
Meo Macey: I ose FO ae 9-94
NasOrnny hick. BT a. MOG ces 2-81
BQ on O98 Pen. Baan Le 9-96
pay Rae TaA@! ie 1-62
Com aa } 64 Ig. ...... { BO" Vanier “54
100-54 100-39 100-20

I. Hornblende-porphyrite, intrusive in quartzite, base of Beinn an Fhurain.
II. Porphyritic-diorite, base of Beinn an Fhurain.
III. Plagioclase-pyroxene- hornblende rock, near Inchnadampf, intrusive in limestone.

Titanic acid, phosphoric acid, and manganese are present in the
above rocks, but have not been determined. ‘They have therefore
been weighed with SiOz, Al,O;, and Fe,O;. Specimen I. contains
two generations of felspar, and is a typical. porphyritic rock.
Specimen II. contains only one generation of felspars. The horn-
blende is more abundant than in I., and sometimes occurs in good-
sized porphyritic crystals. Specimen III. differs from the others in
containing a large amount of colourless pyroxene.

It is seen to be richer in lime and magnesia, but not richer in iron.
In all probability the pyroxene is a nearly pure lime-magnesia
bisilicate, and one is tempted therefore to ask whether it may not be
due to the absorption by the igneous magma of a certain amount of
the dolomitic limestone into which the rock has been intruded. ‘The
sporadic manner in which the pyroxene occurs is in favour of the
view here suggested. As telling somewhat against this view we have
to mention the frequent occurrence of a colourless pyroxene in the
more basic plagioclase-hornblende rocks, as, for example, in some of
Prof. Bonney’s hornblende-picrites! and the allied rocks of War-
wickshire described by Mr. Allport as diorites.*

One very interesting feature which a comparison of the different
varieties of diorite brings out is the variation in the state of crystal-
lization in the ground-mass. In the compact rocks the individual
felspars are minute, and give more or less lath-shaped sections. It
is impossible to determine the precise character of the original
ground-mass in consequence of alteration, but it evidently approxi-
mated to that of the hornblende andesites. In the medium-grained
rocks the microstructure of the ground-mass is thoroughly granitic.
Here then we see a gradation exactly similar to that described by

1 On the so-called Diorite of Little Knott, with further remarks on the occurrence
of Picrites in Wales, Q. J. G. S. vol. xli. p. 511.
2 On the Diorite of the Warwickshire Coal-field, Q. J. G. S. vol. xxxv. p, 637.

J. J. Harris Teall—Hornblende-Bearing Rocks. ool

Messrs. Hague and Iddings! as occurring in the diorites and horn-
blende-andesites of the Washoe district.

A specimen of a fine-grained rock collected by Prof. Judd shows
a curious spotted or variolitic structure. The rock is much altered,
and it is therefore impossible to ascertain its original character. The
spots and the main mass of the rock both contain needle-shaped
pseudomorphs after hornblende and a microcrystalline ground-mass.
The hornblende-needles are not arranged in any definite manner in
relation to the spots; sometimes a needle may be observed with one
end in a spot, and the other in the ground-mass of the rock. The
external boundaries of the spots are not defined by a sharp line, and
where two or more spots coalesce, there is no line of separation
between them. Where the spots are best defined, they consist of a
central more or less spherical portion, which is rendered nearly opaque
by opacite dust, and a marginal portion in which the ground-mass is
nearly colourless. The structure appears to be analogous to that of
the variolitic diabases.

CoMPARISON OF THE Rocks witH ALLIED Rocks OF OTHER
DISTRICTS.

The plagioclase-hornblende rocks form a very difficult and some-
what unsatisfactory group. In some, as, for example, the epidiorites
of Giimbel, the hornblende is undoubtedly secondary ; in others, in-
cluding the rocks now under consideration, it is certainly original.
As the question of the origin of the hornblende is one of the greatest
interest in relation to the past history of the rocks themselves
and of those portions of the earth’s crust of which they form a
part, it becomes of importance to separate those in which horn-
blende is secondary from those in which it is a product of the
consolidation of an igneous magma. Mr. Allport? has shown
that in certain plagioclase-hornblende rocks surrounding the Land’s
End mass of granite, the hornblende is wholly secondary after
augite. Such rocks have therefore no affinities with those now
under consideration. The same observer has, however, described
certain plagioclase-hornblende rocks (diorites) from Warwickshire,?
-in which the hornblende is mainly original. These rocks have
certain points of resemblance with those above referred to. The War-
wickshire rocks are, as arule, much altered; but Mr. Allport was
fortunate enough to obtain one specimen from Marston Jabet which
was absolutely fresh. It was mainly composed of long prisms of
well-formed hornblende set in a crystalline aggregate of plagioclase.
This rock, therefore, is closely allied to some of those described in
this paper. Another point of resemblance between the Warwick-
shire rocks and those from Assynt is the occurrence in both of a
colourless, or nearly colourless, pyroxene, in association with horn-

1 On the Development of Crystallization in the Igneous Rocks of Washoe, Nevada,
Bull. U. S. Geol Survey, No, 17, 1885.

2 On the Metamorphic Rocks surrounding the Land’s End Mass of Granite,
Q. J. G. 8. vol. xxxii. p. 407.

3 Q. J. G. S. vol. xxxv. p. 637.

302 J. J. Harris Teali—Hornblende-Bearing Rocks.

blende. There are, however, some important points of difference.
The original hornblende of the Warwickshire rocks is brown, and
where it occurs abundantly is in the form of large ophitic plates con-
taining inclusions of lath-shaped felspar. In the Assynt rocks the
hornblende is green, and appears in all cases to have preceded the
felspar in the order of consolidation. Again, some of the Warwick-
shire rocks contain numerous pseudomorphs after olivine, whereas
no trace of this mineral has been detected in any of those from
Assynt. The ophitic character of the hornblende and the presence
of olivine both point to the conclusion that some of the Warwick-
shire rocks are more basic in composition than any yet found in
Assynt. Many of the Anglesea “ diorites”’ bear the closest relation
to the corresponding rocks from Warwickshire. They consist of
brown hornblende often passing into green, a colourless pyroxene,
plagioclase and magnetite or ilmenite. By the coming-in of olivine
and the dying-out “of the felspar, these rocks shade into Professor
Bonney’s hornblende-picrite. Mr. Tawney! has described similar
rocks from the Lleyn peninsula, Caernarvonshire, under the name of
hornblende-diabase. An interesting little boss of “diorite” occurs
on the right-hand side of the footpath leading from Mount Sorrel to
Swithland (Leicestershire), and just outside Brazil Wood.

This boss projects through the soil, and measures only a few yards
across. It varies considerably in texture, some parts being com-
posed of a medium-grained granular rock, and others containing
large hornblende crystals or plates. Prof. Bonney has described
the rock of this knoll as follows: ‘ Under the microscope the latter
mineral [hornblende] is seen to occur in irregular grains, plate-like
in section, pierced and intersected by the plagioclase [ophitic] with
a little iron peroxide (? some of it ilmenite). The hornblende with
transmitted light is both brown and green in colour, and much of it
and of the felspar is still in good condition. Here and there patches
of the pale fibrous actinolitic variety occur, associated with a mineral
rather like a fibrous variety of serpentine. These last are certainly
secondary products, and much resemble a variety common in the
altered Cornish gabbros. Most of the larger hornblende is strongly
dichroic. Some of the brown variety resembles biotite. One or
two pieces indeed appear from their optical properties to be that
mineral. There is a little calcite with characteristic cleavage. The
plagioclase often shows brilliant colours and characteristic twinning,
with occasional indications of a zonal structure.”

My slide of rock from the same locality agrees with Prof. Bonney’s
description, but contains, in addition to the minerals which he has
mentioned, a colourless pyroxene. This brings the rock into the
closest relation with some of Mr. Allport’s diorites from Warwick-
shire, with the Anglesea “diorites,” and with Mr. Tawney’s horn-

lendic-diabases from the Lleyn peninsula. I would suggest that, for
convenience of description, we should use a special locality as a

1 Woodwardian Laboratory Notes, Gzoz, Mac. Decade II. Vol. VII. pp. 212 and
457; also Vol, IX. p. 548.

Rev. A. Irving—The Brookwood Well-Section. 3038

means of designating rocks of this kind, and as this appears to be the
only variety of diorite which is found in the boss at Brazil Wood,
it might be termed the Brazil Wood type of diorite. If we do this,
we may then state that diorites of the Brazil Wood type occur in
Warwickshire associated with Cambrian strata, and also in Anglesea,
the Lleyn Peninsula, and the Lake District. It is worthy of note
that in no single instance is a diorite of this type known to be
associated with Upper Paleozoic or later strata in Britain. I have
a specimen of diorite from Glen Tilt (Perthshire) of the same general
type, but can say nothing about its mode of occurrence.

The differences between diorites of the Brazil Wood type and
those from Inchnadampf described in the present paper have already
been referred to. The interesting fact of the close relation of these
diorites to Prof. Bonney’s hornblende-picrites has also been pointed
out.

V.—Tuet Brooxwoop Drrp-WELL SEcTIoN.
By the Rev. A. Irvine, B.Sc., B.A., F.G.S.

HIS section, which was completed last year, appears of such value
and interest to students of the Tertiary strata of the London
Basin, that I have thought it worth while to offer a description of it
to the readers of the GronogicaL Macazine. ‘Through the courtesy
of Dr. Barton, the Governor of the Asylum, I have had free access
to the specimens preserved of the various strata passed through, and
very careful use of them has been made in the preparation of the
tabulated statement which follows; much of the information having
been kindly furnished from the engineers who were employed. The
Asylum is situated at Knap Hiil, about a mile and a quarter from
Brookwood Station on the South-Western Railway, and is on the
Upper Bagshot Sands. The mouth of the well is in the valley just
below, about 140 feet above O. D., and about the same ievel as that
at which the Middle Bagshot Beds occur in the famous Goldsworthy
section, which furnished Prof. Prestwich, some forty years ago, with
the clue to the succession of the beds of the Bagshot Formation. It
is about a mile and a half distant therefrom. The evidence as to
the horizon in the Bagshot Series, at which the well commences, is
very clear to those who are familiar with the stratigraphy. The
widely-extended pebble-bed at the base of the Upper Bagshot Sands
occurs here very near the top of the well, and I saw it exposed again
at about the same level in an excavation made by the side of the
high road which runs along the western side of the Asylum Hstate.
The same greenish loamy sand was intermingled with the pebbles in
both cases. In the ploughed field a stiff yellow loam, such as so
commonly occurs above this pebble-bed in the Bagshot area,’ crops
out in the valley where the well is situated. The ‘brown sandy
bed’ which occurs at the top of the section is probably a portion of
this, re-constructed by later drift action, and mingled with more

1 Vide Q.J.G.S. for August, 1885, pp. 493 (No. 2 of the Section).
DECADE III.—VOL. IlI,—NO. VIII, 23

354 Rev. A. Irving—The Brookwood Well-Section.

sandy materials washed down from the sandy strata situated at
higher levels on the slopes of the valley.

In attempting to classify the Bagshot Beds I have used the
grouping adopted in descriptions recently published of other deep-
well sections! in the Bagshot District (those namely at Wellington
College, Farnborough and Mytchett), and for the reasons there given.
A comparison of this section with those brings out a very remark-
able continuity in the general characters of the Middle and Lower
Bagshot Beds, though there is just that amount of variation in details .
which we should be led to expect from the conditions under which
they appear to have been deposited.” I have found it by no means
easy to draw a line between the Lower Bagshot Beds and the London
Clay, for there is no abrupt transition from one to the other, in the
description given below; while a careful study of the actual speci-
mens leaves no alternative that I can see to the recognition of a
gradual passage upwards from the London Clay to the characteristic
Lower Bagshot Sands. The resemblance of what is seen here to
what is seen in the specimens from about the same horizon in the
Wellington College well-section is very close indeed; and is in
striking contrast with the abrupt transition between the two forma-
tions which I have observed in sections already described at Aldershot,
Wokingham, and Bracknell, on the marginal portions of the area.

The following points in connection with this section (see p. 355)
appear to me worthy of note.

1. The apparent gradual passage from the London Clay into the
Lower Bagshot Sands, as contrasted with the abrupt transition
observable in the Walton section recently described by Mr. Hudle-
ston, and in those on the marginal portions of the Bagshot area to
which I have referred above.

2. The remarkable absence of any considerable development of
clays, the entire absence of all record of pebbles, and the general
predominance of quartz sand stained by carbonaceous matter of
vegetable origin are characters which the Lower Bagshot beds of
this section possess in common with the Lower Bagshot strata of
three deep-well sections, of which I have given a fuller account else-
where,‘ and to which I have referred above.

3. The specimens of the slightly loamy sands which occur in this
section between the depths of 68 and 143 feet bear a striking re-
semblance to those which occupy about 92 feet of the Lower Bag-
shots in the section at Wellington College. This resemblance comes
out very strongly when the specimens from the two places are
directly compared.

4, Of the pyrites found in the Bagshot Sands one large heavy
specimen (found at the depth of 180 feet) and many smaller
ones are preserved. They are quite unweathered, and are probably
pyritized wood in situ; but with the cement stones found in the same
beds the case is different. They are very much weathered, their

1Q.J.G.8. loc. cit.

2 Cf. Q.J.G.S. loc, cit.; also Grou. Mac. Dec. IIT. Vol. II. p. 25.
5 Q.J.G.S. April, 1886. 4 Q.J.G.8. loc. cit,

4

Heicut asove O. D. Leven apour 140 Feet.

Ree ot een Strata passed through in the Brookwood Deep Well.
3 3 Brown sandy bed.

SG 1 4 Gravel (well-rounded pebbles of flint in greenish sand).
s 54 oe Dens fam ’ ’ Dark grey and black sand
Fa 15 10% | ‘Tron band,” or ‘rust | with traces of pyrites and frag.
Sy es 4 lit Shaly band ments of clay ironstone highly
as = 2+ 133 Dark sand weathered, with sand-grains
iS Ag 3a 17 ‘Marly’ with sandy veins J adhering to the old surfaces.
os 3 8 25 ‘Light marl’ (quite a pure pipe-clay in the specimens).
438 1 26 Brown clay (a very stiff clay slightly laminated).

2 43 302 | ‘Greenish clay.’

19 62 374 | Dark brown sand.

Fre Wray 1808 68 Dark sand with pyrites and cement-stones. erains).
{ 10 78 Hard dark (carbonaceous) loamy sand (with some black

ie 19 97 Lighter grey (carbonaceous) sand (black grains more

S 5 102 Darkish grey sand (loamy). [numerous).

aa 3g 1053 | Grey loose sand (with black grains).

Se 4 109 Light grey sand.

aa 11 120 Grey sand (with black grains).

= 2 234 1433 | Dark grey carbonaceous coherent sand, with pyrites.

+, B 65 150 Hard dark shaly sand and Specimens preserved of a
Ss Bid 1 151 Grey sand. [clay. ) dark grey indurated marl
3s 1 152 Dark ‘clay.’ with a very definite fracture.
a2 at 154% | Nearly black shale with intervening layers of grey sand,
Sa inclosing numerous green and black grains.

25 95 164 Thinly-laminated sandy shale (light grey) with minute
sep black grains and spangles of mica on planes of lamine.
2 54 169% | Fine clay and sand The specimens are similar to
o 2 171} | Clay those of the bed next above, but

2 1733 | Light grey sand rather more sandy.
Brea (692 343 London clay.

a = 3434 | ‘ Bed of stone.’

a 185 ope Hontlon clays c Se Paes pete
a 2 264 ce 22 with pyrites, fare for the most part. 3
= 1% 3745 9 ” The only specimens
= oy 37d ‘Bed of stone.’ preserved are what ap-
Be 25 400 London clay. pear to be typical of the
35 1 4002 nah] Oe ae clay and the stone-beds

2 2 respectively. The former
ban 38 438% | London clay. is a mass of bluish-grey
oss 82 447 op », with pebbles. pasa e o1ay many
ac 2 450 ” ” Ns definite rantane Poth
= 10 460 ” ” (thin sand layers). latter, ‘‘found in the L.
iS) 19 479 ah », with pebbles. Clay,” is simply a portion
iS 99 508 Mi if of ee ordinary ecuiamen
ah (ste eae iso

2 z ondon clay.

Fe 1 519 atten 3 an pebbles.
= 15 534 ny Mes
eee lOn 544% | Dark sandy clay (basement-bed of L. clay: no record of

Peli. (2l5 566 Dark brown mottled clay. [pebbles).
A; 1 567- ‘Bed of Stone.’

S 65 5733 | Red mottled clay (a very characteristic specimen pre-
6 10 5834 | Red sandy clay. [served).
ee 73 591 Fine sand. ; :
OS 4 3 594 Red sandy clay. [olive-green grains).
2 8 602 Coarse brown red sand (very ferruginous, with black and
oa 22 624 Red mottled clay, interbedded with dark grey sand, with
& traces of pyrites and numerous green grains.

el 634 Loose grey sand of the same description as in the bed
250 884 Chalk with flints. [above.

The specimens of flints preserved from the chalk are of
the usual colour of native flint from that formation.

1 Cf, Etheridge, Manual of Geology and Paleontology, pp. 609, 610.

3596 Rev. A. Irring—The Brookwood Well-Section.

calcareous material seems to have been entirely dissolved away, and
their surfaces are coated with a layer of coarse sand-grains, as if
they had rolled about in sand when softened at their surfaces by
water. They present a very different appearance to that presented
by the specimens found zn situ in the London Clay. These Bagshot
cement-stones may therefore be considered as derived in all proba-
bility from the London Clay itself.

5. The least thickness we can assign to the London Clay in
this section is 371 feet, not including the passage beds at the
top. In the paper referred to above’ I have drawn attention
to the greater thickness of the London Clay in these deep-well
sections of the more central portions of the main mass of the
Bagshot Sands, as compared with the thickness of the London Clay
beneath the Bagshot Sands, nearer the north and south margins (e.g.
in the Aldershot Town Well and the Wokingham Well). This
difference of course might arise either (1) from attenuation of the
London Clay owing to the conditions of original deposition, or (2)
to destruction of the upper beds of the London Clay by denudation
during the earlier and middle portions of the Bagshot period. The
strong evidence we have now in at least two of the more central
well-sections of a passage from the London Clay into the Bagshot
beds above, goes to show that deposition was continuous in the
central portions of the area; while the abrupt transition from the
one formation to the other and the frequent erosion of the London
Clay surface beneath Bagshot Beds observable in sections on the
northern and southern margins point to the obvious conclusion that
the London Clay was there at the same time undergoing destruction
by denuding agencies. If this be admitted, it is hardly necessary to
point the inference that a slight synclinal curvature was given to the
London Clay during the earlier portions of the Bagshot period. But
this is not all. This Brookwood section is the first, so far as J am
aware, to throw some light upon the horizons occupied by the 270
feet of London Clay penetrated in the deep well at Wokingham. A
reference to the table of strata given by Prof. Rupert Jones, F.R.S.,
for the Wokingham Well,’ and comparison of it with the London
Clay strata penetrated in this Brookwood section, brings out a remark-
able correspondence (in the occurrence of layers of septaria, of
pebbles, and of pyrites) between the 273 feet of London Clay at
Wokingham and the lower 200 feet or rather more of the London
Clay in the Brookwood section ; while from the upper 150 feet or so
of the London Clay in the latter section there is no record of such
occurrences. So close is the correspondence here cited that there is
only a difference of a foot or so in the distance of one of the layers
of pebbles in the two sections above the base of the London Clay.
These observations harmonize too with the well-known fact that the
London Clay becomes more arenaceous, and has a less pronounced
marine character in its upper beds, where shown in its full normal
development.? Of the two alternatives suggested above, we are
surely justified, in the light of this new evidence, in preferring the
denudation to the original attenuation explanation of the facts, and

1Q.J.G.S. loc. cit. * Cf, Etheridge, Joc. cit.

J. R. Gregory—Two French Meteorites. BY

can hardly escape a conclusion favourable to the notion of a certain
amount of unconformity between the two formations, along the
north and south flanks of the area. The occurrence of sharks’ teeth,
septaria, and flint pebbles in the London Clay at Aldershot, where
I have seen them dug out of the stiff blue London Clay only a few
yards below the Bagshot Sands of that section, is also in favour of
the assignment of the less than 200 feet of London Clay of that
district to the lower portions of that formation. In a future paper
I shall show that the unconformity inferred from the above evidence
can be established from a wider induction.

VI.—Tue Bots pe Fontaine Mereorirz, AND ITS PROBABLE
IDENTITY WITH THAT OF CHARSONVILLE oF 1810.
By James R. Grecory.

FEW years since I received from a correspondent in Paris
several fragments of a meteorite, which my informant stated
fell at Bois de Fontaine on the estate of the Marquis de la Touane,
near Mung, in the department of Loiret, France, in 1825, but no
precise date was given. It was said to be unknown and undescribed.
My informant also stated that it was presented to the physician of
the Marquis de la Touane, from whom he, my informant, received it
in exchange. Of the specimens that I received, two had some of the
original crust on them, one a small fragment only, and the other a
specimen of 254 grammes, but with only a small amount of crust. I
had also five or six other specimens without the crust.

On recently referring to the very detailed accounts of some of the
falls of meteorites in the early part of this century in the “ Mémoire
Historique et Physique sur les Chutes de Pierres,” by M. P. M.S.
Bigot de Morogue, published at Orleans in 1812, I find a very
precise description of the fall at Charsonville, as observed by several
eye-witnesses ; but what excited my curiosity were the same names
of persons and of places mentioned in connection with the Charson-
ville fall, as with that of the Bois de Fontaine. As the dataof the so-
called Bois de Fontaine was very meagre, and the year of its supposed
fall so widely different, I thought that possibly some error had arisen
as regards date. I afterwards compared my specimens of the
Charsonville, which I have had in my possession some years, in fact
long before the Bois de Fontaine was heard of. The British Museum
had indeed a specimen from me of the Charsonville stone at the same
time I had mine. I found on careful examination with the Bois de
Fontaine that they were identical in texture as well as in colour
when fresh broken. ‘To be still more certain, Mr. Thomas Davies, of
the British Museum, was obliging enough to allow me to compare
my Charsonville specimen with the Museum one, and I also compared
a specimen of the Bois de Fontaine with the Charsonville at the same
time.

It will be seen that it is possible that the physician named by my
informant in connection with the Bois de Fontaine stone may be a
descendant of the Dr. Pellieux named in the account of the Charson
ville fall in 1810; also that I find Meung in the map of the depart-

308 J. R. Gregory—Two French Meteorites.

ment of Loiret, but not spelt Mung as I had it with the Bois de
Fontaine stone, although in M. de Morogue’s work it is spelt Meung
asin modern maps. In M. de Siemachko’s Catalogue, Bois de Fontaine
near Beaugency is mentioned, and in M. de Morogue’s work it says
that Dr. Pellieux resided at Baugenci: this is also probably the same
place.

At page 240 of his work Mons. Bigot de Morogue says with regard
to the meteorite falls, ‘The most important which has come to my
knowledge is the fall of three stones on the 25rd of November, 1810,
in the parish of Charsonville, Canton of Meung, Department of
Loiret. At this time I was residing on my estate about six leagues
from Charsonville, and a league and ahalf south of Orleans. Some
people attributed it to the explosion of a powder magazine in the
direction of Tours; but the true cause did not long remain unknown,
for the Baron Pieyre, Prefect of the Department of Loiret, who was
as zealous for the progress of science as for the success of his
administration, having immediately made inquiry, received a few
days afterwards a detailed report from the celebrated physician Dr.
Pellieux, residing at Baugenci, a town about two leagues from the
place where the stones fell. That report was very interesting, and
was accompanied by a fragment of one of the stones, and was read
at the Public Séance of the Society of Agriculture, Physic, and
Medicine of Orleans on November 28, 1810. It was afterwards printed
in No. 7 of the report of this learned society, and has been the first
public announcement of this event due to a remarkable but never-
theless common phenomenon.”

At page 245 of the same work M. Morogue says: ‘The report of
Dr. Pellieux appeared to me to have been written rather hurriedly,
and lacked the details which I wished to know; but not being able
to go to the place where the stones fell, | wrote to M. de La Touanne,
my relative and friend, who was residing at this time on the beautiful
estate which bears his name, situate about one league from Charson-
ville, and begged him to obtain all the details possible on the
phenomenon which interested me.”

At page 247 he also says: “Monsieur de La Touanne was about
one league from the place of the fall, and was walking with his
children, when, looking by chance towards the sky in the direction
of Charsonville, he heard violent detonations or thunderings, which
seemed just over their heads. Forty persons ran from the court of the
castle, but they saw nothing. The same evening, however, they
heard that some stones had fallen at Charsonville, the fall of which
had doubtless caused the noise which had startled them. M. de
La Touanne, wishing to verify this fact, went himself the next
morning to the place, accompanied by a gamekeeper, a man-servant,
and two of his children; arriving at the farm of Villorceau, he
was convinced of the truth of the report which he had heard,
but no one had either seen the ball of fire or the light. He was told
the exact places where the stones had fallen, and he went to examine
them himself, and there he picked up some fragments of the stone,
one of which he gave me, and he then went himself to visit the
holes from which the stones were extracted. He gathered some,

J. H. Collins—Cornish Serpentinous Rocks. 309

details from some of those who had been witnesses of the pheno-
menon, of which one was a carman, a shepherd, and many others
who saw the stones fall close to them. He concluded at last all his
researches by saying that on the 23rd of November, 1810, at ten
minutes past one p.m. there fell three stones in the parish of Charson-
ville, Canton of Meung, Department of Loiret. Their fall was
accompanied by a series of thunderings which lasted several minutes.
The stones fell on a space of ground of about half a league, and
their fall was perpendicular. The inhabitants perceived neither light
nor globe of fire, either immediately above Charsonville, nor in the
neighbourhood. One of the stones fell near Mortelle, and was not
found ;* the two others fell at Villeray and at Moulin-briélé; of
these two, one weighed about 20 lbs. and had been found in a hole
just large enough to hold it, and about two feet in depth and one
foot in calcareous tuff; this hole was vertical, and the stone was
removed about half an hour after it fell, being then hot enough to
cause considerable discomfort to those who held it in their hands.
The second stone had made a similar hole in the ground, and had
penetrated three feet in depth; its weight before being broken was
40 lbs. It was taken up about eighteen hours after its fall. It seems
certain that the smaller stone, while still warm, emitted a strong
odour of gunpowder, and that it retained it even in the house to
which it was taken, until it was quite cold.”

At page 250 he continues: “One can see in No. 362 of the
‘British Library,’ published in January, 1811, an account of the
same phenomenon, which was extracted from a letter which Madame
de La Touanne had written to her mother, and of which some copies
had been by chance circulated through Orleans.”

In conclusion I think from this account that it may be taken for
a fact that the Charsonville and the Bois de Fontaine meteorites are
certainly of the same fall, though there is a probability of the Bois
de Fontaine stone being the one that at the time of the fall was not
found, and which was described as having fallen at Mortelle by M.
de La Touanne. It would, therefore, be interesting to know if
those museums and collections possessing specimens of both these
stones would carefully compare them in order to ascertain if any
similarity exists in their specimens, which might help to prove
the identity, and of which myself I have little doubt.

VII.—On tHe GeotocicaL History or THE CornisH SERPENTINOUS
Rocks.
By J. H. Coxuins, F.G.S.
(Continued from Vol. II. p. 298.)

\ Y argument that at Porthalla there is a “passage” from horn-
‘fi blende-schist to serpentine; or rather that some beds of a
common series have been changed into serpentine, others into horn-
blende-schist, and others again into a substance of intermediate
character, is, I think, much strengthened by the fact that many such
“apparent passages” are admitted to exist by all those who have

1 Query, Was this the stone known as the Bois de Fontaine ?—J. R, G.

360 J. H. Collins—Cornish Serpentinous Rocks.

examined the Lizard Coast with any degree of detail. De la Beche’s
description of that seen near the Lizard Town is as follows, and it
would apply equally well to the others. “The hornblende slate,”
he says, ‘supports the great mass of the Lizard serpentine with an
apparent passage of the one into the other in many places—an ap-
parent. passage somewhat embarrassing,” that is, from his point of view;
from mine it is perfectly natural. He goes on to say : ‘ Whatever
the cause of this apparent passage may have been, it is very readily
seen at Mullion Cove, at Pradanack Point, at the coast west of
Lizard Town, and at several places on the east coast between Lan-
dewednack and Kennick Cove, more especially under the Balk... .
and at the remarkable cavern and open cavity named the Frying-
Pan, near Cadgwith.”! At Kynance some of the laminz of serpentine
are not more than one-tenth of an inch in thickness for considerable
distances. It would not be easy to explain how such thin plates of
molten intrusive matter could be forced between the laminz of an
already consolidated stratified rock for many feet together. Now,
although thin films of remarkably pure serpentinous matter are
often found deposited from aqueous solution in thin fissures in certain
parts of the Lizard district, yet in such cases as those referred to at
Kynance I do not think such an explanation will apply, and I see
no alternative but to believe that these thin bands consist of altered
material originally stratified and forming part of the same series as
the containing rocks.

It seems to me that those who deny the origin of serpentine from
certain beds of stratified rock are ready enough to invoke Sir H.
De la Beche when his views support theirs. If, on the contrary, they
happen to clash with their views, or, which is here the same thing,
to support mine, they are very ready to explain away his conclusions.

The popular idea that the Lizard Peninsula is composed almost
entirely of serpentine or serpentinous rocks is far indeed from the
truth. Considerably less than half the area is so coloured on the
Geological Survey Map, and there is good reason to doubt whether
the whole of this is actually serpentine. Inland, the excavations are
few and far between; on the coasts, many of the cliffs are inac-
cessible ; and it may very well be that large areas of hornblende-
schist, mica-schist, gabbro, or even of ordinary clay-slate exist, within
the area hitherto regarded as wholly serpentinous, the tendency
having been hitherto to mark as serpentine whatever is covered by
a soil containing fragments of that rock.

II. Tae Exrra-Lizarp SERPENTINES.

Whatever may have been the origin of the Lizard serpentines, it
is certain that serpentinous change in the West of England is not
confined to the Lizard District. Serpentinous rocks exist in many
other parts of Cornwall and Devon; and probably the total area of
what may be called the “‘ Extra-Lizard ” serpentines is not less than
that of the serpentines of the Lizard Peninsula. Some of these
rocks have been described by various writers, and in considerable

* Report on Cornwall, etc. See also Memoirs of the Geological Survey.

J. H. Collins—Cornish Serpentinous Rocks. 361

detail ; but the descriptions not being generally known, as are those
of the Lizard, I refer to them here a little more in detail.

A large proportion of the Extra-Lizard serpentinous masses seem
to have been at one time essentially hornblendic rocks. I do not
say originally hornblendic, but the production of hornblende has
preceded that of serpentine. Some, too, appear to have contained
considerable proportions of olivine, but this mineral does not, so far
as I am aware, exist in them in an unchanged state.

Some writers draw a notable distinction between serpentine rocks
and those which are merely serpentinous. This is no doubt a con-
venient distinction in some instances; yet it will be often difficult
to define the limits of this distinction, since there is no radical differ-
ence. On the one hand, there is no such thing as a rock-mass of
pure serpentine ; while, on the other hand, all serpentinous rocks,
whether approximately pure, porphyritic from the presence of un-
altered or only partially altered crystals of foreign matter, or con-
taminated by streaks and patches of foreign substance, are altered
rocks, and the serpentine present, whether much or little, is admittedly
an alteration product. To avoid naming such rock-masses serpentine,
as that of Duporth for instance, it has been proposed to class them
with picrite, but I cannot see that much is gained by this. Some
portions of this rock, it is true—from the presence originally of a
great many crystals of felspar, now mostly kaolinized—are indeed
highly aluminous; but other parts contain very few such crystals,
and consequently the alumina sinks to an insignificant amount.
But, whatever the amount, the basis of the rock is plainly and dis-
tinctly serpentine, and even very pure serpentine; and to call it a
picrite, apart from the objections to the use of this term as a rock-
name owing to its indefiniteness, seems to me not merely undesir-
able, but even somewhat misleading, if it be understood to beg
the question as to the nature of the original rock. Certainly there
is neither olivine nor diallage present now, and it is by no means
certain that the rock ever contained either.’

T will now proceed to give some brief particulars of the various
masses of rock outside the Lizard Peninsula, but within the mining
region of Cornwall and West Devon, which exhibit a high degree
of serpentinous change.

1. Veryan? (Gerrans Bay).—The serpentinous rock at Veryan is
a narrow band of dark green colour, which is associated with well-
marked gabbro similar to the rocks which form a great part of the

1 T do not find picrite mentioned in my edition of Von Cotta. Dana says (p. 258),
Picryte from Moravia ‘‘ consists half of chrysolite (olivine) along with felspar,
diallage, hornblende and magnetite.” Rutley defines it (Study of Rocks, p. 265) as
‘blackish -green crystalline rock with a compact black matrix containing porphyritic
crystals and grains of olivine. The matrix may consist of hornblende, diallage, or
biotite, associated with magnetite and calc-spar. The olivine constitutes nearly
half the bulk of the rock.’’ Prof. Bonney regards it as a compound of olivine,
a small variable amount of felspar, such as anorthite or labradorite, enstatite or a
pyroxenic mineral with biotite.

2 This district was surveyed by Mr. N. Whitley, of Truro, in 1841, and described
in the Report of the Royal Institution of Cornwall. The serpentine was also
described by the Rev. Canon Rogers in the Trans, Royal Geol. Soc. of Cornwall,
vol, vi. p. 41, 1846.

362 J. H. Collins—Cornish Serpentinous Rocks.

parish of St. Keverne. It comes in as a wedge between the dark
hornblendic “ greenstones” of the Nare Head and the Lower Silurian
slates and quartzites of the same locality. The excavations upon this
band are now mostly filled in, and it is greatly decomposed where
it reaches the sea in Gerrans Bay, and appears only as a soft ferru-
ginous mass, so that it is almost impossible to determine whether
it is simply an altered bed or occurs as an intrusive mass. For
reasons which I need not now specify, I incline to the latter opinion,
yet it is worthy of remark, as pointed out by Canon Rogers, that
the strike of the band lies in a straight line with that of the serpen-
tine of Porthalla, in the parish of St. Keverne, which is distant some
15 miles to the south-west, and this is at least suggestive of a
common origin. However this may be, the serpentines of these
two localities are extremely different; the Veryan rock more
resembling the ordinary Lizard serpentine than does that> of
Porthalla. It has no cleavage, but breaks with a splintery fracture
like ordinary serpentine. In the mass it is slightly magnetic.
Under the microscope, using a 2-inch power, it is seen to consist of
a transparent green base, which incloses and surrounds many large
much-fractured crystalline masses, not definite crystals, which may
be altered olivine. No calcite is visible, but in some places numer-
ous fibres of asbestos may be seen. Throughout the serpentinous
ground-mass are sprinkled numerous dark patches of ferruginous
matter, as in the serpentine of Coverack. The base of course is not
dichroic, nor are the crystalline patches; but these latter are
brilliantly coloured by the use of polarized light, especially the
asbestos fibres when both polarizer and analyzer are used. The base
changes as one Nicol is rotated from pale yellowish green to black.
It is possible that this may be altered picrite or some similar rock ;
but if so, the metamorphosis is very complete, as it contains only one
per cent. of alumina. The following are my analyses of this rock :
1 2

Silica SS AO Teor io OO TaL) sccatek 86:05
MUMING A. .hehen eons bee, cael, wl'300 Be Ree "95
Inert Ora. o55 0 c068 coo. doors »eP iO ABREMEaSC 8-00
Ferrous Oxide... ... ... ... 2°25 1 UR 1:00
Chromic Oxide Soil et Pitrace a aos trace
Lime ican Weide ow sed oa uel a UEACE witthn goes trace
MAGNESIA seek ny occ MOS 00 Beate dae 33°79
‘Alivaliess emcee Bae rans le Spare aoe 4:89
Water (by ignition) ... ... 14°69 daa, dae 12°39

101:05 97:07

T have observed thin layers of serpentinous matter in the joints and
fissures of the hornblendic “‘ greenstone” of the Nare Head, where
it comes in contact with this serpentine, but I have not suffi-
ciently examined this latter to be able to say whether it exhibits
evidence of serpentinous change in itself, or whether these thin films
have been merely deposited from water percolating through the rock,

Duporth.—This serpentinous rock has been analyzed and described
by Mr. J. A. Phillips! and by myself.? It seems to form the eastern
termination of a dyke of hornblendic greenstone which extends from

1 Phil. Mag. Feb. 1871. 2 Min, Mag. Nov. 1877.

J. H. Collins—Oornish Serpentinous Rocks. 063

near the ancient earthwork called Trethullan Castle, in the parish of
St. Mewan (near St. Austell), to the sea near Duporth, a distance of
over four miles. The typical greenstone in the St. Mewan quarries
often contains asbestos and thin layers of serpentine in its joints, and
an examination of this intrusive mass in different parts of its course
shows that it becomes more coarsely crystalline and porphyritic as it
approaches the cliffs, and that the chemical composition is also
changed, until finally the hornblendic rock of St. Mewan becomes a
serpentine at Duporth.

The less decomposed portions near the sea-level are seen to consist
of serpentine of a darker green colour, full of greyish-white spots of
a substance resembling kaolin, which on examination appear to be
pseudomorphs of hornblende and perhaps felspar, varying from 35
to 4 of an inch in length. The crystals have not quite lost their
power of depolarizing polarized light, but the difference between the
crystals and the green base in this respect is not extremely great.

The green serpentine base is often somewhat fibrous, the fibres
curving round the larger crystals and exhibiting brilliant colours
with polarized light; it is sprinkled with very small prisms of
scarcely altered felspar. The base and the altered included crystals
are both sprinkled pretty thickly with crystals and grains of oxide
of iron, and the whole rock is in places stained yellow or brown
with per-oxide of iron.

The following analyses show the interesting changes of chemical
composition exhibited in this mass in different parts of its course.
(a) is the mean of three analyses of the rock at St. Mewan made by
Mr. Phillips,’ (6) is my own analysis of the rock from the quarry
near Gewans, (c) my analysis of the rock at Duporth, and (d) a
recent analysis of the same rock made by Mr. J. Arthur Phillips.’
(é) is a partial analysis of a selected sample which is more free from
included crystals and from oxides of iron than ordinarily.

a. b. C. d. é.
SPM GUe sen cececkenmncsasectee DOO A Gas 1 ROSE) wan nn ROG Da MTG ee PACtaKG)

F ; 72 me
Berens ee 5 uate SO iach ADI CSAC Beene apa| ven EE
SILO, DS Aa Shania aeeene eeasee MTS con OPKS 50 BADD con BOE coe SIMD)
Iie ANGI, .casosoecboospcob THEN) iady TURKS Wedge “ANRAIGE Sogo === og
Phosphoric Acid............ Di ier 2.0) “i Pa ee 18... —
MAN ITAMINIT AS Wert fee dod Sebeaeclee U7 UG is ROTO ea O90! Fe, wDe28) SAS
HerriciOxide)esssss..ceoeeoe 13°04 15°30 ene aia a 8-8
Ferrous Oxide ............... aa aa WAV ory BERHE) S>
Oxide of Manganese ...... TEARS) beg | WHEXE®). oon HS gc 98... ———=
PUI OIMET? 616s SdosbabonbeEedee trace ... trace ... 506 .._o—
SIGIO EA aN DE Nea cis fe saatbstvcicelelsis Ao) MOsO2ie ese tracer) 2.40) trace!) 324)/)i——=—=
IMI eMESI aye ersck.-2idesjocslsteas trace) cea PB can NOW cog 2G ic.) 28
ROPASH 22 vceasiesiesbectessces'e 2°30 7-2] ised trace... ——
Sisk Geacnaae aeeeeearaaorcr 5 re Be : “25 —

99°85 98°89 99°31 100°04 91:08

1 Phil. Mag. Feb. 1871.
2 For this analysis, which was given in the Mineralogical Magazine, Joc. eit., I
am indebted to Mr, Phillips. He remarks, “I find more magnesia than you do, but

364 J. H. Collins—Cornish Serpentinous Rocks.

From these analyses it appears that the change is not great at
Gewans as compared with St. Mewan, a distance of a mile and a
half, and that it consists chiefly in a lessening of the proportions of
iron oxides and a slight increase in the silica. Within the next mile,
however, a very notable change takes place, the silica being reduced
by upwards of 12 per cent., and the alkalies entirely carried off,
while the proportion of water increases from less than one to over
eight per cent., and the magnesia from less than one to nearly sixteen
per cent., or in Mr. Phillips’ specimen over 22 percent. Chemically
and mineralogically the rock now consists essentially of something
over 30 per cent. of serpentine as a base or ground-mass, containing
in crystals and grains nearly 50 per cent. of kaolin, and nearly 20
per cent. of peroxide and magnetic oxide of iron, while in e it is a
fairly pure serpentine.

I must refer to the paper above mentioned for illustrative draw-
ings of the microscopic structure of the rock. Prof. Bonney con-
siders that from the high proportion of alumina present in this
rock, it ought not to be classed with the serpentines; in his
Presidential Address to the Geological Society he says of it, “The
serpentinous rock of Duporth . . . . appears to be a member of the
picrite group. Many of the picrites certainly hang on very closely
to the dolerite group, and can be seen to graduate into representatives
of it;” but the analyses given above will show that this is an accidental
rather than a characteristic component, arising from the distinctly
imbedded crystals, and that, in the portions of the rock where these
crystals are more sparsely distributed, it approaches in composition
an ordinary serpentine rock (which is usually a very different thing
to the mineral serpentine).

I have said above why I think this rock should not be classed as
picrite. It does indeed seem to have been originally a dolerite,
but there is no proof that any considerable proportion of olivine was
ever present. ‘The first alteration of the augite seems to have been
its conversion into hornblende, and this has subsequently been altered
to serpentine.

As to the cause of this remarkable change of a hornblendic into
a serpentinous rock, I may remark that the district is one of very
extensive disturbance, traversed in all directions by mineral lodes
and elvan courses; and it is not more than two miles from the St.
Austell granite. I have elsewhere! given my reasons in detail for
believing that the extensive kaolinization of the felspar of that
granite has been produced by mineral solutions acting through
fissures from below. I have little doubt that this production
of serpentine is due to a similar action, and probably fluoride of
magnesia was the principal cause of this alteration, both of the
hornblendic base and of the felspathic crystals.

Clicker Tor, near Liskeard.—This remarkable intrusive serpen-

my specimens have undergone more extensive change than yours, as you will see from
the fragment which I inclose.’’ He also observes, ‘‘ My recent analysis of some
remarkably fresh rock from the Sanctuaries gave 1-75 per cent. of maguesia.”’

1 The Hensbarrow Granite District, 1876.

J. H. Collins—Oornish Serpentinous Rocks. 365

tinous mass, well known to tourists as well as to geologists, has
been fully described by Messrs. Allport’ and J. A. Phillips.’

Mr. Allport regards the serpentinous base as being due to the
metamorphism of felspar, and this is no doubt the case to some
extent, as at Duporth; however, much of it appears to be due to the
alteration of hornblende, itself an alteration product of augite.

Mr. Allport describes it as follows :—

“Under the microscope, a thin slice of the intrusive rock exhibits
a variegated mass of pale green serpentine and a nearly colourless
substance intimately blended together; imbedded in this matrix
there are numerous pseudomorphs after olivine, and irregular plates
of unaltered augite, together with minute grains of magnetite scattered
here and there through the mass. The pseudomorphs after olivine
are of two kinds, consisting either of serpentine or the white sub-
stance just mentioned ; both are highly characteristic ; the crystalline
forms are perfectly preserved, and they are traversed by veins
representing the original cracks so generally formed in this mineral.

“Tn one slice the augite is also greatly altered, and it is interesting
to compare the two pseudomorphs side by side.

« Although the ground-mass of the rock exhibits a confused amor-
phous appearance both in ordinary and polarized light, we are
fortunately not left in doubt as to the nature of at least one of its
original constituents. The augite frequently incloses highly charac-
teristic pseudomorphs after felspar; some are completely inclosed,
while others are only partially imbedded in it; the mode of occur-
rence is, in fact, precisely the same as that observed in the altered
gabbro of Costorphine Hill, near Edinburgh, and in several Scotch
dolerites described by me on a previous occasion.’ In many cases
the unaltered augite has preserved in the most perfect manner the
sharp edges and angles of the felspar prisms; and whenever the
latter project from the augite, it may be readily seen that both the
inclosed and outlying portions have been converted into precisely
the same serpentinous substance as that forming the ground-mass.
It should also be noted that, in the case of partially-inclosed prisms,
only those sides or ends which have impressed their shape on the
augite exhibit a crystalline form, the outstanding portion being quite
undistinguishable from the surrounding mass.

«As it would evidently be absurd to suppose that originally there
was no felspar save that inclosed in the augite, there can be no
doubt that the original felspathic matrix has been completely meta-
morphosed, and that we have in the Menheniot. rock a highly-in-
teresting and instructive example of the conversion of an intrusive
olivine-dolerite into a mass of imperfectly-formed serpentine.”

The following is an analysis of this rock by Mr. Phillips :—

Silica} encsven chy Be kee ee eee 86360
Alumina Py ea ee am cies, Pree ucts)
Herrie Oxide@.15 ses keg sees eee meester eee
Ferrots Oxides .{..ciibeeiyeedsi. 28 Ghelkes Wo 4502
1 Quart. Journ. Geol. Soc. 128, Nov. 1876, p, 422. 2 Phil. Mag. 1871.

3 Quart. Journ. Geol. Soc. vol. xxx. p. 557.

366 J. H. Collins—Cornish Serpentinous Rocks.

GhromiciOxides, 225 etveeecon ch Se Ole:

Chidori @t IWieNey S55 a5 ong ose con I
Tame) Sekev cect, 28s), Chee cee he as LEEeneee ain FOROS:
Mapnesia onusser save e svete sunecc tsa “tee! MONON
Soda. cso Be eis tise, Cee nents BOS!
Moisture Sihe, (edo Lifesed bess Seeeetedan toeeemelOL6G

99:10

Polyfant.—The “ potstone” of Polyfant near Launceston has long
been known as a very infusible and easily wrought rock, one of the
few Cornish rocks suitable for elaborate and highly-finished church
decoration, and it has been used for such purposes in most of the
churches of the neighbourhood,' but I am not aware that the rock
has been hitherto described from the point of view of the petrologist.

The quarries are very ancient and much filled in, but as far as can be
seen they lie in the strike of the associated slates. To the unaided
eye the rock appears as a dark greyish-green slightly talcose mass,
in some places spotted brown with peroxide of iron. Its structure
is somewhat schistose and at the same time brecciated. Whether it be
an intrusive mass or an altered volcanic agglomerate is still somewhat
uncertain, but I incline to the latter supposition. Under the micro-
scope, and using the 2-inch power, it exhibits a great many colour-
less crystalline masses, having two cleavages forming oblique angles,
which may be altered diallage or enstatite. They are slightly dichroic,
but quite dark with crossed prisms. There are also some nebulous
nearly circular or hexagonal patches which occasionally have a green
spot or a grain of magnetite in the centre. The ground-mass is green
—in some parts dichroic; in others not—it is resolvable under the
4-inch power into a fibrous mass of asbestiform material, which polar-
izes strongly using crossed prisms where thin. A great many black
square crystals of magnetite are present—also some patches of brown
oxide of iron probably resulting from the decomposition of pyrites.

My analysis of the rock—in duplicate—gives the following as its
composition :—

a. 6

Water given off in dessicator...... 94 : ive
i ae ignition ...ee.eeecssees we phy OLS tpl ogze
Siltea: ieee caw. chee oehindan tence ten san HOO) sg END
VAT UMN aa aatewateattet hee eee Snore Jub Sa5 ie
HernonsiOxidepeecneeeeee eee eres weal) ONOO ene eso.0)
Bernica Oxides t..cescccecdeseeteheees ano) LATO) 555 SILC)
TMG EE EER cote es ltae ote Mey 280) meee aol
MAO MESIA Ste seeecce pase anse aren ene ee -. 16°03 ... 18°58
(Po bashty:.. sattasdso cecal eaecontane Pek ORO Plepay) pono,
Soda..........- Neale Nc CARRE MRE tae neta ... trace trace
98°89 99°34

Although there are considerable differences between this composi-
tion and that of the Duporth rock, yet if chemical composition alone
be taken into account—and as a whole there is a good deal of

' A shallow basin or crucible of this rock has been recently found in close juxta-
position with a ‘‘celt mould’’ of hard sandy slate at Altarnum, a few miles from the
_Polyfant quarries. It was probably used for melting the bronze used by the ancient
Britons, It is now in the Museum of the Royal Institution of Cornwall at Truro.

Notices of Memoirs—Short Notices of Scientific Papers. 367

analogy between them. But in the Polyfant rock felspar, whether
kaolinized or not, seems to be entirely absent, and this forms a
notable distinction. Moreover, a great deal of the serpentinous
matter certainly does not resemble highly altered olivine; so that,
if there be any rock properly to be classed with the picrites in
Cornwall, this is it. It must, too, be admitted that the Duporth rock
has a good deal of superficial resemblance to it, although it was
originally so very different. The Polyfant stone is quite soft—
except for the occurrence of occasional hard grains of pyritous or
siliceous matter—so that it can be readily cut with a chisel or even
with a pocket-knife. Sound fragments have been formed into
crucibles and used for melting tin and copper for small castings. It
appears to be well adapted for this purpose, although I am unable
to say that it has advantage over the ordinary ‘‘ black-lead ” pots.

IN(OaRIESG aS) OusT AMEA IM KO ab Sa=)-

———__

I.—Suort Notices oF SCIENTIFIC PArErs.

1.—Iattagelser Ofver qvartira bildningar pa Gotland. Af Henrik
Munthe. Geol. Foreningens i Stockholm Forhandlingar. No. 100.
Bd. viii. H. 2. :

2.—Om postglaciala sinkningar af Gotland. Af. G. Lindstrém.
id. No. 102, Bd. viii. H. 4.

HE first of these papers contains many interesting facts respect-
ing the Glacial and Post-Glacial phenomena of the isle of
Gotland. Two systems of Glacial striz have been noted, one, best
developed in the north and north-west, has a main direction from
N.W. to S.E., and the other, extending over the rest of the island,
runs from N.E. to S.W. Raised beaches are traced at various eleva-
tions up to 78:5 m. or 259 feet above the sea-level, the highest point
on the island. A description is given of a remarkable As or Kame
near Visby, which rests on Boulder-clay, and is partially covered by
it. The erratic boulders are traced from the Aland isles, Angerman-
land; possibly from the South-west of Finland, and from the bed of
the Baltic. ‘Two maps are appended ; one showing the direction of
the striz and the contour-lines of the island, and the other of the
district round Visby.

In the second paper, Prof. Lindstrém gives a description of sections
lately exposed at Hafdhem in Gotland, in which turf deposits,
nearly 50 feet above the sea-level, containing 28 species of existing
freshwater mollusca, are overlaid by a marine sand with littoral shells.
The author points out certain facts in the configuration and structure
of the rock terraces in Gotland which indicate that the island received
its present form by denudation, previous to the Glacial Period, and
that various changes of level have taken place since that time.

3.—Om Kambriska pyramidalstenar. Af A. G. Nathorst. Ofversigt
af Kongl. Vetens.-Akad. Férhandl. 1885. No. 10.

4,—Sur les causes de la production de facettes sur les quartzites

368 Notices of Memoirs—Short Notices of Scientific Papers.

des alluvions pliocénes de la vallée du Rhone, par M. F. Fontannes.
Bull. de la Soc. Geol. de France, t. xiv. 1885-6, p. 246.

Dr. Nathorst notices the various opinions held by German and
Scandinavian geologists respecting the origin of pebbles with dis-
tinctly facetted surfaces, and he points out that, before they had been
particularly remarked in Europe, attention had been called to them
in New Zealand by Mr. Travers,! in 1869, and their facetted surfaces
had been rightly attributed to the action of wind-driven sand. The
author records the interesting fact that pebbles with facetted surfaces,
precisely similar to those from New Zealand and elsewhere, had been
lately discovered in the Hophyton sandstone of Lugnas, Sweden.

M. Fontannes brings forward, in the paper cited, ‘several objections
against the sufficiency of wind-driven sand to produce the facetted
surfaces of the quartzitic pebbles found on the slopes of the Rhone
valley, and attributes the phenomena to the current action of water
and sand.

5.—On the Minute Structure of Stromatopora and its Allies. By
Dr. C. Rominger, Proc. Acad. Nat. Sci. Phil. 1886, pp. 29-56.

This paper is a criticism of the joint essay by Prof, Nicholson and
Dr. Murie on the structure of Stromatopora, which appeared in the
Journal of the Linnean Society in 1879! It is certainly peculiar to
read this review on a paper published six years ago, and one wonders
what Dr. Rominger has been doing in the interval. He does not
even now seem to be aware that one of the authors of the paper,
with which he can see so much to disagree, has in the meantime
further studied the subject, and has himself considerably altered his
previously-expressed views. It seems somewhat presumptuous on
Dr. Rominger’s part to propose to substitute some names of his own,
which he brought forward in an unpublished paper unluckily rejected
by the Smithsonian Institution, for those given by the authors of
the paper he criticizes.

6.—Review of the Progress of North American Invertebrate
Paleontology for 1885. By J. B. Marcou. ,American Naturalist
Extra, June, 1886, p. 505.

This paper gives a list and a short précis of the various works
which have appeared on the subject. The author remarks that there
is a distinct increase in the number of articles on paleontology, and

that the tendency to publish new species without any illustrations is
also diminishing. _

7.—A List of the Cretaceous Foraminifera of Keady Hill, County
Derry. By Joseph Wright, F.G.S. Proc. Belfast Nat. Field Club
Appendix, 1885, p. 327.

Mr. Wright published in 1874 a list of the Cretaceous Microzoa
of Ireland obtained from the material in the interior of flints, and
the present paper contains a list of 94 species and varieties of
foraminifera from the base of the White Chalk at Keady Hill.
Twenty-seven of these are additions to the Cretaceous Fauna of

1 See also a paper by J. D. Enys, “ On Sand-Worn Stones from New Zealand.”
Quart. Journ, Geol. Soc. vol. 34, 1878, p. 86.

Reviews—Dr. Johnston-Lavis—Earthquakes of Ischia. 369

Ireland, and three forms, Gaudryina Jonesiana, Bolivina decorata, and
Marginulina Reussiana, are new to science. The new forms, as well
as some others, are figured in the plate accompanying the memoir.

GideE.

54) da DVG SRS WA tSe

I.—MonocrarH oF THE HartTHquakes oF Iscntra. A Memorr
DEALING WITH THE SeErsmic DisTuRBANCES IN THAT IsLAND
FRoM Remotest TIMES, WITH SPECIAL OBSERVATIONS ON THOSE
or 1881 anp 1883. By H. J. Jouyston-Lavis, M.D., F.G.S.,
etc., and Some Caxtcunations by Rev. Prof. Samurn Haveuron,
M.D., F.R.S. 4to. pp. 112. With numerous Plates and Photo-
graphs. (F. Furchheim, Naples; Dulau & Co., London, 1885.)

N this work Dr. Johnston-Lavis has essayed to do for the recent

earthquakes of Ischia that which was so well accomplished for

the great Neapolitan earthquake of 1857 by the late Mr. Robert

Mallet. In the mathematical portion of the work he has been

fortunate in securing the co-operation of Dr. Haughton, who supplied
Mr. Mallet with the necessary equations for his work.

The excellent way in which Dr. Johnston-Lavis made use of his
opportunities as a resident in the neighbourhood, after the earthquakes
of 1881 and 1883, is very well known; and the columns of Nature
and various newspapers were supplied with detailed accounts of
catastrophes from his pen, many of which contain observations
of considerable scientific value. But in the present work, he has
treated the whole subject in a systematic and comprehensive manner,
and has succeeded in producing a book which, like that of Mallet,
is of great value both to seismologists and geologists.

After a short introductory chapter, the author devotes six pages to
a résumé of what is known concerning the geology of Ischia, based
on the researches of Scacchi, Fonseca, Vom Rath, Fuchs, and other
geologists. Chapters III. and IV. are chiefly historical; the former
dealing with the earthquakes and eruptions which have occurred in
the island from the earliest historical times down to the present day ;
while the latter contains a translation of Covelli’s interesting account
of the Ischian earthquake of February 2nd, 1828. Chapters V. and
VI. are occupied with the details of the author’s own observations
on the effect of the earthquakes of March 4th, 1881, and of July
28th, 1885, respectively. The destructive effects of these great earth-
quakes are made strikingly apparent to every one, and especially to
those who have visited the island, by the series of admirable photo-
graphs, taken for the most part by the author himself, and repro-
duced for the purpose of this work in Turin.

The next three chapters of the book are devoted to a discussion of the
nature of the earthquake waves, and of the paths which they followed,
and to a determination of the positions of the seismic vertical,
the epicentra, and the isoseismals of the two earthquakes; while,

DECADE III.—VOL. III.—NO. VIII. 24

870 Reviews—Dr. Johnston-Lavis—Earthquakes of Ischia.

from the observations on angles of emergence at various points, con-
clusions are deduced as to the form of the “ focal cavity ” and its
mean depth from the surface. It is admitted that the data obtained
by those observations are too few and imperfect to base absolutely
reliable conclusions upon ; but the careful plotting upon maps and
sections of those measurements which seem most worthy of con-
fidence, points to the conclusion that the centre of the disturbance
was the same in both cases, and must be sought on a line less than
one mile in length, running nearly north and south beneath Casane-
nella from near Lacco towards Fontana. The mean depth of the
focus was calculated for the earthquake of 1881 as 518-25 metres
from the sea-level, and that of 1883 as 528 metres. The author
suggests that the seat of disturbance is a vertical fissure, filled with
igneous matter, which is gradually extending itself upwards towards
the surface.

In a chapter on the phenomena connected with the earthquakes,
the author points out that the Ischian earthquakes were accompanied
by muffled rumblings, which near the centre were simultaneous
with the shock, but which further away from the centre preceded
the shock. Dr. Johnson-Lavis’ careful investigation of the reported
changes in thermal and other springs in the island before the shock
led him to the conclusion that these reports were for the most part
unworthy of credence; but in the case of a well near Forio, what
seems to be satisfactory evidence is adduced in support of the
conclusion that shortly before and after the earthquake sudden
changes in the qualities of the water took place; and Prof. Palmieri
suggests that the well might be in communication with a fumarole,
which from time to time exhibited increased activity. Landslips
affecting the soft tufaceous masses which cover so large a part of
the island are also shown to be a frequent accompaniment of earth-
quake-shocks, though they also sometimes occur quite independently
of seismic disturbances.

In his two final chapters, and in an appendix, the author indulges
in some interesting speculations concerning the cause of the earth-
quakes of Ischia, and he ventures on some suggestions as to the best
methods by which their destructive effects may be guarded against
or even prevented. If, as he thinks, a fissure on the side of the
old voleano of Eporneo is being extended upwards, till at last the
disturbances will culminate in a volcanic outburst, producing another
parasitical cone on the old volcano, he suggests that a deep bore-hole
might serve as a safety-valve to prevent the destructive accumulation
of steam. More practical, perhaps, is the suggestion that careful
seismic observations with suitable instruments might result in ob-
taining useful warnings, as well as more exact knowledge of the
phenomena. And lastly he points out that not a little may be
done, during the rebuilding of the towns, in the selection of sites,
the arrangement of the positions and forms of houses, and in the
choosing of the materials and designs of their construction, to ward
off the terrible dangers which seem to beset them.

In concluding this notice of a very interesting work, we must

Reviews—Prof. John Milne—Earthquakes. 371

heartily congratulate its author upon the energy and zeal with which
he has performed his self-appointed task, no less than on the character
and appearance of the volume in which he has recorded his results.

IJ.—EHartruquakes AND oTHER Hartu-Movements. By Pror. Joun
Mitnz, F.G.S. With 388 Figures. Vol. LVI. of the Inter-
national Scientific Series. (Kegan Paul, Trench & Co.)

INCE Mallet’s “First Principles of Observational Seismology,”
better known as “A Report on the Neapolitan Earthquake of
1857,” no book has appeared on this subject comparable in importance
to the present volume. This seems indeed to mark a new epoch in
the progress of the science, as that book certainly marked a former
epoch, which should probably be reckoned the first. A contrast may
be drawn between the two. ‘The first is mainly observational, and
its observations are made on single great earthquakes ; its names are
Mallet and Hopkins ; its region of research is Italy ; and its concep-
tion of an earthquake is one or more shocks. The new epoch is
experimental as well as observational ; and its observations are made
on all, even the minutest tremors ; Hwing, Gray, Milne, are its names,
its classic region is Japan; and it conceives an earthquake as a train
of vibrations. Its great advance is due to the introduction of an
instrument of exact research, the seismograph properly so called, a
seismometer with recording apparatus. All previous means, the
author remarks, ought to be classed not as seismometers capable of
measuring a disturbance, but as bare seismoscopes indicating only
that a disturbance has taken place.

Our volume presents a full view of the present state of knowledge
on this obscure and difficult subject. If any person wonder that
so complete a treatise can issue from so remote a region, let him
remember that from that region come all the latest additions to our
information. Much credit is due to Mr. T. Gray for his revision of
the proofs. The correctness shows the pains that must have been
bestowed. The only serious error we have noticed is in the equations,
etc., of p. 211. Here certainly either explanation or correction is
needed. Ought not the index of the second power to be affixed to
each letter in these equations ?

No branch of the study is neglected: all receive attention. Hven
practical aspects, so often despised by men who suppose themselves
scientific, here have a full share of notice. The ‘general conclusions’
at the end of Chapter VII. give valuable advice to those who have
to build a house in a region exposed to such dangers. There is even
a suggestion for the use of Earthquake lamps to extinguish them-
selves in the act of being overthrown. The ‘ Harthquake coats,’
described as having pockets ready filled with provisions as preparation
at a moment’s notice for spending a night in the air, relieve with a
little amusement more serious recommendations. Undoubtedly the
most important notes of advice are No. 8: ‘ Follow one of the two
systems for constructing an earthquake-proof building,’ and No. 1:
‘In choosing a site, find out the localities which are least disturbed.’

372 Reviews—Prof. John Milne—Earthquakes.

The chapters on the ‘ Distribution in Time’ of earthquakes contain
much information and some valuable tables. Extremely interesting
is an attempt to exhibit graphically the variations of seismic energy
for a particular district, that of Kioto, during twelve centuries. It
is curious to find not a continuous decrease but a general diminution
interrupted by a temporary increase four centuries back. Not much
faith, however, can be placed in any conclusions based on mere
records of remarkable shocks. We find surely the temperature of
a day easier to estimate than the intensity of a shock. Yet how
uncertain are we still as to any real alterations in English climate
during a like succession of ages.

Far better founded are the discussions as to the relations of
earthquake frequency, intensity, or time of occurrence, with seasons,
tides, planets, or barometer. Even here, however, negative answers
are disappointingly prevalent, and the solitary result to emerge is
that their number is greater in winter.

More valuable and far more trustworthy conclusions are obtained
under the heading, ‘ Distribution in Space.’ The author’s somewhat
novel sport of ‘ Harthquake hunting’ (Chap. X.) has already brought
to light several facts of the first rank in importance. Such are, the
existence of groups with more or less definite boundaries and separate
centres of radiation (see p. 191); the significant coincidence of much-
shaken regions with lines where continents dip-steeply into oceans ;
and the action of mountain ranges in barring the progress of a
shock. More information on this last now celebrated observation is
very much to be desired. Some mountain countries (as Switzerland)
are often shaken. Do these shocks originate in the mountains, and
if so do they extend into the plains? or does each region keep its
products to itself? Is there Free Trade in earthquakes there, or
Protection? If delicate instruments like Professor Milne’s were
judiciously placed and regularly observed, we think it probable that
much information might be obtained on points of this nature.

Descriptions of these beautiful instruments form a very interesting
portion of the book. The account is, however, brief. It enables the
reader to see the action of the machines, but does not go very deeply
into either fundamental principles, or practical difficulties. For
these a student must refer to the various original memoirs. The
principle which underlies all these machines alike is that the surface
of the earth moves, and that to obtain a true record of its motion,
something must be provided which remains unaffected and does not
move with the earth. A freely suspended pendulum fails because
a motion of its point of attachment soon creates motions of the bob.
A slab on rolling spheres fails because impulses to the slab by
friction from the balls cannot be avoided. And whereas a beginner
would expect a moving point to write records on a plate, the reader
will learn that the writing point is arranged to be motionless, while
it is the recording plate which moves with the earth. The difficulty
of recording vertical motions by any device is so great that one
almost disbelieves any measure of success can be obtained.
Ingenious means for overcoming these difficulties are described,

Reviews —Prof. John Miine—Earthquakes. 379

and students desirous of learning more may consult a paper in
vol. xxxix. of the Quarterly Journal of the Geological Society ; and
the Transactions of the Seismological Society of Japan. Not the
least important application of those beautiful instruments has been
the observation of artificial earthquakes. Much curious and useful
information has thus been obtained. The effects of canals and
even ditches in arresting surface vibrations, though to some extent
previously known, are here more completely established. A result
of the highest scientific importance that seems looming in the possible
future is a true measure of the intensity at origin of a disturbance,
as is hinted at on page 62. One drawback to the value of these
experiments is that they are made solely with disturbances produced
by percussion or explosion, while we can hardly doubt that some
earthquakes at least, and probably very many, are due to causes
which have no resemblance to a blow.

Interesting purely theoretical discussions will be found in various
parts of the book. The diagram in Chap. VII. illustrating reflection
and interference is clear and instructive, but readers should remember
that the energy of a reflected shock is probably greatly diminished
from the energy of incidence. The problem of deducing the origin of
an earthquake from observations of its time of occurrence at several
distinct points receives elegant treatment in Chapter X. All methods
described are vitiated theoretically by changes in velocity of pro-
pagation (which Prof. Milne himself has shown to exist), and practi-
cally, in such cases as our own Colchester Earthquake, by the
inexactness of most records of time. When these last can be trusted,
it is probable that the theoretical methods will approximate to the
true origin, if there be one, with sufficient accuracy for any practical
purpose.

A well-known effect, often observed and often commented on, the
rotation produced in many objects by the earthquake, is discussed in
the chapter on ‘Determination of Origins.’ Preference is given to
an ingenious explanation credited to Mr. Gray. We cannot, however,
ourselves see that this is a very essential advance on the explanation
given by Mallet. Their common principle is that a resultant impulse
which does not pass through the centre of gravity will create in the
body rotation, and the point of the new suggestion appears to be that
in bodies on rectangular bases, this impulse must in general come
from oneangle. The explanation is not applicable for circular bases.
Both seem insufficient in view of Meldola and White’s observation
(‘Hast Anglian Earthquake of 1884,” p. 206), that chimneys were
in general rotated all in the same direction ; with which agrees Prof.
Milne’s own remark on the stones of the Yokohama cemetery.
After all, what object is there in trying to dispense with ‘ vorticose
motion’? As we are dealing not with water, but with earth, the
only meaning of the phrase is that a vibratory motion is propagated
in a direction transverse to the direction of vibration; the trans-
mission, in brief, of a wave of shearing strain. All instruments at
present in use only record the motions of a single point, and none of
them are able to distinguish between normal vibrations and trans-
versal such as these.

374 Reviews—Ulrich’s Palwontology.

In Chap. III. a lucid but too brief exposition is given of the
consequences from snap after tension, slip after shear, and shock
after explosion of steam. The question of Cause is again referred
to in Chap. XVII., and other notices occur. The accounts of Earth
Tremors and Harth Pulsations refer to subjects which ought, one
would hope, to lead hereafter towards much completer insight into
earth-crust state, but at present they only raise, without gratifying
our hopes. The possible connection of these with secular oscillations
of land and sea is necessarily dismissed with no more than a re-
ference to the possibility. Materials do not exist for anything fuller.

Readers may from time to time be conscious that what they are
reading is somewhat familiar, that they have met with the account
or seen the figure in some not very ancient paper, number, or
volume. Ample defence, were defence necessary, would be that
such a conspectus of knowledge must, from the nature of the case,
be largely a compilation. But there is another reason. It was said
once: ‘None but himself can be his parallel.’ Prof. Milne might
almost say that none but himself could be his authority. Those
most interesting notes on the results of Japanese observations that
have from time to time appeared in “ Nature,” are to a large extent
abstracts of papers from the Seismological Society’s Journal. Prof.
Milne could find scarce any store worth pillaging except the
productions of his own creation. . EH. H. (Cams.).

I1].—Conrrisutions to Ammrtcan Patmontotogy. Vol. i. No. 1.
Published by E. O. Ulrich, Cincinnati, 1886. 8vo. pp. 385, pls.
1—3.

CCORDING to Mr. Ulrich’s experience, the learned societies of

America are inadequate to the needs of the Paleontologist, since

if they accept papers, they are unable or unwilling to furnish the

necessary illustrations, and he therefore intends to make himself

independent by bringing out, from time to time, a series of what are

pores ‘private publications,” of which the present number is the
rst.

It contains descriptions of “ New Silurian and Devonian Fossils,”
for the most part Bryozoa. A fresh classification, to replace one
brought forward by the author in 1882, is proposed for the families
Fenestellidee and Acanthocladide. In the former, three new genera
are introduced, but they are left without names; there is no descrip-
tion of any type species ; and their essential characters appear to be
extremely slight.

Descriptions and figures are given of a number of new species
belonging to the genera Fenestella, Semicoscinium, Unitrypa, Polypora,
Fistulipora and Eridopora in addition to two new genera, Buscopora
and Lichenotrypa.

The author bases a new genus of Brachiopoda, named Schizobolus,
on the internal characters of Discina truncata, Hall. The generic
affinities are stated to “appear to lie between the Obolide on the
one side and the Discinide on the other; the dorsal valve is not
unlike that of Discina, whilst the whole shell resembles Discinisca,

Reports and Proceedings—Geological Society of London. 375

Dall.” The author describes the specific characters in detail, but
fails to point out those which should mark the proposed genus from
its nearest allies.

A new species of, Rhynchonella is founded on specimens showing
casts of the interior, and a new species of Gypidia is described.
Several new species of Platyceras, a new genus of corals, Bucano-
phyllum, and new species of Strombodes and Labechia are introduced
and figured. Finally a new genus of Foraminifera named Moellerina
is based on some minute orbicular bodies with spiral ridges on the
outer surface. It seems to have escaped the notice of the author that
these bodies have been already described and figured by Professor
Dawson, as Saccammina (Calcisphera) Eriana, and that they were
previously mentioned by Prof. Meek as probably the fruits of Chara.

ISI POIs) /NAN(ID, 2S054O\SCn aI DAMN Re S-

—-——__
GrotogicaL Society oF Lonpon.

I.—June 23, 1886.—Prof. J. W. Judd, F.R.S., President, in the
Chair.—The following communications were read :

1. “On some Perched Blocks and associated Phenomena.” By
Prof. T. McKenny Hughes, M.A., F.G.S.

The author described certain groups of boulders which occurred
on pedestals of limestone rising from 3 to 18 inches above the level
of the surrounding rock. The surfaces of these pedestals were
striated in the direction of the main ice-flow of the district, while
the surrounding lower rock in no case bore traces of glaciation, but
showed what is known as a weathered surface.

He inferred that the pedestals were portions of the rock protected
by the overhanging boulder from the down-pouring rain, which had
removed the surrounding exposed parts of the surface. When the
pedestals attained a certain height relatively to the surrounding rock,
the rain would beat in under the boulder, and thus there was a
natural limit to their possible height.

He referred to the action of vegetation in assisting the decompo-
sition of the limestone, and considered that there were so many
causes of different rates of waste and so many sources of error, that
he distrusted any numerical estimate of the time during which the
surrounding limestone had been exposed to denudation.

Considering the mode of transport of the boulders, he thought that
they could not have been carried by marine currents and coast-ice,
as they had all travelled, in the direction of the furrows on the rock
below them, from the parent rock on the north. Moreover, marine
currents would have destroyed the glaciation of the rock and filled
the hollows with débris. .

Furthermore, the boulders and striz are found in the same district
at such very different levels and in such positions as to preclude the
possibility of their being due to icebergs.

Nor could the boulders represent the remainder of a mass of drift
which had been removed by denudation, for the following reasons :—

376 Reports and Proceedings—

1. They were all composed of one rock, and that invariably a rock
to be found in place close by.

2. Any denudation which could have removed the clay and
smaller stones of the drift would have obliterated the traces of
glaciation on the surface of the rock.

3. The boulder which had’ protected the fine glacial markings
below it from the action of the rains would certainly in some cases
have preserved a portion of the stiff Boulder-clay.

4. The margin of the Boulder-clay along the flanks of Ingle-
borough was generally marked by lines of swallow-holes, into
which the water ran off the Boulder-clay ; and when the impervious
beds overlying the limestone had been cut back by denudation, a
number of lines of swallow-holes marked the successive stages in
the process; but there was not such evidence of the former extension
of the drift up to the Norber boulders.

d. The boulders themselves were not rounded and glaciated in the
same way as the masses of the same rock in the drift, but resembled
the pieces now seen broken out by weathering along the outcrop of
the rock close by.

Having thus shown the improbability of these boulders having
been let down out of a mass of drift the finer part of which had
been removed by denudation, or of their having been masses floated
to their present position on shore-ice, he offered an explanation of
their peculiar position, which he thought was not inconsistent with
the view that they belong to some part of the age of land-ice.

That they were to be referred to some exceptional local circum-
stances seemed clear from the rarity of such glaciated pedestals,
while boulders and other traces of glaciation were universal over
that part of the country. He therefore pointed out in explanation,
that they occurred always where there was a great obstacle in the
path of the ice:—at Cunswick the mass of Kendal Fell curving
round at the south and across the path of the ice; at Farleton the
great limestone escarpment rising abruptly from Crooklands; at
Norber the constriction of the Crummack valley near Wharfe and the
great mass of Austwich grit running obliquely across its mouth. In
all these cases the ice had to force its way up hill; and there would
be a time when it would just surmount the obstacle after a season of
greater snowfall, and fall back after warm seasons, until it fell back
altogether from that part. During the season of recession, boulders
would be detached below the ice-foot; during the seasons of advance
they would be pushed forward; and in those exceptional localities
of isolated hills from which the drainage from higher ground was
cut off, the boulders were left on a clean furrowed surface of lime-
stone, which was then acted upon by rain-water and the vegetation,
except where protected by the boulders.

2. “On some Derived Fragments in the Longmynd and Newer
Archean Rocks of Shropshire.” By Dr. Charles Callaway, F.G.S.

Further evidence was added to that given in the author’s previous
paper (Q.J.G.S. 1879, p. 661), to show that the Longmynd rocks
of Shropshire were chiefly composed of materials derived from the

Geological Society of London. Ore

Uriconian series, and that the Uriconian series itself (Newer
Archean) was partly formed from the waste of pre-existing rocks.
This evidence consisted of (1) the presence, throughout the greatly
developed Longmynd conglomerates and grits, of purple rhyolite
fragments, recognized by microscopical characters as identical with
the Uriconian rhyolites of the Wrekin, and the occurrence of grains,
probably derived from the same rhyolites, in the typical green slates
of the Longmynd; and (2) the existence of conglomerate beds con-
taining rounded fragments of granitoid rock in the core of the
Wrekin itself, whilst the Uriconian beds of other localities, and
especially those of Charlton Hill, contained waterworn pebbles,
chiefly metamorphic. These pebbles appeared to have been derived
from metamorphic rocks of three distinct types. The views put
forward were founded on microscopical evidence, of which some
details were given in the paper, and were supported by the views
of Professor Bonney, who had furnished notes on the microscopical
characters of the rocks.

3. “Notes on the Relations of the Lincolnshire Carstone.” By
A. Strahan, Esq., M.A., F.G.S.

The Lincolnshire Carstone has hitherto been supposed to be
correlative with the upper part of the Speeton series, and to be quite
unconformably overlain by the Red Chalk (Quart. Journ. Geol. Soc.
vol. xxvi. p. 326-347). But the overlap of the Carstone by the
Red Chalk, which seemed to favour this view, is due to the northerly
attenuation, which is shared by nearly all the Secondary rocks of
Lincolnshire. Moreover, the Carstone rests on different members
of the Tealby group, and presents a strong contrast to them in litho-
logical character, and in being, except for the derived fauna, entirely
unfossiliferous. It is composed of such materials as would result
from the “ washing” of the Tealby beds.

In general it is a reddish-brown grit, made up of small quartz-
grains, flakes and spherical grains of iron-oxide, with rolled phos-
phatic nodules. Towards the south, where it is thick, the nodules
are small and sporadic. Northwards, as the Carstone loses in
thickness, they increase in size and abundance, so as to form a
“ coprolite-bed,” and have yielded specimens of Ammonites speetonensis,
A. plicomphalus, Lucina, etc. When the Carstone finally thins out,
the conglomerate character invades the Red Chalk, similar nodules
being then found in this rock.

The presence of these nodules, with Neocomian species, taken in
connexion with the character of the materials of the Carstone, points
to considerable erosion of the Tealby beds. On the other hand,
there is a passage from the Carstone up into the Red Chalk. It
would seem, then, that the Carstone should be regarded as a “ base-
ment-bed” of the Upper Cretaceous rocks.

The Lincolnshire Carstone is probably equivalent to the whole of
the Hunstanton Neocomian, the impersistent clay of the latter being
a very improbable representative of the Tealby Clay. It therefore
follows that the whole Speeton series is absent in Norfolk, and also
in Bedfordshire. The unconformity at the base of the Carstone

378 Reports and Proceedings—

becomes greater southwards, and the nodules have been derived
from older rocks. Similarly north of Lincolnshire, where the Spee-
ton series is overlapped, the nodules in the Red Chalk, marking the
horizon of the Carstone, have been derived from Oolitic rocks.

In the South of England it would seem that equivalents of the
Speeton series reappear. The Atherfield clay contains an indigenous
Upper Speeton fauna, while a pebble-bed near the base of the Folke-
stone beds is described by Mr. Meyer as containing derived Oolitic
pebbles, and being probably the representative of the Upware de-
posit, and presumably, therefore, also of the Lincolnshire Carstone.

4. “The Geology of Cape-Breton Island, Nova Scotia.” By Edwin
Gilpin, Esq., Jun., A.M., F.R.S.C., Inspector H.M.’s Mines.

After referring to previously published descriptions of Cape Breton
geology, the author stated that the various formations found in the
island had been thus classified by the officers of the Geological
Survey :—

The Felsite series.

BesCiuibuig (Ceseauiim), uclvding, The Crystalline Limestone series.

Lower Silurian, —- ( Lower Coal-formation.
Devonian. | ;Gypsiferous series.
Carboniferous, including< (Limestones, ete.

| Millstone-Grit.
Middle Coal-formation.

He then proceeded to give an account of each system and its sub-
divisions in order, commencing with the most ancient and adding a
few detailed sections of the rocks belonging to some of the principal
series. He described the distribution and relations of the several
divisions.

The paper concluded with a few notes on the superficial geology
of the island. There is a general absence of moraines and of the
fossiliferous Post-Pliocene marine clays of the Lower St. Lawrence.
The older beds are generally exposed, but deeper soils and deposits
with erratic boulders are found overlying the Carboniferous beds.
Marks of recent ice-action are found on the shores of some of the
lakes, and are due to the ice being driven by the wind.

5. “On the Decapod Crustaceans of the Oxford Clay.” By James
Carter, Esq., F'.G.S., ete.

The author commented on the paucity of these fossils as indicated
in British lists, only three or four species having hitherto been
recorded.

The discovery of considerable numbers of Decapod Crustaceans
in the Oxford Clay of St. Ives has enabled the author to increase
the list materially. Many have been collected by Mr. George, of
Northampton. These fossils occur in the clay immediately beneath
the St. Ives rock, and therefore presumably in the uppermost zone
of the Oxford Clay. Many of the specimens are more or less
mutilated, but some fifteen or sixteen distinct species have been
made out. None of these have been recorded as British except
Eryma Babeaui, mentioned by Mr. Etheridge as having been found in

Geological Society of London. BYES)

the Kimmeridge Clay. Seven species are identified as foreign forms,
and seven are new to science. They are distributed as follows :—

INYO bo cod, oe, to species.
ERY ING Wyerolsssiekessi less ws OL OLLGh lls
CHYVOWAB end G0 oe con ”
JUTE: G80 ona B00) Cod A OVS 1 cp
MMARDEVGFUB: “ooo c00. obo 2 5p
Gonvochorus- 0 te oe 55
Undetermined... ... ... 8 5p

Nearly all the forms belong to the type of the Macrura, the Bra-
chyura being doubtfully, if at all, represented.

6. “Some Well-sections in Middlesex.” By W. Whitaker, Esq.,
B.A. Lond., F.G.S.

Accounts of many well-sections and borings having been received
since the publication of vol. iv. of the Geol. Survey Memoirs, the
author now gave more or less detailed descriptions of fifty-six of
these, all in the Metropolitan county, and all either unfinished or,
in a few cases, with further information as to published sections.
The depths range from 59 to 700 feet, more than half being 800 feet
or more deep. Nearly all pass through the Tertiary beds into the
Chalk, and most have been carried some way into the latter. Papers
descriptive of like sections in Essex, Herts, and Surrey have been
sent to Societies in these counties.

7. “On some Cupriferous Shales in the Province of Houpeh,
China.” By H. M. Becher, Esq., F.G.S.

This communication contained some geological observations made
during a visit to a locality on the Yangtse river, near I-chang, about
1000 miles from the sea, for the purpose of examining a spot whence
copper-ore (impure oxide with some carbonate and sulphide) had
been procured.

The principal formations in the neighbourhood of I-chang were
said to be Palzeozoic (probably Carboniferous) limestones of great
thickness, overlain by brecciated calcareous conglomerate and reddish
sandstones, which form low hills in the immediate vicinity of the
city. About fifty miles further west the limestones pass under a
great shale-series with beds of coal, the relations of which to the
sandstones are not clearly ascertained.

The copper-ore examined by the writer came from the shales,
which contained films and specks of malachite and chrysocolla, and
in places a siliceous band containing cuprite, besides the oxydized
minerals, was interstratified in the beds. Occasionally larger masses
of pure copper-ore are found imbedded in the strata. The ground
had not been sufficiently explored for the value of the deposits to
be ascertained.

8. “The Cascade Anthracitic Coal-fields of the Rocky Mountains,
Canada.” By W. Hamilton Merritt, Esq., F.G.S.

The coal-field named occurs in the most eastern valley of the
Rocky Mountains, that of the Bow river, and, like other coal-fields
of the country, consists of Cretaceous rocks, which lie in a synclinal
trough at an elevation of about 4300 feet above the sea. The under-
lying beds, of Lower Carboniferous or, possibly, Devonian age, rise
into ranges 3000 feet higher.

380 Reports and Proceedings—Geological Society of London.

Further to the eastward the Jurassic and Cretaceous coal contains
a large percentage of hygroscopic water and volatile combustible
matter, and has the mineral composition of lignite. The average
composition is :—

Fixed carbon ste) cee see cee cen ve cos 42 per Cent.
Volatile combustible matter... 0. <6. ccce sce. 84 455
iver oscopic water san uych scasbeesy aces cecuueeemeM ORL nis
ANS 5 a6 elasOk) 55
—100

As the mountains are approached, the amount of hygroscopic water
is found to diminish by about one per cent. for every ten miles, and
fifteen miles from the range the percentage is about five. In the
foot-hills the lignites pass into a true coal, with 1-63 to 6-12 per cent.
of hygroscopic water, and 50 to 63 per cent. of fixed carbon. In the
Cascade-river Coal-field the average character of the coal is that of
a semianthracite, with the following composition :—

Hixed canbonsy ic. a is-speccpeieccbere, qerctiacen SOR percents
Volatile combustible matter esx Picith gsestimeson LOCUS

)

Hysgroscopic water Santis, dice: (acne US eng
STIGNN SEONG eo Urs SiG ES RAUL: dee MOOT ae
100-00

The coal-seams have been subjected to great pressure, and the
change in the quality of the coal appears to be due to metamorphic
influence.

9. “On a new Emydine Chelonian from the Pliocene of India.”
By R. Lydekker, Esq., B.A., F.G.S.

The author described the shell of an Emydine Tortoise from the
Siwaliks of Perim Island, Gulf of Cambay, which he regarded as
decidedly distinct from any of the previously-described Siwalik
species, and proposed to refer to the genus Clemmys, with the name
of C. Watsoni, in compliment to the donor of the specimen.

10. “‘On certain Eocene Formations of Western Servia.” By Dr.
A. B. Griffiths, F.R.S.E., F.C.S. Communicated by the President.

A great thickness of paper-shales containing paraffin occurs near
the river Golabara; these extend over 30 square miles of country.
Small beds of clay with rock-salt are also found: the whole is said
to resemble the paraffin and salt districts of Galicia. The paraffin
shale is free from bituminous impurities. It contains :—

Baraiiin waxigcs) cet lepeie.carl esneveuw cis pate pL >Spenicents
WEIR OF COMO 45 oo ooo ors on oo SU 5
Ammonia Hels” aBS)) eeeehcl eee qlee ¥ ose Cask eh eta MLO | ta
The mineral constituents of the shale are :—
Alumina p09 600 30a ps8 on onc) FSIS) arse eh
Tron oxide : derich of 20 he
Magnesia... 260 eites
aie serene. eeee tte LOT Nats
Potash: (at ROR es, EE TR REE a
OGaPSSIAtT.uiMens, jl eeath cee wns Be ceede: GM tieeed bean) LOLAIepi eR
Silica EE, hice cd Wicsen Stesaytvese coca ieee Mase) Mice OOOO INEa En
MOSS: sing shee g asp pcak eas woos WA Sessy kere 004 =~,

100-00

Correspondence—Mr. A. G. Cameron. 381

The brown coal of the neighbourhood, whose natural distillation
has most probably ee the 1 hydrocarbon in the shales, contains :—

Carbone ccc) ce Pen ower atcecl ll deceit estat OvAaperacelts

HET ATO ONY veep sayy) was fhe seal Feed pees ecel tried poetry GLE weg

Wiateracomibinediy i sacl aosn ueccat bese ake ate eae aves 8 (le Deienas

Water, Iy OTOSCOPICieacwil- seu itsssie eset acolaeeeun LL OONe uss
100:00

The beds containing these coals have been invaded by eruptive
porphyry and trachytic rocks, of which the former contains 754 and
the latter 61 per cent. of silica.

The clays from which the shales were originally formed contain
abundance of marine Diatomaces and Foraminifera (chiefly Num-
mulites), as also species of Ostrea, Cyrena, Cerithium, Voluta, and
Nautilus, together with the remains of Placoid and Teleostean fishes.

CORRESPONDENCE.

>.

WATER-BEARING NODULES IN THE LOWER GREENSANDS.

Sir,—The brilliant and varied colouring of the Lower Greensands
at the Great Northern Railway at Sandy Junction, and at Flitwick
Station on the Midland line, must be familar to every one who has
travelled those districts. At Sandy, the cutting is a deep one and
nearly all in clean sand, varying through shades of green, grey
and yellow, the yellow predominating, to almost pure white. At
Flitwick, the colouring is still more varied; beautifully tinted bands
of a fleshy pink or salmon tint, merging into violet, appear near
the bottom of the pit from which Mr. Franklin, of Bedford, obtains
his sand. The parti-coloured bands are more numerous at this place
than I recollect seeing elsewhere in Bedfordshire, although the white
and yellow sand at Heath and Reach, makes very picturesque open-
ings amongst the woods and ferns. The sands at Flitwick remind
one of the assemblage of colours met with in the sands,! from which
the well-known sand pictures are made in the Isle of Wight.

But besides the varied colouring, ironstone nodules, associated
with hard lumps of ferruginous rock, like the carstone quarried at
Snettisham in Norfolk, are very general in the Greensand. Being
of all shapes and sizes and in every stage of growth, they are
curious to look upon, and still more interesting to crack for the
fossils and sparry crystals that are sometimes found inside them.
An abundance of these concretions occurs both at Sandy and Flitwick,
some spherical, others tabular, and many other forms.

With Rhodes, the fossil collector, I have lately obtained a number
of these nodules from Flitwick,? some of which, for description sake,
and from the fact of their having water in them, I have designated
water-bearing nodules. ‘These are readily distinguished from others
inclosing phosphatized fossils (principally the internal casts of some

1 Bagshot Sands.
2 From the peat at Flitwick I picked out, last year, a small flint implement.

382 Correspondence—Prof. J. W. Judd.

species of oyster), by being audibly full of water when shaken.
Many contain only sand, lime or earthy matter, perhaps the residue
of fossils destroyed.

Collecting the water-bearing nodules is somewhat akin to choosing
cocoa-nuts at the greengrocer’s. We pick up one after the other from
the ground, rejecting the light ones, and those that give forth no
sound, in favour of those which, like the cocoa-nuts with milk, bear
unmistakeable evidence of containing liquid.

What the nature of this liquid may be,' or what duration of time
has elapsed since it was sealed up in these portable reservoirs, is not
for me at present to say, having as yet made no minute examination.
The specimens contained water when we picked them up, as did
others when split with the hammer. Since bringing them home,
they have been in a warm room, and the water from some reason,
probably increased temperature, has evaporated or disappeared. The
iron pan which forms the walls of the cavity may be porous,
and I have placed them in a vessel of water, expecting them to
become water-bearing nodules again; the phenomenon would then be
probably explained, by supposing that during periods of wet these
nodules absorb the water percolating through the Greensand.

It then becomes a question whether these nodules may not be
a cause of diminution in the water supply ? in districts where they
are largely developed. But against the absorption theory, remains
the fact that the weather was very warm and fine when the nodules
were gathered, and the recent heavy rains had not set in.”

A. G. Cameron,
BEDFORD. H. M. Geological Survey.

ON THE TERM NEOCOMIAN.

Sir,—In writing his article upon the above subject, in the last
Number of the Grotocican Magazine, my friend Mr. Jukes-Browne
appears to have been labouring under a curious and very unfortunate
misconception, He says :—

“For many years English geologists were content with the nomen-
clature employed by the earlier students of the Cretaceous system—
Webster, Murchison, Mantell and Fitton. In 1864, however, the
French term Neocomian was introduced by Prof. Judd, who adopted
it for the Cretaceous portion of the Speeton Clay, and Sir Charles
Lyell subsequently used it as a synonym for the whole Lower
Cretaceous series in England, as distinct from the Upper Cretaceous
series or the beds lying above the Lower Greensand.”

Through the whole of the following pages, the writer of the article
enlarges upon this text, treating myself as responsible for the error,

1 Since writing the above, it has been suggested to me that an analysis of the
water might be made. This would of course be a valuable guide to the source of
supply.— A. G. C.

* For a description of the mode of formation of the ironstone concretions, see
Penning, Grou. Maa. Dec. II. Vol. III. p. 218. Geology of Cambridge, Geolo-
gical Survey Memoir, p. 12, Penning and Jukes-Browne.

Correspondence—Prof. J. W. Judd. 083

as he regards it, of introducing the term Neocomian into English
geological literature.

Now what are the real facts of the case? For the last forty or
fifty years the term Neocomian has been quite commonly applied, by
many eminent English geologists, to a part or to the whole of
the Lower Greensand, and even those who are prepared to credit
me with the most phenomenal precocity, could scarcely charge
me with leading astray my fathers in science so long ago as that.
The author who had the chief honour, as I esteem it, of introducing
the term to English science was the late Mr. R. A. C. Godwin-
Austen, and his practice dates at least as far back as the year 1843.
If my friend Mr. Jukes-Browne will refer to several memoirs by
that author—such as those ‘‘On the Geology of the South-East
of Surrey” (Proc. Geol. Soc. vol. iv. (1848), pp. 167-173,
196-198) ; “On the Age and Position of the Fossiliferous Sands
and Gravels of Farringdon” (Quart. Journ. Geol. Soc. vol. vi.
(1851), pp. 454-478); and “On the Possible Extension of
the Coal-measures beneath the South-Hastern part of Hngland”
(Quart. Journ. Geol. Soc. vol. xii. (1856), pp. 88-73)—he will find
that Mr. Austen not only uniformly employs the term Neocomian
for a part at least of the Lower Greensand, but that he defends
his practice by some very judicious and cogent arguments. If
the writer of the article will look through the contemporary
geological literature in this country, he will also find that the
example of Mr. Godwin-Austen was followed by other geologists of
high reputation.

Of course Mr. Godwin-Austen—who happened to have a remark-
ably extensive acquaintance with continental geology—was well aware
of the fact referred to by Mr. Jukes-Browne, that at Neuchatel there is
no exact representative of our Lower Greensand; but Mr. Godwin-
Austen’s arguments, based on the fact that the fossils of our English
formation (or at least of the lower part of it) are very similar to
those of the Neocomian, while they are on the whole very different
from those of the Upper Cretaceous, have always seemed to me to
be worthy of the most careful consideration ; and many other geolo-
gists, I find, have acknowledged their weight by following his
example.

My own part in connection with this question was very different
from what my friend supposes; it consisted in describing a series
of strata, in Lincolnshire and Yorkshire, which are for the most part
older than the Lower Greensand, and correspond in age with strata
on the Continent which all geologists, including Mr. Jukes-Browne,
agree in calling Neocomian. At the same time, as I have already
stated in a paper in this Journal (Gzox. Mae. Vol. VII. 1870, p. 220),
J have always regarded Mr. Godwin-Austen’s proposal to extend
the use of the term as originally defined, so as to include the English
Lower Greensand, to be much more logical and defensible than that
of M. D’Orbigny—which was to restrict the name to one part of
the series.

Considering, as I do, the Neocomian to be a great continuous

384 The New Zealand Volcanic Outburst.

system of strata, with no very important breaks in it, the conven-
tional limits which are to be adopted for the Upper, Middle and
Lower divisions, respectively, appear to me to be a question of by
no means great importance. At the same time, any attempt to
disturb, without very good cause shown, names which have come
into general use, or to alter the definition of terms which have been
generally accepted—-whether the attempt be made by officers of the
Geological Survey, in their individual or their corporate capacity—-
will, I strongly suspect, prove a hopeless, as I am sure that it is a
useless, task. Consequently, I trust the idea of “ formulating a new
nomenclature” as the result of “the revision by the members of
the Geological Survey” of the Cretaceous rocks of England, is one
that will, in moments of calmer reflection, be abandoned. Scientific
names go through a “‘ struggle for existence,” and the fittest survive.
I trust my friend Mr. Jukes-Browne will draw a moral from the
fact, that the name Neocomian has shown a very considerably greater
vitality than he seems to have suspected.

But while Mr. Jukes-Browne gives me credit for that of which I
cannot possibly accept the honour, he himself assumes a respon-
sibility which, it seems to me, he is not called upon to bear. In
speaking of “the merits of the name (Vectian) which I have already
proposed as a substitute for Lower Greensand,” he must surely have
forgotten a well-known passage in the works of Dr. Fitton. After
remarking that he had long since stated his objections to the use of the
term Lower Greensand, that author writes as follows :—“ If here-
after a change be thought desirable, he conceives that the new
denomination should be taken from the Isle of Wight, where this
portion of the sub-cretaceous groups was first distinguished, and
where the sections on the coast are remarkable for their distinctness ;
and if such a case should arise, he suggests the name Vectine for the
strata now called Lower Green Sand, from the ancient name of that
island,—Insula Vectis of the Romans” (Quart. Journ. Geol. Soe.
1845, vol. i. p. 189).

As the paper in which this passage occurs was read in 1844 and
published in 1845, it seems to me scarcely more likely that Mr.
Jukes-Browne could have offered useful hints on the subject to Fitton
than that I was engaged in a previous year in improperly influencing
Godwin-Austen. Joun W. Jupp.

Eruption oF Mount Tarawera, North Istanp, New ZEALAND.
—A most destructive volcanic outburst occurred on the night of the 9th of June,
from Tarawera, a mountain not more than 3000 feet high, which rises near the lake
of the same name, and about nine miles from Rotomahana. At two o’clock a shock
of greater violence occurred followed by a terrific roar, a pillar of light shot up from
the summit of Tarawera, molten lava and hot mud were rained abroad, while huge
rocks were thrown up and around in all directions. Showers of hot cinders and
boiling mud covered the settlement of Wairoa, killing on the spot or burying alive
numbers of persons. For sixty miles the destruction has spread. About 100 persons
have perished, whilst villages and settlements are covered with eight or ten feet of
mud or ashes. We hope to give a fuller account in our next number.

Geol. Mag. 1886. Decade Il Vel: Ik Pro

s

C.Berjeau del etlith. West,Newman & Co. amp.

To illustrate M’ Tomes's paper.

THE

GEOLOGICAL MAGAZINE.

NEWinSERIES., DECADE: Ul VOR I:

No. IX.—SEPTEMBER, 1886.

(Qa gwlE AEN WA NaS aka CAa ahs)
——_—

T.—On Some New or Imperrectty Known MaApRreEpoRARIA FROM
THE INFERIOR OOLITE OF OXFORDSHIRE, GLOUCESTERSHIRE AND
DorsETsHIRE,

By Rozert F. Tomes, Esq.

(PLATE X.)

die the thirty-eighth volume of the Quarterly Journal of the
Geological Society is a paper by me on the Corals of the
Inferior Oolite, and in the following volume is one on the Corals
of the Great Oolite. The forty-first volume of the same periodical
contains a supplement to the latter, but to the former no such
addition has yet been made. The present communication makes
good that deficiency, and is a supplement to it. It contains, besides
the description of some new species, additional remarks on others
already known, mention of genera about which doubt has been ex-
pressed, and the description of one which I consider new. Another
genus, Stephanocenia, though well known elsewhere, has up to the
present time remained unrecognized as British, and is now introduced
on the evidence of two well-marked species from the Inferior Oolite
of Gloucestershire. The addition to our Coral fauna of such genera
as the above, and of others equally well known which I have also
had the opportunity of making known, is of even greater interest
than the discovery of new genera and species. Epismilia, Donaco-
smilia, Cyathophyllia, Adelastrea, Stylosmilia, Rhizangia, Thecoseris,
Leptophyllia, and Enallohelia, form a valuable contribution towards
the Coral fauna of this country.

Three papers on Fossil Madreporaria have lately appeared from
the pen of Professor Duncan, two of which are professedly criticisms
on my own communications on the same subject. The title of the
first is, ‘On the Astroccenia of the Sutton Stone and other Deposits
of the Infra Lias of South Wales.”

That of the second is, “‘ On the Structure and Classificatory Position
of some Madreporaria from the Secondary Strata of England and
South Wales.” Both these were read at the meeting of the Geological
Society on the 4th November, 1885, and appeared in full in the
Journal of the 1st of February, 1886. The third paper appears in
the February Number of the Gxonogroan Macazine for the present
year.

Of the first of these I have only at present to say that it is
deserving of consideration, because it is based on the examination
of authentic specimens, though whether the conclusions sought to be

DECADE IlI.—VOL, MI,—NO. IX. 25

386 R. F. Tomes—Inferior Oolite Madreporaria.

maintained are substantiated is yet open to question. The purpose
of the paper is to re-assert what I have objected to, namely, that the
distant and cylindrical corallites of such compound and compact corals
from the Sutton Stone and neighbouring conglomerates as have
columellz have become cylindrical by matter added to the walls them-
selves, and not by the interposition of true coonenchyma, as in Stylina
and other allied genera. To this I shall refer on some future occasion.
Professor Duncan’s third paper is an answer to one of mine on some
Cretaceous Madreporaria, and the consideration of it may also remain
over until another opportunity. But the second paper, as it relates
principally to Oolitic genera and species, may be here discussed.
I have not, however, the remotest intention of entering into a con-
troversy on the many, points on which Professor Duncan and I
entertain opposite opinions. Controversy, when carried to the length
it sometimes is, embarrasses the editor, is offensive to the reader, and
lowers the tone of the periodical in which it appears—a consummation
much to be regretted. With every wish, however, to avoid such an
occurrence, ] must claim the privilege of making known the con-
clusions to which my investigations have brought me, and of re-
asserting or modifying from time to time, if I have good reason for
doing so, any statement I may have made. But while doing this, it
will be my most earnest wish to avoid the occurrence of anything
which may seem captious or discourteous.

A great many of the objections raised by Professor Duncan against
my several papers on the Madreporaria of our Secondary formations
refer to mere matters of oversight, and as they do not affect the con-
clusions arrived at, are of little importance. They might prove
useful on some future occasion in making corrections, were the
papers to re-appear in a collective form. Objections of another kind
take the form of direct and unsupported contradiction of facts, and
there are again, some, which, from their very nature, and for the
author’s own sake, should be allowed to pass unnoticed. But such
statements as affect the definition of genera and the determination of
species, and have therefore a more legitimate bearing on the subject
in hand, will receive due attention in their proper place.

A collection of specimens from the Inferior Oolite of Dorsetshire
has lately been placed in my hands by Mr. Buckman, and these with
others kindly supplied by Mr. Hudleston, with the addition of a
collection made by me during a recent visit to the same district,
have afforded me the long-wished-for opportunity of comparing the
Dorsetshire and Somersetshire species with those from the counties
of Oxford and Gloucester. A list of the Dorsetshire species will be
given further on.

Diligent search has been made for Corals in the lowest beds of the
Inferior Oolite at Crickley Hill, Leckhampton Hill, Cleeve Hill,
and Frocester Hill, in consequence of the species already found
in them having differed so materially from those in the more
clearly defined coralliferous deposit overlying the Pisolite. They
are, besides, interesting as being the earliest representatives of
Madreporaria in the Oolitic formation, differing greatly in their facies

R. F. Tomes—Inferior Oolite Madreporaria. 387

from the few small corals which are found in the Upper Lias, though
not nearly so much from those species which occur in the under-
lying Marlstone. The following are such as have up to this time
been taken from the Pisolite, and the beds below it.

MontiivaLt1a conctnna.—Pisolite at Crickley and Leckhampton,
and in the broken-up bottom beds at Huddiknoll, near the
Horsepools, Gloucester.

MontTLivaLTIa CUPULIFORMIS.—Beds under the Pisolite, Crickley.

MontiivaLtia DE LA BecuEer.—Bed under the equivalent of the
Pisolite, Frocester Hill.

Montirvattia Lens.—Beds under the Pisolite at Leckhampton
and Crickley, and in the beds overlying the Upper Lias sands,
Dover’s Hill, Chipping Campden.

IsasTR#A, an undetermined species.—Bed under Pisolite, Crickley.

_ CHorisastR#A, sp.—Pisolite, Crickley, and the bed overlying the
Upper Lias sands, Dover’s Hill, Chipping Campden.

THAMNASTRHA, Sp.—Pisolite, Crickley.

THAMNASTRHA, Sp.—Bed overlying the Upper Lias Sands, Dover’s
Hill, Chipping Campden.

OrosEris Ootrtica.—Bed under the Pisolite, Crickley.

CoMOSERIS VERMICULARIS.—Pisolite ? Crickley.

Several of the above are either undeterminable or have already
been passed under review, but mention will hereafter be made of some
of them in the notes on the species.

Mr. Witchell, in his valuable work on the Geology of Stroud,
records the occurrence of a Coral-bed resting on the Upper Trigonia
Grit. The position being wholly at variance with that assigned to
the Upper Coral-bed near Cheltenham by the late Dr. Wright, I
have recently visited Stroud, and, under the guidance of Mr. Witchell,
have examined one of the sections mentioned by him—the Stroud
Hill section. The result has been the full confirmation of his
opinion, that there are four coralliferous deposits in the Inferior
Oolite of Gloucestershire, instead of three as stated by the late Dr.
Wright. The Coral-bed exposed in Worden’s quarry in the Slad
Valley, Stroud, though supposed by Dr. Wright to correspond with
the upper one near Cheltenham, is really of more recent date, and is
indeed the same as the one in the Rodborough Hill and Stroud Hill
sections. The position of these four coralliferous layers in the Inferior
Oolite of Gloucestershire may be defined as follows :—

1. The Upper Coral Bed.—Occurs in the upper part of the Upper Trigonia Grit,
and is exposed at Rodborough Hill, Stroud Hill, and in the Slad Valley, near
Stroud.

2. The Second Coral Bed.—Lies in the bottom of the Lower Trigonia Grit, andis_ .
exposed at Cleeve Hill, Leckhampton Hill, Ravensgate Hill, Brown’s Hill near
Seven Springs, Juniper Hill near Painswick, and at Birdlip, all localities in
the Cheltenham district.

3. The Third Coral Bed. — Lies in the Oolite Marl at Birdlip Hill, Leckhamp-
ton Hill, Juniper Hill, and at Notgrove on the Cheltenham and Chipping
Norton Railway.

4. The Fourth Coral Bed.—Lies directly upon the Pisolite, and is well exposed
at Crickley Hill, Birdlip Hill, Sheepscombe, the Horsepools, at Huddiknoll,
and at Juniper Hill near Painswick. It is absent at Cleeve Hill and at the
Leckhampton and Frocester Hills.

388 R. F. Tomes—Inferior Oolite Madreporaria.

The Corals of Beds 2, 3 and 4 have already received attention, but
those of Bed No. 1, have not been made known. It appears, how-
ever, to be very poor in species, only three having as yet been noted.
They are, Isastrea tenuistriata, Isastrea sp. undetermined, and
Thamnastrea sp. undetermined.

The following are the species from the Inferior Oolite of the
counties of Dorset and Somerset which I have met with up to the
present time, with their several localities, and, as far as determined,
their Ammonite zones.

Discocyathus Hudesi. Burton Bradstock, probably in the zone of
Ammonites Parkinsoni; Corton Denham, Somerset, in the zone of
Am. Murchisoni. |

Trochocyathus magnevillianus. Half-way house near Yeovil, in
the zone of Am. Parkinsoni ; under cliff, Burton Bradstock, probably
in the same zone; in the “Marl Bed” at Bradford Abbas, in the
bottom of the zone of Am. Parkinsoni.

Trochocyathus sp. A small conical species not yet determined,
obtained by Mr. 8. 8. Buckman from the Bradford Abbas quarry,
but the position not recorded.

Thecocyathus discus, E. de From. Burton Bradstock, the zone
not noted, but associated with specimens of Discocyathus Eudesi, which
were stated to have been taken from the zone of Am. Parkinsoni.

Thecocyathus, a species undetermined, obtained from the “ Marl
Bed” at Bradford Abbas by Mr. Buckman.

Montlivaltia lens. Bradford Abbas railway-cutting, in the zone of
Am. Murchisoni, immediately overlying the sands; Castle Cary Hill
in the zone of Am. Parkinsoni; Corton Denham, Somerset, in the
zone of Am. Murchisoni; and in the zone of Am. Sowerbyi, at
Bradford Abbas.

Monitlivaltia de la Bechet. Bradford Abbas railway-cutting, in the
zone of Am. Murchisoni; Drimpton near Broadwinsor, Dorset, in
the zone of Am. Parkinsoni ; Castle Cary Hill, Somerset, in the zone
of Am. Parkinsoni ; Bridport, the zone not noted.

Monitlivaltia tenuilamellosa. A single specimen has been sent to
me labelled Bradford Abbas, but it has more the appearance and
colour of Burton Bradstock specimens.

Montlivaltia cupuliformis. Bradford Abbas, in the paving-bed at
the top of the zone of Am. Murchisoni, where it is not uncommon.

Montlivaltia sp., undetermined, occurs with the last, and may
perhaps prove to be identical with it.

Tsastrea, sp. Notdeterminable. From the paving-bed at Bradford
Abbas.

Latimeandra Flemingi? A species very nearly allied to, or
identical with this, occurs in the paving-bed at Bradford Abbas, and
is remarkable from having a thick and wrinkled epitheca. !

? A compound coral having calices in shape like those of
an Isastreea, with confluent septa, and a columella, occurs at Bradford
Abbas, but the zone has not been determined.

Thecoseris polymorpha. Several small specimens referable to this
species have been taken from the paving-bed at Bradford Abbas,
and I have one from the Inferior Oolite at Stoford, Somerset.

R. F. Tomes—Inferior Oolite Madreporaria. 389

Leptophyllia, sp. (Podoseris constricta, Duncan). The type-specimen
of Podoseris constricta, which was for some time in my hands, has
so much the appearance of the Burton Bradstock specimens that I
have no doubt that it was obtained from that place. It is stated to
have come from the Lower Ragstone of Dorset, which I presume is
the zone of Am. Parkinsoni, the zone from which the other Burton
Bradstock Corals here mentioned have been obtained.

Thamnastrea Defranciana. A single example from the Inferior
Oolite of Dorset is in my collection, but I do not know either its zone
or exact locality.

Dimorphareu Oolitica, Duncan, sp. Occurs at East Coker, and is
common ; also at Stoford near Yeovil, in the zone of Am. Sowerbyi.

Dimorpharea Beanii (Cyclolites Beanti, Duncan). Occurs in the
paving-bed of the Bradford Abbas quarry, in the upper part of the
zone of Am. Murchisoni.

Dimorpharea expansa, n.s. East Coker, the zone not ascertained.

Microsolena, a small globular species. 'Two examples have been
met with, one from the paving-bed at Bradford Abbas, and the other,
although said to have been collected at the same place, has so much
the appearance and colour of the Burton Bradstock Corals as to
leave little doubt that it came from there.

The number of Turbinolide in the above list, occurring so low
down in the Inferior Oolite of Dorset and Somerset, is rather re-
markable, and would seem to indicate a continuous period from the
Upper Lias upwards, the conditions of which were favourable to the
growth of these small Madreporaria, and which did not prevail
during the formation of corresponding deposits in the Gloucester-
shire and Oxfordshire areas. The general resemblance between the
Turbinolide of the Upper Lias and those of the Inferior Oolite of the
Western Counties of England is very obvious.

The following section at present exposed in the quarry at Bradford
Abbas was taken by me a few months since, and although it does
not materially differ from those already given by Mr. 8. 8. Buckman *
and Mr. Hudleston,’ is repeated here for the purpose of showing all
the more correctly the position of the Corals in it.

ft. in.

1. Surface soil . SA rhe eat: Colic SAREE BOM marries slo
2. Shattered stone and rubble .. 3 6
3. Stone in nodular ee divided by ‘thin irregular layers ‘of marly

shale or ac 50 ac tr. sia, f£ 0
4, Soft stone ... 0 8
5. Marly shale; the “Marl bed” of §. §. Buckman. Contains

Tr ochocyathus magnevillianus .. 0 2
6, Gasteropoda bed, consisting of hard suberystalline stone, which is

thin and ragged and blue in the midile. It is overlain by a

soft friable layer. It contains Gasteropoda of great bapa!

and a considerable number of small sponges ... : @
7. Yellowish compact limestone 2 0

8. Paving-bed, containing the following corals : — Montlivaltia
cupuliformis, M. lens and another species undetermined,
Latimeandra Flemingi, a compound coral allied to Jsastraea,

1 Quart. Journ. Geol. Soc. vol. xxvi. p. 591.
2 Proceed. Geol. Assoc. 1885, p. 198.

390 R. F. Tomes—Inferior Oolite Madreporaria.
ft. in.
Thecoseris polymorpha, Dimorpharea Beanti, and a species
of Mierosolena ... 50 ac 300 ooe spe eo eas
9. Dewbed, forming the bottom of the quarry, and lying on the
Midford Sands. Depth not ascertained, more than ... Seam alae,
I now proceed to notice such species of corals from the Inferior
Oolite as appear to be either undescribed, new to this country, or
as demanding further remark.

THECOCYATHUS Discus. From. et Fer., Paléont. Franc. Polyp. Terr.
Jurass. p. 34, pl. 2, fig. 2.

I have received a specimen of this species said to have been
obtained from Bradford Abbas, but which, from its colour and litho-
logical condition, most likely comes from the same horizon and place
as a number of specimens of Discocyathus Eudesi, that is to say,
from Burton Bradstock.

EPiIsMILIA PORPITA, Tomes,
Montlivaltia porpita, Tomes, Quart. Journ. Geol. Soc. vol. xxxviii. p. 419, 1882.

The small Corals I described under the name of Monilivaltia porpita,
as having very peculiar septa, have proved, when some of their
septa were exposed by the removal of others, to have their sides
ornamented by tubercles instead of vertical ridges. These tubercles
are ranged in rows, which are parallel to the edge of the septa, and
when the latter have been worn down, the upper row on either side
comes close to the top, and the septa, which are in reality very thin,
are rendered thick and rugged by them. Until fully exposed, they
were mistaken for the upper ends of vertical ridges.

The genus Epismilia is one about which there has always been
some doubt, attributable probably to the difficulty attending its deter-
mination from Monitlivaltia. M. de Fromentel proposed it, and it
was clearly recognized as distinct by M. Etallon, under the name of
Ellipsosmilia, D’Orb. Thurman, Fromentel and Ferry, knew and
made use of the differences between it and Monétlivaltia, and so did
Stoliczka, while Milaschewitsch not only adopted it, but pointed out
a character by which it could more easily be recognized. He showed
that the septa have small tubercules on their sides instead of ridges,
and Prof. Koby, availing himself of that means of determination,
has described ten species as occurring in the Jurassic deposits of
Switzerland.

To the description I formerly gave of the present species, under
the name of Monitlivaltia porpita, I need only add the above. Though
confident of the existence of the genus Hpismilia in our Oolites, I
could not determine the species when I wrote my former paper.
One species may now, however, with certainty be introduced into our
Coral fauna.

Donacosmitia Wricutt, Edw. and Haime sp.

This common species occurs in the lower or fourth Coral bed
wherever it is exposed in the Cheltenham district, as well as in the
third Coral bed at Leckhampton Hill. Crickley Hill has, however,
supplied all the best specimens, and they show that it is a tall

R. F. Tomes—Inferior Oolite Madreporaria. ool

species, the corallites of which are placed close to each other. Many
well-preserved calices have now been examined, and the generic
characteristics fully made out. Prof. Duncan assumes that the simple
corallum of Axosmilia Wrighti has been taken by me as the foot-
stalk of Donacosmilia, but I never for a moment entertained such a
supposition. On the contrary, I distinctly stated my belief that
both Aaosmilia Wrightt and Montlivaltia Holli were nothing more
than single corallites of Donacosmilia broken off at their point of
attachment to the parent stem, and I have seen nothing to induce
me to modify that conclusion. The entire margins of the septa,
which are so peculiarly characteristic and common to all the above-
mentioned forms, are not so much as alluded to by Prof. Duncan
in his late paper.

PLACOPHYLLIA GRACILIS, sp. nov. (Plate X. Figs. 5 and 6.)

Single corallites of a Coral having a gracile growth, and almost
always in an indifferent state of preservation, have frequently been
found in the Lower Coral-bed of the Cotteswolds. These could not
be attributed to any known species, and were too fragmentary for
description. Renewed search at those places where that Coral-bed is
exposed has brought to light some better-preserved specimens, which
may be described as follows :—

The corallum consists of a bush-shaped mass of rather closely
placed and nearly parallel corallites, which have nearly the same
diameter from the bottom tothe top. Lateral gemmation takes places
at considerable intervals, and the young corallites thus produced
spring from the parent-stem horizontally, but speedily assume a
perpendicular position by the side of the older corallite, and both
grow upwards together. All the corallites, old and young, have a
well-developed epitheca, which presents numerous and regular rings
of growth. The walls are produced upwards, and with their epithecal
covering, form thin and prominent margins to the calices.

The calices are ovoid and deep, and the fossula is elongated. The
margins of the septa have very little curvature, but slope inward
and downward in nearly a straight line. At the wall the septa are
thick, but they diminish in thickness, and become quite thin as they
approach the columella; though there is sometimes a little thinning
just at their union with it. They are twenty-four in number, that
is to say, three cycles in six systems. The first and second cycles
are united to the columella, and two of the primary ones run into
its two ends, and with it divide the calice longitudinally in half.
The septa of the third cycle are three-fourths the length of the
primary and secondary ones. There are a few rudimentary septa
of the fourth cycle in some of the systems. The columella is thin,
well defined, but not prominent, and is about one-third the entire
length of the calice.

Diameter of the corallites from two to three lines. Their height
cannot be ascertained.

This species bears considerable resemblance to the Placophyllia
rugosa of Becker, from the Corallien of Nattheim.

392 R. F. Tomes—Inferior Oolite Madreporaria.

STEPHANOC@INIA DENDROIDEA, sp. nov. (Plate X. Fig. 10.)

I have long been familiar with fragments of a tall dendroid Coral
from the Oolite Marl of Leckhampton Hill, which had characters I
could not associate with any other Oolitic species, but which were
too ill-preserved for identification. Some well-preserved pieces of
a large specimen from Birdlip Hill, also from the Oolite Marl, having
lately come into my hands, I am now able to describe this species as
follows :—

The corallum is tall and branching, and attains to a height of a
foot, or a foot and a half, and has very much the habit of growth of
Thamnastrea Lyelli. The basal part has sometimes a diameter of as
much as two inches, the horizontal section of which, as well as that
of the branches, is nearly round, but they are nevertheless consider-
ably nodulated.

The calices are evenly distributed, but are a little more distant
from each other in the longitudinal direction of the branches. They
are for the most part lozenge-shaped, ovoid, or even quadrangular ;
but the largest have a rounded outline, and there is a delicate but
distinct line of depression between them. They are superficial, but
have a circular and open centre.

The septa are short and stout, and they are continuous with those
of adjoinin® calices, with which they unite, but yet are divided by
the fine but distinct line before mentioned. When the septa are
worn down, this line of depression is obliterated, and many of the
united septa are very regularly geniculated. In a full-sized calice
there are about thirty septa which are, generally speaking, of nearly
the same thickness and length. Those, however, which have pali
before them are a little stouter than the others. The pali are of
nearly equal thickness and length with the septa, and in a calice
having thirty septa there are fourteen pali, that is to say, nearly each
alternate septum has one before it.

The columella is small and deeply seated. It-is styliform, though
a little compressed, and it is united in some of the calices to one of
the pali. Both septa and pali are regularly denticulated, and the
greater diameter of the denticulations is across the septum. This
is most distinctly observable towards the ends of the branches,
where the calices are circular and much more prominent.

When the septa are worn smooth and the lines of junction with
those of contiguous calices are obliterated, this Coral has much the
aspect of a Thamnastrea. Gemmation appears to take place in the
interval between the calices, where smaller calices are observable.
There is so much similarity between the septa of this species that I
am wholly unable to trace the cycles. The cycles of the pali for the
same reason are equally difficult of determination. The appearance
presented is that of a calice with fourteen principal septa, and their
pali. The diameter of the calices is about one line.

Although the genus Stephanocenia is placed in the Eusmeline, and
for want of better information respecting the Oolitic species I have
placed the present species in that family, I am by no means assured
that it should not be included in the Astreing. That both septa

R. F. Tomes—Inferior Oolite Madreporaria. 393

and pali are distinctly denticulated is obvious, and that, with the
union of the columella with one of the pali, should that prove
constant, indicates a distinct genus.

Of the walls or endotheca I possess no information, the whole of
the inside being crystalline.

STEPHANOCGNIA EXPANSA, sp. nov. (Plate X. Fig. 11.)

The corallum consists of a thin and somewhat rounded plate, the
edges of which are very thin, turned up, and a little undulating, and
there is on a part of it a second or superimposed plate which partly
covers the original one. The under surface has the middle part
most prominent, by which it appears to have been broadly attached.
There is an epitheca with faint concentric wrinkles. The whole of
the upper surface is furnished with calices which are much smaller
and shallower than those of Stephanoceenia dendroidea. As in that
species, they are lozenge-shaped, ovoid, or round, and the depression
bounding them is small but distinct, but the septa are continuous
with those of adjoining calices. There are from thirty to thirty-seven
septa, of which twelve are a little more developed than the others,
and have pali before them. Twelve others have the same length,
but are a little less stout, and the remainder are about two-thirds of
that length, and are much thinner. Both they and the pali are a
little exsert, and have their margins denticulated. The fossula is
small, but well-defined, and contains a slightly depressed but styli-
form columella, which is larger relatively than in the preceding
species.

The endotheca has not been observed.

Gemmation takes place in the interval between the calices.

Only one specimen has yet been met with. It was taken from a
coralliferous stratum at Cooper’s Hill, near Gloucester, which holds
precisely the same stratigraphical position as the one at Crickley
Hill.

Diameter of the corallum, three inches; its height about three-
quarters of an inch; diameter of the calices, a little less than a line.

Montirvatt1a Patnswick1, Duncan.

Many specimens of this species have now been taken from the
Lower Coral bed at Crickley, Birdlip, the Horsepools, and in the
Painswick valley, most of which are small in size, the largest not
exceeding that of the type-specimen figured by Professor Duncan.
As a species it may be distinguished by the tendency to have one or
more of its sides flattened. The form of the calice varies a good deal.
When one side only is flattened, it has a rudely-formed semicircular
outline. It may be more or less triangular or quadrangular, or
indeed polygonal, according to the number of flattened sides of the
corallum. There is an indication only of flattening of one side in
the specimen figured by Professor Duncan, which was for some time
in my hands. The calice of that specimen is deeper than is usual,
owiny to the septa having been somewhat worn down.

In the Oolite marl this species attains to a greater size than it does
in the Lower Coral-bed. Twoexamples from that horizon at Birdlip

394 R. F. Tomes—Inferior Oolite Madreporaria.

Hill are attached, the one to a corallite of Donacosmilia, and the
other to a shell. They are three times the size of the figured
specimen.

Several specimens of this species obtained from the Inferior Oolite
in the railway-cutting at Hook Norton, Oxfordshire, have been sent
to me with other Oolite corals by Mr. Hudleston. In all of these
the flattened side, though visible, is only a little indicated.

Milaschewitsch pointed out that Oppelismilia gemmans, Duncan, was
nothing more than a Montlivaltia which had been subjected to that
sort of interrupted growth to which he gave the name of rejuven-
escence. This growth, Professor Duncan maintains, is only what was
long ago called by MM. Milne Edwards and Haime, “ bourrelets
d’accroissement,” or growth-rings. It is, however, at the present
moment, quite unimportant under what name we speak of it, but it
is very important that we should distinguish very clearly between
it and calicular budding, which is wholly different. But after the
recent remarks by Professor Duncan on the subject, I can only con-
clude that he still confounds the two processes. He now places in the
subgenus Oppelismilia the so-called Montlivaltia Holli, the ‘ Mont-
livaltia turbata, Milasch., and any forms which Mr. Tomes may have
noticed with calicular budding.” If the so-called Oppelismilia
gemmans has calicular budding, then have we a very extensive list
of species of Oppelismilia, and the much crowded and difficult genus
Montlivaltia will be materially and unexpectedly relieved. A very
large per-centage of Lower Lias Montlivaltiz will have to be with-
drawn from that genus, and amongst others Montlivaltia rugosa,
M. mucronata and M. Haimei, while from the Oolitic Montlivaltiz
a goodly number must also be eliminated.

In like manner a considerable number of genera or subgenera
will have to be created for such compound corals as have the same
sort of growth as in the so-called Oppelismilia. For instance, I have
now before me a specimen of Cladophyllia Babeana, some of the
corallites of which exhibit gemmation, supposing it to be gemmation
which takes place in the supposed Monitlivaltia Holli, and if one
species of the genus Cladophyilia is really subject to calicular budding,
it must, by a similarity of argument to that applied by Prof. Duncan
to Montlivaltia, be separated from the other species of Cladophyllia.
But it is an error to suppose that calicular budding takes place
in either case, and even had it been so, it would still have been in-
consistent in the extreme to retain Montlivaltia Holli (which is
distinctly affirmed to have calicular budding) in the genus Mont-
livaltia, while for another Montlivaltia a new genus (Oppelismilia) was
formed, for no other reason than that it had calicular budding.

MonttLivaLtTia Concinna, Tomes.

Subsequently to the description of this species several specimens
were obtained, and with the exception of a single example they were
taken from the Pisolite. They confirm the specific characters already
given. This species may now be regarded as being invariably
attached by a somewhat expanded foot, and as having an undulating

R. F. Tomes—Inferior Oolite Madreporaria. 395

calicular margin, which is sometimes partially everted as in the spect-
men originally described. The thickness of the septa near to and at the
wall is observable in all the specimens I have seen, and is a dis-
tinctive character.1_ It occurs in the Pisolite at Crickley Hill, Leck-
hampton Hill, and at Huddiknoll near the Horsepools, and a single
example has been taken from a sandy bed immediately above the
Upper Lias sands at Dover’s Hill near Chipping Campden.

MonriivantrA DE LA Becuer, MM. Milne Edw. and Haime.

T have collected specimens of this species from the well-known
section of the Inferior Oolite at Frocester Hill, where it is confined
to the upper layer of the compact stone marked C in Dr. Wright’s
section,” which immediately underlies the equivalent of the Pisolite.
The stratigraphical position corresponds therefore with that of the
allied species Monilivalitia lens at Orickley and Leckhampton Hills.
It is by no means rare at Frocester, but is with difficulty extracted
from the stone. I have also taken this species from an exposure of
a few feet of Inferior Oolite in the road leading from Bath to Combe
Down, at a place called Holloway, and by the kindness of Mr.
George I have had the use of a number of small examples which
had been collected at Dundry. By the list of Dorsetshire species it
will be seen that it occurs in several places in that county.

MontTLIVALTIA CUPULIFORMIS.

A single example of this species was all I had seen in 1882, and
no other one has been met with from the same locality. I have,
however, been favoured by Mr. 8. S. Buckman with several ex-
amples from the Inferior Oolite of Bradford Abbas. In the original
specimen obtained by me from Orickley, the adherent base is as
broad as is represented in the figure given by the original describers,
but in those from Bradford Abbas the constriction near the foot is,
generally speaking, much greater, and the upper part of the corallum
much more globose. None of the specimens from Mr. Buckman are
attached, the narrow foot having been fractured.

MontTLIVALTIA sp.

There is a very distinct layer about the middle of the Pisolite at
Cleeve Hill, Cheltenham, containing large flat concretions. Some of
these are much overgrown with Bryozoa and small sponges, and
occasionally a very young and attached Monétlivaltia may be observed.
The species is not determinable, none of the examples yet examined
having attained to any visible height, while the greater number of
them have not even reached that period of growth when the in-
closing wall first shows itself. —

1 T think it right to suggest the possibility of this and some other Montlivaltiz
having wavy and everted margins, being merely the peduncles of a compound genus.
The abnormal septa of the present species, as well as the excessively numerous ones
of the species from the Middle Lias of Charmouth which I have described under the
name of Montlivaltia foliacea, may prove to be costal prolongations of the septa in
progress of development preparatory to gemmation,

* Quart. Journ. Geol. Soc. vol. xvii. p. 9, 1860.

396 R. F. Tomes—Inferior Oolite Medreporaria.

CYATHOPHYLLIA OOLITICA, Tomes.

Repeated and diligent search for this species has been rewarded
by the acquisition of two additional specimens, one from the Crickley
Coral-bed, and the other from the same horizon at Huddiknoll, near
the Horsepools, Gloucester, where the bed is much broken up and
in a mixed condition. In neither of these is the columella so large
or so clearly made out as in the type-specimen.

Prof. Duncan takes great exception to my retaining the genus
Cyathophyllia, and after quoting Reuss and Pourtales, and giving
cogent reasons for merging it into Antillia, as a subgenus of Circo-
phyllia, observes that the facies of the Oolitic species of Cyathophyllia
is not that of Antillia, and further “that any one who had studied
the simple Fungida would place the form in the neighbourhood of
Thecoseris, EK. de From., the uniting and numerous septa being strong
characters amongst the group. One must demur, therefore, to the
admission of this comparatively unexamined form into the genus
Antillia (which has precedence of Oyathophyllia).” Certainly. And
I do most decidedly demur to its being placed in Antillia, even with
the approbation of Reuss and Pourtales, and fully intend to retain
it in Cyathophyllia. Examples of Cyathophyllia liassica (the type
species) and Cyathophyllia Oolitica are now before me, and in both I
observe the same crowded and anastomozing septa. Their generic
identity does not admit of any doubt, nor does any doubt exist in
my mind as to the propriety of retaining Cyathophyllia as a genus.

THAMNOSMILIA, gen. nov.

In the Oolite Marl of Leckhampton Hill, and at no other place, so
far as I at present know, is a branching coral which possesses some
of the characters of Rhabdophyllia, with the addition of a well-
developed and rugose epitheca. Although by no means rare there,
all the specimens I have seen have been completely inclosed in
matrix, and could only be obtained by the use of the chisel and
graver on some of the softer blocks. I define the genus as follows :-—

The corallum is bush-shaped, the corallites lessening in size very
gradually. Branching occurs unfrequently, and the branches are
thrown out at a considerable angle. The wall is thick, and the
epitheca well developed and very rugose. The calices are deep,
circular, and their margins are thin. The septa are numerous,
anastomozing, and passing into the columella, which is large, rugged,
and spongy.

THAMNOSMILIA ANNULATA, sp. nov. (Plate X. Figs. 7, 8, 9.)

The corallum is not of great size, the greatest diameter of a
corallite being only half an inch, and it consists of a peduncular
portion attached to a shell. Generally the corallites have a diameter
of two or three lines. They are seldom straight, but very frequently
considerably curved. The epitheca is very thick and wrinkled, and dis-
posed in rings around the corallites; they are nearly equidistant from
each other and of nearly equal size, and they are continued the whole
height of the corallites. The calices are very deep, almost circular,
and a little expanded just at the margin, which is thin. The septa

_ R. F. Tomes—Inferior Oolite Madreporaria. 397

of the small corallites are not numerous, being about 21 or 24 in
number, that is to say, there are three cycles. Of these the septa of
numbers one and two pass up to the columella, and those of cycle
number three often bend towards and become attached to the earlier
ones. In the larger corallites there are a great many more septa,
and the cycles cannot be traced owing to their anastomozing so much.
In the calicular surface of the peduncle I have mentioned there are
at least fifty septa, and the older ones unite with each other, mostly
in pairs, quite close to the columella, into which when united they
often pass, while the newer ones run into the older ones at points
more or less remote from the columella, according to their age. I
have not as yet met with a perfect calice, that is to say, one in which
the septa have their margins uninjured, and I cannot therefore
describe them with any degree of completeness, but so far as I can
observe, there is no ornamentation of any kind on their sides.

The columella is rather large, rugged, and spongy; its upper
surface having about ten or twelve papilla. It is deeply seated in
the calice, and has no convexity.

The height of the corallum has not been ascertained.

Genus ————— ?

I have met with some portions of a dendroid Coral at Crickley and
at Cooper’s Hill, near Cheltenham, which I have failed to place
satisfactorily. Its ramifications closely resemble those of Donacosmilia
Wrighti, and increase takes place by lateral gemmation near the
calice, just as in that genus, and there is usually a constriction at
the attachment of the new corallite to the old one. As in Donaco-
smilia there is a well-developed epitheca. But it differs essentially
from that genus in having numerous and very thin septa which
have their sides ornamented by rather numerous and well-defined
vertical ridges, ending in prominent points on their upper margins.
The earlier formed cycles meet in the centre of the visceral cavity,
and there form a rugged columella, which has its upper surface
toothed like the margins of the septa. Where the epitheca has been
worn off, numerous dissepiments are exposed.

I am at present unable to refer this species to any known genus,
and the specimens are too fragmentary to admit of the formation of
a new one.

EXPLANATION OF PLATE X.

Fic. 1. Platastrea endothecata, sp. nov., the under surface of the corallum of a
small specimen (natural size).

nee Pe 5 a portion of a larger specimen (natural size) showing
the form of the calices and the continuity of the
septa.

ss Ok Bp 99 the upper margin of a septum, magnified four times
to show the denticulations.

» 4. Br Ms a portion of the lateral surface of a septum, magnified
five times to show the regular and arched dissepi-
ments. :

» 9. Placophyllia gracilis, sp. noy., the corallum, natural size.

6

to) GE * es a calice magnified four times,

398 The Recent Volcanic Eruption in New Zealand.

Fic. 7. Thamnosmilia annulata, sp. nov., a portion of a corallum, natural size,
showing the rugose epitheca.
5 Se 5p o calice of the same specimen (natural size).
ny We 09 39 some septa magnified 24 times, showing their con-
nection with the columella. In this and in the
foregoing figure, the septa are dark in colour as
in the original ; the infilling of the loculi being

white.
5, 10. Stephanocenia dendroidea, sp. nov., three calices, magnified six times.
pyle “3 expansa, sp. nov., acalice, magnified nearly 14 times.

In neither of the figures of Stephanocenia are the denticulations of the septa
shown.

(Zo be continued in our-neat Number.)

_II.—Nors on THe Recent Votoanic Hruprion In New ZeaLanp.

Communicated by Ropert Erurrripex, Jun., Esq.,
of the British Museum.

WHE “Lake District” of the North Island is too well known to

all students of volcanic phenomena, especially of that branch
comprising hydrothermal action, to need a detailed description. It
will be sufficient to say that it forms a belt, crossing the island from
north-east to south-west, and forms a portion of the Middle and
Upper Waikato Basins of Hochstetter. The district has been re-
cently brought into prominent notice by the disastrous eruption of
Mount Tarawera, very full accounts of which have appeared in New
Zealand papers lately received. The eruption commenced in the
early morning of Thursday, June 10th, but premonitory symptoms
showed themselves a few days before in a tidal wave, three feet high,
on Lake Tarawera, great uneasiness of the springs at Ohinemutu,
and the reported appearance of smoke issuing from Ruapehu, the
highest of the great trachytic cones at the extreme south-westerly
end of the system. The belt of activity extends from Mount
Tongariro at the one end to White Island, in the Bay of Plenty, at
the other, a distance of about 150 miles. White Island has under-
gone considerable change from volcanic action during recent years,
and Tongariro was last in eruption in July, 1871; whilst its snow-
clad sister cone Ruapehu has never manifested volcanic action
within the historic period until now. This wide zone in the centre
of the North Island has, ever since the arrival of the Maoris, been
the scene of such extraordinary phenomena, that it has of late been
the resort of visitors from all quarters of the globe.

At 2°10 a.m. on June 10th the inhabitants of the rising town of
Rotorua were aroused by a violent earthquake, accompanied by a
fearful roar, whilst away to the south Mount Tarawera appeared to
be in eruption, an immense black mushroom-shaped cloud hanging
over the whole country from Taheke to Pairoa Mountain, accom-
panied by lightning and heavy peals of thunder. About 4 a.m.
ash-dust began to fall, but a shift of wind turned it coastwards,
“where it worked its calamitous will to the full.” As the day wore
on it was found that Rotorua had not suffered much beyond this
covering of dust and the appearance of fresh boiling springs, neither

The Recent Volcanic Eruption in New Zealand. 399

had the celebrated hot bath of Ohinemutu suffered. On the opposite
side of Lake Rotorua, however, the mud-hole of Tikitere, noted for
its violent spouting and smell, had broken out.

It appears from later accounts that this volcanic outbreak com-
menced at Ruawhia, one of the three peaks into which the cone-like
Tarawera is split. This volcano stands on the southern shore of the
lake of the same name, and is about 2000 feet high; but no tradition
of its ever having been active before exists amongst the Maoris.
indeed, it had been used by them for centuries as a place of sepulchre,
somewhat after the manner of the Parsees and their “'Towers of
Silence.” At the early stage of the eruption it was found that three
large craters had developed themselves on Mount Tarawera, whilst
a fourth was afterwards ascertained to have opened. on the flank
towards Lake Rotomahana. From these were belched forth flames
and large quantities of stones, ash-dust, and clouds of smoke, which
passed over the country both in a northerly, north-easterly, and
southerly direction.

It was, however, at the Township of Wairoa on Lake Tarawera,
midway between Rotorua and Mount Tarawera, that the greatest
devastation took place and injury to life and property. Violent
earth tremors were experienced between | and 2 a.m., accompanied
by showers of ash-dust, and followed by that of stones and volcanic
mud, which ultimately buried the whole place to the depth of ten
feet. The houses were demolished, both those of Huropeans and
Maoris, and many persons killed, including Mr. C. A. Hazzard, the
resident schoolmaster, and members of his family. Had it not been
for the great intrepidity of Mr. McRae, proprietor of the Rotomahana
Hotel, which was also destroyed, a further loss of life would have
doubtless taken place. The pretty Tikitapu bush between Wairoa
and Rotorua was completely destroyed, and the ground covered to a
depth of three feet with dust; trees of 170 feet in height uprooted,
and forming in places tangled masses ten feet thick. All under-
growth was swept away by the accompanying storm, and vegetation
destroyed. The waters of the Tikitapu and Rotokakahi Lakes,
celebrated for their blue and green colours, were changed to a dirty
brown tint, and the outlet of the latter to the larger lake Tarawera
was blocked, and its course altered.

The explosions which took place during the eruption of Mount
Tarawera were plainly heard in Auckland, 180 miles to the north,
and also at Te Aroha. Harthquakes were experienced at Tauranga,
Maketu, and Opotiki, on the shores of the Bay of Plenty, and dust
showers took place at each. At Cambridge and Hamilton, north-
west of the more acutely disturbed district, and between it and
Auckland, reports of heavy explosions were heard, and the windows
shaken ; and much the same phenomena were observed at Coro-
mandel. Even at such distant places as Dunedin and Christchurch,
in the South Island, electrical disturbances were manifested, believed
to be traceable to this volcanic outbreak.

On June 13th matters had calmed sufficiently to allow exploration
and relief parties to proceed beyond Wairoa, and ascertain the con-

400 The Recent Volcanic Eruption in New Zealand.

dition of the world-reputed Lake Rotomahana, and the fate of the
Maori settlements on the southern arm of Lake Tarawera. The ex-
peditions in question were conducted by Mr. James Stewart, Major
Mair, Mr. G. M. Reed, Mr. McRae, the Warbrick Brothers, and Mr.
H. Steele, with Dr. Hector, the Government Geologist, at great
personal risk and after much acute suffering. The sum of their
reports was, that Lake Okaro and Mount Kakarema, to the south of
Rotomahana, were in their normal condition, but along the creek
connecting the former with Lake Rotomahana four craters had
broken out, as well as a large one, 400 yards long, on the flank
of Mount Tarawera, overlooking Rotomahana, where all had before
been fern and tussock grass, throwing up showers of stones, dust, and
volcanic mud. Rotomahana itself appeared to be one immense
cauldron, composed of a series of smaller craters in full action, of
which eleven to fifteen were counted, belching out clouds of steam,
stones and mud. The site of the Pink Terrace was occupied by one
of the largest of these, but that of the White Terrace was “clean
blown out of existence,” and occupied by immense fumaroles. The
dividing line hetween the mud eruption and the showers of dry dust
over the surrounding country was remarkably well shown. From
Rotomahana towards the south-west, the latter extended around
Lake Okaro, and back to Lake Rerewhakaitu, covering an area
of not less than seven square miles. Away to the northward, the
whole of the north shore of Lake Rotorua “ wore the grey drab tint
of the volcanic debris.” It now appears tolerably well proved that
it was the mud from the volcanoes developed on the site of Lake
Rotomahana that destroyed the ill-fated Wairoa township; as well
as the Maori settlements of Te Ariki and Moura on Lake Tarawera,
with all their inhabitants. This volcanic mud has covered a very
large area, from fifteen to twenty miles in length, by an average
breadth of ten or twelve miles. It extended from Rotomahana on
the south to near Ohinemutu on the north, and along the shores
of Lake Rotorua to Ta Heke. The depth varied from a few inches
to ten feet, but at Te Ariki, near the point of ejection, it was esti-
mated to be at least thirty feet in depth, and it was very heavy,
which will account for the manner in which the houses at Wairoa
were crushed down.

Dr. Hector, C.M.G., F.R.S., is stated to have expressed the opinion
that the earthquake shocks caused by the outbreak of Mount Tara-
wera ruptured the steam pipes in the Rotomahana geysers, and let
in the water of the lake upon the subterranean heat, resulting in the
generation of enormous quantities of steam, and the ejectment of the
mud at the bottom of the lake. The material thrown out by Mount
Tarawera appears to have been more of the nature of a white earthy
pumiceous dust, but so far as yet known lava has not been observed.
The pumiceous dust was examined by Profs. Brown and Thomas,
of Auckland University College, who report on a sample obtained
at Tauranga, that it consisted of angular grains of quartz, volcanic
glass and finely divided pumice, fragments of felspar, hornblende,
and other volcanic minerals.

The Recent Volcanic Eruption in New Zealand. 401

My colleacue, Mr. Thomas Davies, F.G.S., of the Mineralogical’
Department, British Museum, has examined samples of the dust sent
home by Mr. Henry Gray, of Auckland, and collected at Rotorua,
and also at Tauranga, which is from forty to fifty miles from the
points of eruption, and finds, the former, which is the coarser, con-
sists of pumice, a glassy scoria, subangular quartz-grains, and a
felspar which is probably orthoclase; the latter is of the same
materials, but finer, and includes more pumiceous dust.

We cannot do better than close this brief account of the Tarawera
eruption by quoting the statement of two of the explorers, Mr. H.
Steel, and Mr. Blomfield, artist to the New Zealand Herald, who
appear to have approached nearer to the points of eruption than any
other explorers, up to the time our last advices left New Zealand.

“We reached a very high and steep hill, almost perpendicular,
immediately above what once was Rotomahana Lake, but which is
now an immense basin, studded with hundreds of small volcanic
cones, geysers, fumaroles, and ngawhas, a regular witches’ cauldron,
awful and terrible..... From the point at which our party was
standing we enjoyed a good view of T'arawera Mountain, Rotoma-
hana, and the line of volcanoes between Rotomahana and Okaro
Lake. One of these was throwing up black mud to a great height.
It was forming a high bank of mud on the western side of its crater.
An immense body of steam was rolling out of a large circular hole,
some two or three chains in diameter. Other volcanoes were throw-
ing out what seemed like a mixture of steam and smoke, but no
lava was proceeding from any of them. ow down on the Tara-
wera Mountain, across the lake, a crater was still smoking, and from
its lower lip there was a large fissure, through which Rotomahana
Lake had evidently burst into the volcano. By this means an im-
mense amount of steam had doubtless been generated, and the
explosion which blew the bottom and sides out of the lake, leaving
it an almost dry basin, had followed. We observed several other
craters on the Tarawera Mountain still smoking, and in the one
opposite to us we noticed a large deposit of pure sulphur......
The view obtainable from the top of the upper hill, the nearest point
to which any one had penetrated, was always more or less obscured
by the steam rising from the basin.

“From the top of the hill above mentioned the ground sloped
almost perpendicularly, and Mr. Blomfield and myself went down
the first half of the hill in grand style, without realizing the
difference between going down and climbing back again. However,
we had this brought forcibly to our minds very soon afterwards.
We landed on a small terrace, and then the descent of another hill
(not so steep) landed us on a small mud flat which lay between the
foot of the hill we had come down and the edge of the crater—that
is, of the place where Lake Rotomahana once was. We walked to
within five feet of the edge of the abyss, and looked over, and saw
a sight which I do not think either of us will ever forget. The wind
blowing from the north lifted the steam and disclosed the dry bed
of Rotomahana, which is now one scene of volcanic action, impos-

DECADE III.—vVOL. I1l,—NO. IX, 26

402 Rev. A. Irving—The Bagshot Beds and London Clay.

sible for words to describe. .... A few pools of dirty boiling
water still existed at the western end, and a rather large one at the
eastern end. Hundreds of volcanic cones were throwing out steam,
and what appeared to be black smoke. Scores of geysers were
playing away merrily, throwing water many feet into the air. In
one place a small plateau of mud had been thrown up, and on it
was a pool of yellow boiling water, from one end of which a jet of
dirty smoke or steam as thick as a man’s body was issuing. About
one hundred yards from the western end a large volcano, in very
violent action, kept up a continual discharge of mud and steam,
accompanied by a heavy rumbling, roaring sound. It would be
impossible to describe the wonders of the scene in their infinite
variety of volcanic grandeur. We were then standing on the bank
above where the Pink Terraces formerly existed. 'The whole southern
bank of the lake has been blown completely away, and the spot
where the Terraces once stood is now an open gap. We next walked
round the crater to the western end of the lake, to try to obtain a view
of the White Terraces. Having waited till the steam lifted, we
then saw that the White Terraces were also gone. The appearance
of the place where they had stood was entirely changed, but a very
active geyser was still playing. Returning back to where we
first came down to the crater’s edge, Mr. Blomfield took a sketch
of the scene before us. We then started on the return climb—a very
different thing from the descent. After a long pull, we got on to the
first terrace, and then began the ascent of the big hill. We slowly
crawled up its steep face, digging our hands and knees into the soft
mud of which it was composed... . . We stopped to rest every few
minutes, preventing ourselves from slipping back by thrusting our
arms straight into the face of the hill, but when we got within
thirty feet of the top, a slight earthquake shock, which shook the
hill and sent the sand down round us, acted like a refresher, and we
made good time to the top. where we found the rest of the party.”

It is also reported that Tarawera had developed seven craters on
the Tarawera Peak proper, and three on Ruawahie. It is further
believed that those on the immediate site of Rotomahana will remain
permanent.

T1].—Tur UnconrorMity BETWEEN THE BacsHot BEDS AND THE
Lonpon Cuay.

By the Rey. A. Irvine, B.Sc., B.A., F.G.8., of Wellington College.

hfe the paper on the well-section at Brookwood in the August

Number of the Guonocrcan Magazinp,' the author pointed out
that a comparison of the lithological facts brought to light in that
section with those furnished by two other deep-well sections (at
Wokingham and Aldershot respectively) lead to an inference in favour
of a considerable amount of denudation of the London Clay having
taken place during the deposition of the Bagshot Beds; that is to

1 While that paper was passing through the press, the author was informed by the

contractor, Mr. 8. P. Coaker, that “a very perfect shark’s tooth was found at the
depth of about sixty feet.’? May not this have been derived from the London Clay ?

Rev. A. Irving—The Bagshot Beds and London Clay. 403

say, irrespectively of the particular horizon in the Bagshot Series
to which certain marginal portions of the Bagshot Beds may be
ultimately assigned, there seemed to be pretty clear evidence
furnished, from the London Clay itself, of the fact, that along their
northern and southern flanks the Bagshot Beds rest on beds belonging
to lower horizons in the London Clay formation than those on which
the Bagshot Beds rest in the more central portions of the area. The
present brief paper is an attempt to show that the above conclusion
is borne out by a much wider induction from data gathered from
the area of the London Basin in general. I have carefully gone
through the 448 well-sections appended to Mr. Whitaker’s Memoir
on the London Basin,’ and have selected from among them such
instances as seemed to throw any light upon this question. A large
majority of those sections include the London Clay ; but since, in a
great number of them, the thickness of that formation in feet is
given only, unaccompanied by any lithological notes on the strata,
they have been omitted, as affording no help to us in the present
investigation. There are, however, as many as 29 sections, in which
such notes appear. In every one of these the Reading Beds or the
Thanet Sands, and in most cases both these formations, were proved
below the London Clay, so that we are quite sure of a correct basal
horizon. In many instances also the Basement Bed of the London
Clay is noted. In 22 of these 29 sections, the thickness of the
London Clay is less than 200 feet, and in all these there is mention
of such inclusions in the strata as ‘green sand,’ septaria (‘clay-
stones’), pyrites, flint pebbles, and ‘shells.’ These therefore agree
in this respect (without a single exception) with the lower half or
rather more of the London Clay of the Brookwood section, as shown
in the deep well at the Asylum on Knap Hill, which also (as shown
in my last paper) agrees with the London Clay strata pierced at
Wokingham on the northern, and at Aldershot on the southern,
margin of the Bagshot area. From this I conclude that in all these
22 sections we have (within their several limits) homotaxial equiva-
lents of strata of the lower half or rather more of the London Clay,
as that formation is proved in the Brookwood section.

In the remaining seven sections there is no mention of septaria,
etc., above about 200 feet from the base of the London Clay. Of
course this does not absolutely prove the absence of them, in these
seven sections, but the number of instances is sufficiently large to
establish a high degree of probability that they were not found
at those higher horizons; and in every case there is mention of them
at horizons below. The list from which this inference is drawn
includes sections at Aldershot Place, on the south side of the area,
at Hampstead, Harrow, Braintree and Chelmsford, on the north, and
at Canterbury in the extreme east. The great majority however are
in the metropolitan portion of the area. One of these (at Wimbledon)
corresponds so well with the Brookwood section,” that it deserves to
be given here more in detail, as follows :—

1 Memoirs of the Geol. Survey of Great Britain, vol. iv.
* Guou. Mac. August, 1886.

404 Rev. A. Irving—The Bagshot Beds and London Clay.

feet.
Soil and clay (brown) .... fog abe 1a aoe:
se SN Ss
{ Lead-coloured, hard, flaky clay ... me ot is 20
Reddish sand and lead-coloured clay... on see 00
Lead-coloured, strong loam 60
London

Lead-coloured clay or r loam, with stony nodules (septaria) 40
(lige Hard rock . 4
Y- ] Lead-coloured clay with much sulphur, many “Jumps ‘of
stone, giving off ‘‘ noxious air,” some rotten wood
below .. oa mae Suc ad obt we 236
( Hard rock ... a6 sea Bes ig. ois ofa E
Total thickness of London Clay .——437

440 ft.
This well was “sunk all the way.’’

At page 282 of the Memoir, Mr. Whitaker mentions a section in
the Wimbledon neighbourhood, which shows a passage upwards:
from the London Clay into Bagshot Sands. This bears out the
inference which I drew in my last paper from lithological evidence
very similar to that cited by bim, as to such a passage occurring in
the well-section at Brookwood.

It is of course a rare thing in wells in these Tertiary strata
to come across a shoal of fossils, such as that mentioned by me *
elsewhere, as occurring in the green earthy sand of the Middle
Bagshots at Yateley, Hants; but isolated fossils are occasionally met
with, and generally, as might be expected, in a good state of
preservation in the London Clay. In the deep well at the Ascot
Racecourse, of which I have already published an account, ? the
following, which are now in my possession, were found: Pholodomyw
margaritacea (192 above the base) ; Oyprina planata (a rather young
individual). A well-rounded pebble of flint was also found at
75 feet above the base of the London Clay.

Prof. T. Rupert Jones, F.R.S.,° has also mentioned the following
as met with in the Wokingham deep well: Cardium, Cyprina planata,
Pholodomya virgulosa, Nautilus, Panopea intermedia, Pinna (fragment),
Dentalium, Acteon, Natica, Astarte, Cytherea tenuissima, Ditrupa.
These forms range through the whole of the 273 feet of the London
Clay pierced in that section, including the Basement Bed.

From Mr. Phillips’s brick-yard, close by Wokingham Station, and a
few feet only below the unconformable junction of the Bagshot Sands.
and the London Clay, which is seen just below St. Paul’s Church,‘ I
have obtained the following forms: Cyprea Bowerbankii, Cardium Lay-
toni, Corbula Regulbiensis (?), Modiola elegans, Panopea (fragment),
Pleurotoma gentilis, Vermicularia Bognoriensis. Some of the septaria
found in this pit are charnel-houses of scarcely any other forms than
V. Bognoriensis. The presence of these forms would seem again to indi-
cate a tolerably low horizon in the London Clay for the beds on which
the Bagshot Sands at Wokingham are superimposed. Oxidation-pro-
ducts of pyrites and flint pebbles are common in the London Clay here.

1 Q.J.G.S. August, 1885, p. 500. 2 Proc. Geol. Assoc. vol. ix. No. 5.

3 Gror. Mac. Decade II. Vol. yy pp. 422, 423.
4 Q.J.G.8. loc. cit. p. 505, fig.

Rev, A. Irving—The Bagshot Beds and London Clay. 408

_ From the London Clay at Aldershot, in the brick-yard due south
of the Station, I have obtained Cyprea Bowerbankii, Modiola elegans.
The last-mentioned is very abundant in the septaria of that locality.
'* In his excellent work, Stratigraphical Geology and Palaontology,*
Mr. Etheridge remarks: “ Prof. Prestwich has shown that there are
traces of paleontological zones in the London Clay, the lowest
indicating in the east of the area of deposit a maximum depth of
water (500 feet), while a progressive shallowing is seen in the
higher zones, the uppermost of which contains the chief part of a
terrestrial flora, as well as the fish and reptilian remains, all of which
are seen in the Sheppey Beds.”

The thicknesses given by Prof. Prestwich? for the London Clay, as
proved in two wells at Sheerness, are 347 feet and 356 feet, very
near approximations to the least thickness (371 feet) assigned in my
last paper to the same formation in the Brookwood section. There
too, according to Mr. Whitaker,* “the London Clay has a more
loamy character and brown colour; there are also some beds of sand
(north of Wyburns) which become more numerous further east, so
that there is no sharp line of demarcation between the undoubted London
Clay and the overlying sand, which has been referred to the Bagshot
Series.” This corresponds very well with what I have described as
indicating a passage in the Brookwood section; while such features
are conspicuous by their absence in all sections where I have seen
the Bagshots resting on the London Clay along the flanks of the
present Bagshot area.

It is much to be regretted that the works at Brookwood were not
watched during the progress of the well through the London Clay.
As it is, there would appear to be no record of any traces of a
‘terrestrial flora’ or of ‘fish and reptilian remains’ to correspond
with those of the Sheppey Beds. In the most complete as to its
details of the well-sections referred to in this paper — that of the
Wokingham Town Well—furnished on so excellent an authority as
that of Prof. T. Rupert Jones, there is no mention whatever of any
traces of those remains which seem to characterize the higher zones
of the London Clay ; nor have I met with any in the brickyards at
the surface. It would appear, therefore, that at Wokingham the
evidence furnished by the London Clay itself, as to the removal by
denudation of all the upper portions of that formation, before the
Bagshot Sands were deposited upon it, is pretty direct and conclusive ;
and this entirely harmonizes with the observations, which I have
previously recorded,‘ of the evidence of erosion of the London Clay
beneath the Bagshot Sands at Wokingham, and the occurrence of
rounded flint pebbles on that eroded surface at the bottom of the
Bagshot Sands there exposed.

Taking all the facts adduced in this paper, and comparing them
with those mentioned in my paper on the Brookwood section, it is

1 Page 610.
2Q. J. G.S. vol. x. p. 404, quoted by Mr. Whitaker at p. 469 of the Memoir
on the London Basin. ° Memoir, p. 317.

4 Q.J.G.5. August, 1885, pp. 504, 505; Proc. Geol. Association, vol. ix. p, 222.

406 S. A. Adamson—Fossil Tree near Bradford.

difficult to see how we can arrive at any other conclusion than one
favourable to unconformity, from evidence furnished by the London
Clay itself.

Where this formation exists in its full normal development, with
Bagshot Beds superimposed upon it, there appear to be clear signs
of a passage from one formation into the other: on the other hand,
where—as in sections elsewhere described by me—on the marginal
portions of the Bagshot area, the transition is an abrupt one, the
stratigraphical data furnished by the London Clay seem to lead to
the necessary inference, that the upper beds of that formation, to the
extent of probably 100 to 150 feet in thickness, were removed by
denuding agencies (furnishing perhaps the clayey materials of the
Middle Bagshots') before the Bagshot Beds were deposited upon the
London Clay in those localities.

Norr.—In generalizing from a number of deep well-sections in a
given geological district, it would be mere pedantry to insist upon
the exact value of the measurements in every case. Hrrors may
arise from tubes getting out of the vertical, and from the materials
getting mixed up to some extent in the boring tools. But they no
more vitiate the conclusions drawn from a general agreement of a
number of sections than those slight variations allowed for on the
score of “errors of experiment” in experimental science invalidate
the conclusions drawn from a general agreement of results. In some
instances, moreover, we have more definite data than a mere boring
can furnish. At Brookwood, for example, the six-foot well with
iron-cylinders was carried down to a depth of 197 feet, that is to
say, through the whole of the Bagshot series and into the London
Clay; at Wellington College the six-foot well penetrates about
180 feet; in the Ascot deep-well mentioned above the shaft or well
extends down to 250 feet; and in the deep well at Wokingham the
six-foot “dry-sinking” was carried down to 264 feet, that is, into
the Basement-bed of the London Clay.

IV.—Norzrs on tHe Discovery oF THE BASE OF A LarGE Fossin
TREE AT CLAYTON.
By S. A. Apamson, F.G.S.

NLY a short time since there was discovered in the Lower Coal-
measures at Idle, a magnificent specimen of Megalichthys
Hibberti ; and now, at Clayton, near Bradford, has been found one of
the grandest examples yet seen of a fossil Sigillaria tree. It was in
the Fall Top Quarry, at Clayton, worked by Messrs. Murgatroyd and
Sons, that this remarkable fossil was discovered, and these gentlemen
deserve the highest praise from all geologists for the skill and
extreme care with which they have bared the fossil, and also for
their kindness in allowing it to be inspected. This quarry is not far
from the edge of a bold escarpment overlooking the Thornton
Valley, and the well-known Elland Flagstone is worked here for
landings, flags, ete. Between the Better-Bed-Coal and the Flagstone

1 Cf. Proc. Geol. Association, vol. ix. No. 5.

S. A. Adamson—Fossil Tree near Bradford. 407

there is a great thickness of sandstones, shales, etc., of various
characters, and it was in these measures that the fossil tree was dis-
covered about 12 feet below the surface. The sandstones just
referred to are of little commercial value, many being irregularly
bedded, and others very perishable in their nature ; the better kinds
are used for rough walling, the remainder being merely rubbish to
fill up other excavations. ‘The marketable flagstone i is at aconsider- —
able depth in this quarry, and blasting operations have to be carried
on to remove rapidly the overlying strata. After one of these
explosions, Messrs. Murgatroyd observed part of a large fossil tree
exposed, and, profiting by their knowledge of geology (which, by
the work of the Yorkshire Geological Society and also of the Leeds
Geological Association, is rapidly spreading throughout the entire
county), they immediately suspended further operations, and, instead,
gave orders to their workmen to carefully bare the remainder of the
roots. Part of the stump and four of the roots were damaged by
the explosion, but four roots were left in situ. Since then, the
broken pieces have been collected and placed together most admirably,
presenting now the remarkable sight of a huge stump of Sigillaria,
sending out eight forked stigmarian roots. The following dimensions,
carefully measured, will afford an idea of the magnitude of this
fossil :—

ft. in.
Height of stump... ... SGOU Vccg: a Hoes fone Minos Lays AC)
Diameter of stump (longest: axis) bs coo O
9 i (at right angles to longest axis)... 3 10
Distance Distance from point of
Diameter close from stump to bifurcation to present Greatest length
Root. to stump. bifurcation termination of root. of root.
,of roots. Right fork. Left fork.
No. inches. ft. in. ft. in. ft. in. ft. in.
1 5 21 A090 40 ih 9 6 aes 13 0 17 0
2 IES aeoee 40 8 0 50 6 6 12 0
3 16 50 dO 40 12 0
4 16 40 20 46 8 6
5) 174 70 16 3 0 10 0
6 18 5 6 3 0 46 10 0
7 17 76 3 0 20 10 6
8 17 70 9 6 7 0 16 6

The diameter of the visible area covered by the ramifications of
the roots, is, from north to south, 29 ft. 6 in. and from east to west
28 ft., giving a superficial area exposed of 826 feet. The stump of
the tree was embedded in soft sandy shale, locally termed “ yellow
loam,” the roots resting on a bed of soft blue shale, which some of
them penetrate. The roots 7 and 8, and also the roots 1 and 2, re-
spectively cross each other, producing depressions in the lower roots
at the point of contact. The Stigmarian roots present very finely
the characteristic pits or scars from which the rootlets or filaments
formerly originated, and an examination of the shale immediately
touching the roots, reveals these rootlets in vast numbers. The
neighbourhood appears to be prolific in grand examples of Carbon-
iferous vegetation, for in another part of the quarry at a short distance,
I observed two large stigmaria protruding from the side, whilst in the

408 Notices of Memoirs—Short Notices of Scicntifie Papers.

cutting of the railway close by, a good, but much smaller specimen
of Sigillaria, with roots attached, was carefully got out, and presented
by the engineer to the Yorkshire College at Leeds. So remarkable
a fossil as the one described should be procured at once for one of
our museums; it would be an unrivalled example for geological
students. To allow it to meet the common fate of many fine fossils,
that of being broken up for rockeries or gardens, would be an act of
inexcusable and gross scientific vandalism. The proprietors intend,
although it stops the progress of their business, to allow it to remain
undisturbed for three or four weeks longer, and to any geologists
tempted by the breezy Yorkshire hills and fine scenery, they offer
a hearty Yorkshire invitation to inspect this giant fossil.

WOTLICHS OF MEDMZOLRS.

J.—SHort Notions or Sctentrric Papers.

1.—Bibliothéque Géologique de la Russie, rédigée par S. Nikitin.
Large 8vo. pp. 126. (St. Petersburg, 1886, Librairie Eggers et Cie.)

te work is intended to be a record of all books, periodical

publications, and brochures treating of the geology, mineralogy,
and palzontology of Russia, whether published in that country or
elsewhere. It gives a short résumé of the contents of each work in
Russian and French. The present is the first memoir of the series,
and contains references to 256 separate papers which have been pub-
lished in 1885. They appear to have been very carefully prepared,
and in the paleontological papers the names of the new genera and
species are quoted. There is also a complete index. This record
will be of special value to all geologists, to whom at present works
published in Russian are quite unavailable, for it will at least furnish
an idea of the progress of the science in that country, and we
sincerely hope that it may be continued in future years.

Annalen des K. K. Naturhistorischen Hofmuseums ; redigirt von
Dr. Franz Ritter von Hauer. Bd.i. No. 2. (Wien, 1886.)

This second number of the Annals of the new Natural History
Museum at Vienna contains amongst others, the following important
papers :—

2.—Ueber die miocenen Pteropoden von Msterreich Ungarn, von
Ernst Kittl. Mit einer lithogr. Tafel.

The characters of the minute and delicate shells of Pteropods from
the Austro-Hungarian Miocene strata are carefully worked out, and
illustrations given of most of the species. Their presence in great
numbers indicates, according to the author, the abyssal character of
the deposit. The following new species are described: OCreseis
Fuchsi, Vaginella Lapugyensis, V. austriaca, V. Rzehaki, Balantium
Fallauxi, B. Bitineri, Hyalea bisulcata, Spirialis Keneni, 8. Tarcha-
nensis, and S. Andrussowt.

Notices of Memoirs—A. G. Nathorst—Tracks of Animals. 409

3.—Ansichten ueber die paleozoischen Insecten, und deren
Deutung; von Prof. Dr. Friedrich Brauer. Mit zwei photozinkogr.
Tafeln.

This is an elaborate critical review of the classifications adopted
by Scudder, Brongniart, and others, for Paleozoic insects, and of the
significance of the characters on which these have been based. In
many points the author disputes the views of Scudder, lately pub-
lished in Zittel’s Handbuch der Paleontologie. The wing-structures
of many of the Paleozoic insects and of their nearest living allies
are well iliustrated in the accompanying plates. Amongst other
conclusions, the author states that the Palzozoic insects present no
contradiction to the views of biologists as to the origin of the class,
and that they did not form a special order which could be regarded
as a general basis for the existing orders of insects.

4.—Bestimmung des specifischen Gewichtes von Mineralien, von
Dr. Victor Goldschmidt.

The author points out the causes for the differences occurring in
the practical determination of the specific gravity of the same
mineral ; which rest not so much in the method adopted as in the
selection of the materials which are tested. Cradle Jal,

IJ.—NovuvELLES OBSERVATIONS SUR DES TRACES D’ ANIMAUX ET AUTRES
PHENOMENES D’ORIGINE PUREMENT ME&CANIQUE DECRITS COMME
“ AreuEs Fosstues.” Par A. G. Narnorst. Avec 5 planches
en phototypie et plusieurs figures intercalées dans le texte. Kongl.
Svenska Vetenskaps-Akademiens Handlingar, Bandet 21, No.
14, (Stockholm, 1886.)

dae memoir is intended as a reply to the objections raised by
the Marquis of Saporta and MM. Lebesconte and Delgado, to
the opinions previously published by the author, that many of the
supposed fossil alge are in reality nothing more than the tracks of
animals, or phenomena of purely mechanical origin. The fossils,
whose nature is thus contested, are commonly known as Cruziana, or
Bilobites, Harlania, Hophyton, and some other genera. 'They generally
present themselves in demi-relief on the under surface of the beds
in which they occur; no traces of organic substances are found
associated with them, and they are composed of the same minerals as
the matrix in which they are imbedded. The theory of their veget-
able character rests on the peculiarity of their markings, which are
supposed to be incapable of being produced by the tracks of
organisms. Dr. Nathorst, however, shows very conclusively, that
whilst it is difficult to understand how alge could thus form casts in
demi-relief on the under surface of the beds, such structures would
be the natural result of the filled-up tracks or burrows of marine
organisms. Of the manner in which these could be made, the author
gives practical proof by passing a movable roller, shaped like a
double spindle, over the surface of a layer of soft mud, and then by
means of gypsum obtaining moulds of the concave impressions.
Photographs of these moulds are given in the accompanying plates,
and they faithfully represent in almost every detail, the supposed

410 : Reviews—Prof, Edward D. Cope-—

alow. The author by no means denies the probable occurrence of
true Algz in Paleozoic strata, though he considers that most of the
forms described as such by Saporta have no claim to be included in
the vegetable kingdom. adh 136

IIJ.—On tHe Frora or tHe Cromer Forrst-Bep. By Cirment Rerp,
F.G.S. Transactions of the Norfolk and Norwich Naturalists’
Society, vol. iv. pp. 189—200.

ROM various exposures of the so-called Cromer Forest-Bed at
different localities on the coast of Norfolk, and at Pakefield in

Suffolk, Mr. Reid procured samples of dark peaty sandy clays, which
by careful manipulation and washing, yielded the seeds and fruits of
a number of plants. These were patiently and carefully picked out
under a magnifying glass, classified, mounted, and then compared
with existing forms, with the results that the number of species in
the accompanying list is more than double that previously known.
The species of Mosses and Chara have not yet been determined, but
the list includes 40 species of Dicotyledons, 18 of Monocotyledons, 5
Gymnosperms, and 3 Cryptogams. With a few exceptions the same
plants still exist in the locality, but some are locally extinct. Mr.
Reid points out the significance of this fact, when it is considered
that since the period when the plants lived whose fruits and seeds
have been preserved, the Glacial epoch has intervened, and the large
mammals, and even many of the mollusca, have become extinct. So
far the investigations into the Pliocene Flora show that the period
of intense cold produced but little effect in the distribution of the
plants in this locality, since the same forms with few exceptions
returned, apparently without intermixture, to re-occupy their former
habitats.

The paper is a brief one, but it represents a great amount of
steady, continuous work, and careful observation. It will prove of
much value, both from a botanical as well as a geological point of
view, and its importance is enhanced from the fact, that with one or
two unimportant exceptions, no Plant-remains are yet known from
other Pliocene beds in Britain. G. J. H.

ReV Lew Ss.

I.— DEPARTMENT OF THE INTERIOR. Report oF THE UNITED STATES
GEOLOGICAL SURVEY OF THE TERRITORIES. F. VY. Haypren, Unirep
STATES GEOLOGIST-IN-CHARGE. VotumE IIJJ. Tur Vertesrata
or THE TERTIARY Formations or Tue West. Boox I. By
Epwarp D. Corr, Member of the National Academy of Sciences.
(Washington, Government Printing Office, 1883.)

_ recent scientific history of civilization few administrative
events can compare in magnitude, or in their effects upon the
populations concerned, with the Geological Survey of the United
States. In no other part of the world have the resources of the
Government been used with a like wisdom and liberality in
accumulating and diffusing natural knowledge of the country, for

Tertiary Vertebrata of the West. 4\t

‘the benefit of the people. It is impossible to express too strongly
admiration for the administrative discernment which has recognized
that organized knowledge of the geographical, geological, botanical,
zoological, and anthropological conditions of the newly-settled lands.
of the West, is the necessary foundation for their commercial, social,
and political prosperity. But when we contemplate the library in
which the achievements of this great conception stand recorded, with
all the elaboration which the best science of our time could com-
mand, we yield homage to those who have planned and have carried
out this work, for a service to their country and to humanity, which
in its way has no parallel.

The branches of science are so interrelated, that none can be said
to be less or more important than the others. And if to the popular
imagination geology and paleontology do not seem quite so engrossing
as other matters among life’s interest which develope from them, as.
a foundation, it is manifest that they have engaged the enthusiasm
and life-long labour of intellects among the most remarkable which
modern times have produced. And the great American Republic
may be congratulated on having commanded the services of men of
genius, whose courage and industry have been equal to grappling
with this gigantic work.

The latest of the United Survey Reports, by Professor Cope, issued
as a first part of a brief history of the fossil remains of Vertebrata,
found in the Tertiary rocks of the Western Territories, extends to
more than a thousand quarto pages of text, illustrated with some
woodcuts and one hundred and thirty-four quarto plates, and gives
in a noble and connected form a panorama of the life which the
author had studied during the preceding ten years. Professor Cope’s
previous contributions to the same series of publications have pre-
pared us for these matured studies, which are well described by
Major Powell, the Director of the United States Geological Survey,
as a “valuable contribution to paleontology, and a monument to
the labour and genius of the author.”

Professor Cope is a naturalist in the largest sense of the term;
not undervaluing the great results which reward the comparative
anatomist, but conspicuous among those who have cherished the
traditions of zoologists, he has known well how higher results
depend upon detailed work, and clear, full, and accurate description
of the variable elements in organic structures. No man has a keener
appreciation of the order of nature; and it is manifested again and
again in new grouping, or the definition of new groups, or the inter-
calation of new types in their places among well-known tribes,—a.
power which is rare, because it can only flow from a knowledge of
the extent to which the structures of any extinct type may vary,
consistently with the preservation of its group plan, or the elimina-
tion from that plan of a series of characteristics. The gifts and
attainments in which the analytical and synthetic powers are evenly
balanced, and by which the extinct and existing life have been
examined by the same methods, have long made the author of this.
work conspicuous as one of the most successful paleontologists who
have yet adorned the science.

412 Reviews—Prof. Edward D, Cope—

The volume now noticed is conceived in a systematic spirit. After
the preface, which accounts for the origin of the collections, states
the rules of nomenclature, and the chief scientific results attained,
an Introduction describes the geological succession of Tertiary rocks
of Western America, and attempts to correlate, on the evidence
of their fossils, the American rocks which contain vertebrata, with
those of Europe. If we do not discuss this correlation, it is because
it raises questions which would require a volume for their examina-
tion ; but we may say that just as the occurrence of fossil reptiles in
America nearly allied to those in some European strata seems to us
insufficient to fix the age of the American deposits ; so the presence
in American strata of extinct species of European genera of Mammals,
even when many occur in common, is but uncertain proof of identity
in age between the subdivisions of the American Tertiaries and the
subdivisions recognized in Western Europe. But if this problem,
which is taken up as it were by the way, is not finally solved, facts
enough are presented to challenge attention, and justify the correla-
tions which are made.

The first part of the volume discusses the Puerco, Wasatch, and
Bridger groups of American fossil vertebrate life. The oldest of
these is regarded as Tertiary, rather than as Post-Cretaceous. It
is a lower division of the Wasatch series, with a distinct fauna,
accumulated in the Wasatch Lake. The Wasatch beds range from
New Mexico through Colorado and Wyoming, and consist of sand-
stones and marls, which vary from fifteen hundred feet to five
thousand in thickness. Very few vertebrate fossils are found in
the overlying Green River beds; but the Bridger group which suc-
ceeds has yielded a rich fauna, though the beds are less widely
distributed than the older Eocene series.

The fauna of these beds comprises first, a large number of Fishes,
which are observed to have a facies similar to that of the existing
fresh waters of the United States, with the addition of two families
now confined to the southern hemisphere. Among the Fishes we
note a new Hlasmobranch genus, Xiphotrygon, which is the genus
Trygon with the teeth of Raja. The Lepidosteus type is represented
by the extinct genus Clastes, of which four species are indicated.
Pappichthys, another genus of these beds, differs from the existing
Amia in having one, instead of several rows of teeth on the bones
about the mouth, but though founded on mandibles, some of the
species are described from vertebrae. The genus Rhineastes is a type
of doubtful affinity, characterized by possessing vomerine teeth, and
well known from five species. Dapedoglossus is a genus with four
species closely related to Osteoglossum. Diplomystus comprises
five species of Herrings, which differ from the genus Clupea in
possessing small dorsal scutes in the median line of the back. The
Perch type is represented by several genera, defined by the author
under the names Hrismatopterus, Amphiplaga, Asineops, Mioplosus and
Priscacara. Of these genera, perhaps the most interesting is
Mioplosus, which is allied to Lebrax and Percu. This fish fauna
has more than ordinary interest from its occurrence in beds which

Tertiary Vertebrata of the West. 413

yielded the higher vertebrata. Of Batrachia, the only Tertiary
specimen known is from the Green River beds, and belongs to a
tailless Batrachian, but too imperfect for description.

The Reptilia of American Eocene age are in no way remarkable
except for the appearance of new genera. The Crocodilia differ in no
important character from existing species of the genus Crocodilus.
Five species are found in the Wasatch beds, and six other species in
the Bridger beds. Seven species are here described : one, C. heterodon,
is as small as an Iguana, while C. clavis is equal to the largest Hast
Indian species. The Testudinata are more numerous. Sixteen
species are found in the Wasatch beds and thirty-two in the Bridger
beds. Emys, Trionyx and Plastomenus are genera surviving from the
Cretaceous period, while six new genera appear, of which five are
limited to these deposits. The new genera include Awestus, which,
belongs to the Trionychide, Anostira of Leidy, Hadrianus, Notomorpha..
The genus Hmys is represented by eleven species. The Lacertilia
are known from three species of Champsosaurus, especially interesting
as a type which survives from the Cretaceous Laramie formation.
Only one Serpent is known; it is referred to an extinct genus
Protagras. After the remarkable reptile fauna of the Laramie
and Cretaceous rocks, this reptile fauna may seem tame; but any one
who studies the beautiful plates which illustrate it will find abundant
materials for philosophic study among the narrow-nosed Crocodilia,
the variously-modified Tortoises, and the vertebrae of Champsosaurus.

Turning to the Mammals, Professor Cope reminds us that the
Mammalia, like the Reptiles of the Permian epoch, have the family
types in the Eocene rocks of America all more generalized, and
that the orders are not so sharply differentiated from each other as
in the later periods of the earth’s history. The contribution there-
from which America now furnishes to our knowledge of the Mam-
malia is one of the most interesting chapters in the history of the
group.

The story begins with the Marsupialia. This is one of the most
difficult groups to define accurately on account of the strong insecti-
vorous strain of characteristics which is so often present among
fossils. But among genera which are more definite in their affinities
is the remarkable genus Catopsalis, a rodent-like type with the jaw
inflected as in the Kangaroo and Kangaroo Rat, but with a tuber-
culated Mastodon-like molar dentition. Péilodus is another interest-
ing Marsupial, remarkable as representing the Purbeck Plagiaulax
in the American Kocene, though the affinity is not of a distant kind.

Passing to the Rodentia, the representatives are again few. They
are apparently allied to the Squirrels, and are referred to five species
of the genus Plesiarctomys, a well-known type in the Eocene of
France.

The next order is termed Bunotheria. It is defined as having the
animals armed with claws, with a transverse mandibular condyle, the
molar teeth usually tubercular, and with incisors in the premaxillary
bone. There are usually five digits, and commonly a third trochanter
to the femur. Jt comprises all those animals which the author had

414 Reviews—Prof. Edward D. Cope.

at various times referred to the groups Creodonta, Mesodonta, Insec-.
tivora, Tillodonta and Tzeniodonta, tribes which are now regarded
as suborders of the Bunotheria. The group is almost as varied as
the Marsupialia, and is regarded as a generalized type in which the
relationships are not all with the smooth-brained mammalian orders,

NG

a Right ramus external. Inner.
6 Right ramus internal.

e Superior view.

d Inferior view. Outer.

é Polymastodon taoensis, possibly
molar teeth of Catopsalis.

Ptilodus medievus.

but quite as close with the Gyrencephala. The Creodonta are
thought to be the ancestors of Carnivora, while the Mesodonta are
probably ancestors of the Prosimiz, and the affinity between the
Prosimiz and the Carnivora is considered as established. The Teenio-
donta have Rodent-like inferior incisors, but also possess inferior
canines. Hach molar has a simple conical fang, and the enamel

Tertiary Vertebrata of the West. 415

round it combines to suggest the characters of an Edentate. So that
Calamodon is thought to furnish a hint of the relationship of the
Edentata to other Mammals. Teniolabis is a genus of allied character,
founded on a single tooth. The Tillodonta is a suborder with
rodent-like incisor teeth ; and this character distinguishes the group
from the Insectivora, to which the molar teeth approximate. There
are three genera in this suborder. Psitiacotherium has six inferior
molars with cross crests, which with wear assume the form of the
letter B, with the convexities turned forward. The incisor teeth are
powerful and adapted for breaking nuts or cutting fruits. Two
species are known. ‘The other genera of this group have no repre-
sentatives in the Wasatch and Bridger faunas. The Insectivora,
which alone survive at the present day of all the Bunotheria,
are well represented by the genera Conorycthes and EHsthonyx.
Esthonyx approximates to the Tillodonta in having the enamel
of the incisors restricted in the lower jaw to the front of the tooth.
The lower molars closely resemble those of the Hedgehogs, but
several affinities are seen with Lemurs like Chiromys, and with the
genus Pelycodus. Conorycthes has two inferior incisors, and is repre-
sented by several species. Hsthonyx has three inferior incisors. It is

Upper

Lower

Upper

Lower

Esthonyx Burmeisteri.

remarkable for having the scaphoid and lunar bones separate, which
is not the case with existing Hedgehogs. Four species are known.
Another Bunotheroid suinarclen is named Mesodonta,—animals
characterized by approaching the Quadrumana in proportions,
but the rami of the mandible are separate, so that they also
approximate towards Lemurs. Several allied forms occur in the
Hocene of France, and it gradually became manifest that these

416 Reviews—Prof. Edward D. Cope—

animals differ, more than was at first supposed, from existing
types. But the author is unable to separate the group from the
Insectivora by ordinal characters. Eleven genera are comprised
in this tribe, among them being Microsyops with two species; and

Hyopsodus vicarius.
a. Premaxillary and maxillary. 64. Mandible.
Tomitherium closely allied to Adapis of Cuvier, but having two incisor
teeth instead of three. Zomitherium is an animal with slender limbs
and elongated femora, and the limbs generally have much of a quad-
rumanous character, and these resemblances are supported by those
of the lower jaw and teeth; but in the form of the humerus there
is resemblance to Lemurs. The only species is T. rostratum. Pelycodus

Anaptomorphus homunculus. N
a, b. Side views. c. Fromaboye. d. From below.

is distinguished from Tomitherium by having the third trochanter
in the middle of the shaft; and it has two roots to the second pre-
molar. Other characters are shown in five species described. Sarco-
lemur is an allied genus, distinguished by having acute cusps on the
heels of the true molar teeth. Hyopsodus is known from the man-
dibles of five species, and is distinguished by the simple inner tubercle,

with cusps at the angles of the heels of the molars.
The Prosimiz are distinguished from the Mesodonta by having an
opposable hallux which does not exist in the genus Pelycodus. ‘The
author states that Chiromys represents a primary division of the

Tertiary Vertebrata of the West. 417

Bunotheria, with a position between the Prosimiz and the Tillodonta.
There are probably three families of these Hocene Lemuroids, but
there is some uncertainty as to whether the allies of Adapis belong
to this or to the preceding group, so that the author limits his de-
scription to the Mixodectide and the Anaptomorphide.

Mixodectes is only known from mandibles, so that some uncer-
tainty exists as to its systematic position as well as its dental formula,
and the anterior teeth may be incisor, canine, and premolar, or the
incisor tooth may be absent. Two species are known. Cynodon-
tomys is also founded on mandibles; and Anaptomorphus complete
the family. The latter genus, of which we give figures of the
natural size, has large well-defined orbits. There is no sagittal crest,
and the temporal ridges are well defined. In many ways the
cranial characters approximate towards the Lemur Tarsius, yet the _
dental formula agrees with the Indrisinz, but no known Lemur has
premolar teeth with similar interior lobes and cusps, which resemble
those of the higher Monkeys and Man. The small size of the canines
is quite human. The cerebral hemispheres and brain are not smaller
than in the genus Tarsus or in typical existing Lemurs. From the
way in which quadrumanous and definite lemuroid characters are
combined, the author suggests that this type may represent the

Anaptomorphus emulus. Left mandible twice nat. size.

family from which true Monkeys and Men were developed. The
European type which most closely resembles this is Mecrolemur ;
but in that genus the two inferior premolars have but one root.
Anaptomorphus emulus was about as large as a Marmoset. A. homun-
culus is founded on the cranium. It was rather smaller than Tarsius
spectrum, and is thought to have been nocturnal; with feeding
habits like the smaller Lemurs of the Malay Islands and Madagascar.

The Creodonta is a large division of Mammals with the scaphoid
and lunar bones separate, narrow cerebral hemispheres having very
large and exposed olfactory lobes; while the ankle joint is generally
not trochlear. The separation of the scaphoid and lunar bones in
the carpus is a distinction from the Carnivora, yet the articulation of
the lower jaw with the squamosal bone is transverse, as in Carnivores.
The ilium is suggestive of the Insectivora and Marsupials. The
femur has a third trochanter. The astragalus articulated with the

DECADE III.—VOL. III.—NO. IX. 27

418 Reviews—Prof. Edward D. Cope—

cuboid and navicular bones. There were five toes on the hind feet,
in which the terminal digits are compressed and sharp. On the
whole, in the limited number of incisor teeth it approaches the In-
sectivora; it has many affinities with the Prosimiz and some affini-
ties with Lemurs, and is more distantly connected with the Carnivora.
The Creodonta differed from the Carnivora in the small size of the
limbs as compared with the head. Many of the species are thought
to have been aquatic. In Europe the group is represented by such
types as Arctocyon, which has commonly been regarded as a Marsu-
pial. In this suborder six families are included, comprising about
twenty-seven genera. Among these genera the author would look
for the ancestors of the existing Carnivora. The genera with marked
inner cusps and tubercles to the molar teeth are nearest to the
Marsupials. The genera without internal tubercles to the molars
are regarded as ancestors of the Hyznodontidz ; the family Miacide
are the forerunners of the Dogs; and the family Oxynidz were
the forerunners of the Cats. It will thus be seen that this large
group is worthy of careful study. The genus Ictops agrees closely
with Didelphys; but there are only three upper incisors, and the
angle of the mandible is not inflected. Peratherium agrees in dental
characters with Didelphys, and is only retained until the complete
dentition is known. Triisodon is characterized by the simplicity of
the fourth inferior premolar, and the rudimentary anterior cusps
of the molar teeth; from a study of its teeth the author concludes
that the posterior milk molar of Diphyodonts is a permanent tooth
in the Marsupialia. Four species exemplify the characters of this
type. Deltatherium is a genus which has in the lower jaws two
tubercular sectorial teeth, and a third behind them with a long heel.
It has three premolars and a well-developed canine. The dentition
is similar to that of the Opossums. Didelphodus differs from Delta-
therium in having an additional premolar in the lower jaw.

Stypolophus is represented by ten species. 8S. viverrinus is about
the size of the domestic Cat. Its skull is remarkable for the lachrymal
bone not extending posterior to the large lachrymal foramen. The
genus is found in the Phosphorites of France, but the author does
not follow Gaudry in uniting it with Proviverra, because the fourth
upper premolar has an internal cusp and an external cusp, flanked
in front and behind by a basal heel.

The Miacide comprise two genera, Miacis and Didymictis. Miacis
is conspicuous for its canine characters, among which marsupial
affinities are said to be no more prominent than in the case of other
Creodonta ; while Didymictis makes an approximation towards
Oxyena in its dentition. It is well represented by seven species.
The Oxyzenid comprise Pterodon, Protopsalis and Oxyena. Characters
of the skull are suggestive of Cats, but the head was larger and limbs
smaller than in true Carnivora, and they rather resemble the Car-
nivorous Marsupials in proportions. This type is supposed to have
been aquatic. Mioclenus comprises about eight species, known
from their dentition, which affiliates the genus to Arctocyon; but it
is distinguished by the single tubercle on the inner part of the crown

Tertiary Vertebrata of the West. 419

of the upper molars. Enough of the skeleton of M. ferox is known
to show that its nearest living ally is probably Thylacynus ; but it
differs from Marsupials in having a patella. It is about as large as
a Sheep. The remaining American genera of Creodonts are Dissacus,
Sarcothraustes and Mesonyc. The latter genus has some resemblance
to Hyenodon, but more to Amblyctonus. ‘The claws are flat like those
of Seals; but the structure of the ankle suggests that the type was
not exclusively aquatic. Mesonyxz is thought to have lived on Turtles.

M. ossifragus was as large as a large-sized American Black Bear
with the fore-limbs much shorter than the hind-limbs, giving much
the aspect of a huge Rabbit, except that the tail was long. It was
one of the largest Hocene flesh-eaters.

In this review we have attempted to give some idea of the varied
organization comprised in the Bunotheria. The conception of this.
gcoup is the most original contribution to mammalian classification
which has been made for a long time. The group is almost as diffi-
cult to realize, as would be a conception of the Marsupialia, if Marsu-
pials were only known in a fossil state. Some exception may be
taken to the term order, by which the Bunotheria is indicated, for
the group is rather a lower division of the placental subclass ; which
the author would compare to the Marsupialia in the variety of
organization it includes, while he believes it to have developed
simultaneously with the Marsupials, or even to have been an older
group. The classification has necessarily grown out of the affinities
which the described families of Mammals have with each other,
rather than with surviving groups; and although we cannot pro-
nounce a decided conviction on the importance of this great general-
ization without an examination of the specimens on which it is
founded, the principles on which it is evolved are sound. If we
recognized the Creodonta and other groupsas allied to existing orders
of Mammals, but distinguished by their smaller brains, and less
specialized organization, then the existence of the Bunotheria becomes
not only a convenience in classification, but a generalization which
will direct research. H. G. SEELEY.

(To be continued.)

IJ.—Catatocve oF THE BuastorpKaA IN THE GeroLocicaL DEpart-
MENT OF THE British Musrum (NaturaL History), WITH AN
Account oF THE MorpHoLtocy anp Systematic PosiTIoN OF THE
GROUP, AND A REVISION OF THE GENERA AND Sprctes. By
Ropert Erurings, Jun., and P. Herpert Carpenter, D.Sc.,
F.RS., F.L.S. 4to. pp. xiv. and 322. Illustrated by Twenty
Lithographic Plates and Twelve Woodcuts. (London, 1886,
Printed by Order of the Trustees.) Price 25s.

E know not whether it be due to the beneficial effects of trans-
plantation, but there has certainly been a steady issue of
publications in connection with this Department since its removal, in
1880, from Great Russell Street, Bloomsbury, to ie new soil of
Cromwell Road.

490 Reviews—Etheridge and Carpenter—

A penny Guide to the Geological Galleries appeared on their re-
opening to the public on 19 April, 1881, followed by an illustrated
edition in 1882 (price threepence) ; a third followed in 1884; and
a fourth edition (price fourpence) in 1886. Of the three earlier
editions altogether 11,284 copies have been sold. A Guide to the
Fossil Fishes appeared in 1885 (price threepence). A Catalogue of
the Fossil Foraminifera, by Prof. T. Rupert Jones, F.R.S. (8vo.),
appeared in 1882 (price ds.). A Catalogue of the Fossil Sponges,
by Dr. G. J. Hinde, F.G.8., 4to. with 38 plates (price 30s.), in 1884.
A Catalogue of the Fossil Mammalia (8vo.), Part I., by Richard
Lydekker, B.A., F.G.S., was issued in 1885 (price 5s., with thirty-
three woodcuts); Part II. also in 1885 (price 6s., with thirty-nine
woodcuts) ; Part III. in 1886 (price 4s., with thirty woodcuts) ;
(Part IV. we are informed is now passing through the press). A
Catalogue of the Palaeozoic Plants in the Geological Department, by
Mr. R. Kidston, F.G.S. (8vo. pp. 288, price 5s.), appeared in 1886.

The present work was commenced by its authors some years since,
but their task was delayed by the necessity to collect materials which
might serve to illustrate in detail the minute structure of this curious
and extinct group of Echinodermata. They were soon fortunate in
obtaining the co-operation of Mr. Charles Wachsmuth, of Burlington,
Jowa, a gentleman who has devoted some twenty-five years to the
collection of Crinoidea from the Carboniferous rocks of North
America, and who has also published several important memoirs on
these organisms. With his aid, and that of numerous other friends
in Europe and America, the authors have been enabled to examine
probably the largest and most instructive collection of these organisms
ever brought together, thus rendering the comprehension of their
minute anatomy comparatively easy, and giving one confidence in the
interpretation which they offer of each detail of their structure.

With regard to the systematic position of the Buastorp#a, one of
the authors (Dr. P. Herbert Carpenter) has had peculiar advantages
in approaching the subject, from his previous studies of the Crinoidea
collected by the “ Challenger” expedition ; whilst both authors have
long and patiently studied the fossil forms, and have endeavoured
by the examination of numerous remains and by the preparation
of very many sections, exhibiting internal structure, accurately
to work out the morphology of this obscure and but little understood

roup.
: The position of the Blastoidea in relation to the rest of the
Echinodermata has long been a subject of grave discussion ; but the
leading authorities are now agreed in giving the Blastoids a position
as a group equivalent in rank to the Brachiate Crinoids and the
Cystids, or to the Urchins and Starfishes.

Blastoids with stems appear to be extremely rare, although there
is little doubt that the great majority were stalked forms. Indeed
the authors figure several examples (see plate iii. fig. 16; pl. v.
fir. 25; pl. vi. fig. 28; and pl. xvi. fig. 7) showing the remains of
stems. But the stem in Granatocrinus is of moderate size compared
to the diameter of the flat basal disc of which it occupies the centre.

In Pentremitidea, Orophocrinus, Cryptoblastus, and Troostocrinus

Catalogue of the Blastoidea. 421

the basal cup is elongated and tapers elegantly downwards until its
narrow lower end rests directly upon the first stem-joint, which is
sometimes seen still united to the base. One Pentremite has been
obtained by Mr. Wachsmuth, in which the stem terminates below
in a branching root like that of the Bourgueticrinide: whilst three
genera of Blastoids, namely, Pentephyllum, Eleutherocrinus, and
Astrocrinus, appear to have had no stem in the adult state, whatever
may have been the case during their early life.

The following definition of the Penmatozoa' (under which name
the stalked Hchinodermata are classed by the authors) will probably
give the leading characters of this difficult group more clearly than
any words of our own :—

“Phylum Ecuinoprermata, Branch Pretmatrozoa. Echinoderms
which are fixed either permanently or temporarily by the middle of
the aboral surface. A jointed stem containing a neuro-vascular axis
is usually present, but may be lost when maturity is reached ; or, in
the case of a few sessile forms, remain altogether undeveloped. The
apical system consists of a dorsocentral plate, basals, and radials,
with the frequent addition of under-basals and interradials. These
plates form a cup, which either simply supports, or more or less
completely encloses, the visceral mass, and often bears jointed
appendages—the arms and pinnules.

Czy

LL kL Leb dddaaa

|

Fic 1.—Diagram of Troostocrinus Reinwardti. A. the anal side. B. the summit
view. The radio-deltoid sutures are shown by rather darker lines.

«An oral system, which is to some extent a repetition of the apical
system, and consists of a central plate, basals, radials, and inter-
radials, is developed to a very variable extent above the actinal sur-
face of the larva. It may be (1) altogether resorbed ; (2) persist as
basals only which cover the peristome ; or (8) reach a high state of
development so as to form a complex vault or tegmen calycis covering
in the whole visceral mass. The anal tube openson the oral surface,
but is sometimes in close relation with the calyx-plates.

“The water-vascular ring does not communicate directly with the
exterior, and the lateral branches of the radial vessels (when present)
are respiratory, but not locomotor in function.”

1 From wéAua, meAuaros, stalked, and (doy, animal.

422 Reviews—Etheridge and Carpenter—

“Crass Buastorpra.—Armless Pelmatozoa of a pyriform, clavate,
ovate, or globose shape, which usually exhibit a very perfect radial
symmetry. Base monocyclic, of two large plates and one small one,
the latter being always in the left anterior interradius, Fig. 2. II. (A-B).
Five radials, more or less deeply incised by the ambulacra, and five
interradials which rest on them and bound the peristome, one of them
being pierced by the anus. For view of summit, see Fig.1,B.p.421.

Ambulacra fringed on each side by a single or double row of
jointed appendages, which are in close relation to the side plates.
These rest on or against a subambulacral lancet-plate, which is
pierced by a canal that lodged the water-vessel and unites with its
fellows into a circum-oral ring. .

Hydrospires arranged in ten (or rarely eight) groups which are
limited to the radial and interradial plates ; their slits are parallel
to, and more or less completely concealed by, the ambulacra, often
opening externally through pores at their sides, and also by five or
ten openings round the peristome. Neither hydrospires nor ambu-
lacra extend below the basiradial suture.

Peristome naturally concealed by a vault of small plates, which
rarely exhibit any definite arrangement, and are continuous with
the covering-plates of the ambulacra.”

From the foregoing definition it will be seen that the Blastoids
differ in certain important points from other Pelmatozoa, notably in
the perforation of the lancet-plate, ‘‘of which we have as yet no
knowledge whatever in either Crinoids or Cystids. The absence of
under-basal plates and the constant presence of five interradials
(one of which is divided in Eleacrinus), lastly the constant but
peculiar trimerous symmetry of the base, only observed in the rare

|
i
@ Anus
7

Fie. 2.—Diagram showing the arrangement of the basals inI. Platycrinus, and II. in
the Blastoids. A, B, C, D, E, the five radii of the calyx. , the small azygos basal.
y, 2 the two larger basals. d... . d, the dorsal axis. 7... 7, the radial axis,
in which the anus is situated. The arrows show the (probable) direction of the
spirally-coiled digestive tube.

Catalogue of the Blastoidea. 423

Cystid, Cryptocrinus cerasus, and possibly in one Crinoid (Stephano-
crinus). Many Paleocrinoids have a trimerous base, but according
to Wachsmuth and Springer (‘Revision of the Paleocrinoidea,”
pt. ii. 1885, p. 10), the small plate is always in the right anterior
interradius (A—E). (See Woodcut, p. 422, Fig. 2, I.)

The calyx of many Blastoids is marked by very well-defined
ridges, which start from the bottom of the basal cup and extend
upwards until they meet the radial lips at the distal ends of the
ambulacra. The general arrangement of these ridges is the same in
all Blastoids, and is perhaps best studied in Stephanocrinus in which

type they are very strongly marked (see Woodcut, Fig. 3, infra).

W) anus
it

Fic. 3.—Diagram to show the position of the ridges (1-8) on the three basals
and the five radials (4, B,C, D, £) of Stephanocrinus angulatus (modified from Roemer).
(The lettering of the plates is the same as in Fig. 2.)

Lastly we may notice the very symmetrical grouping of the
hydrospires. ‘‘ These organs occur in most Cystids, and perhaps even
in some Crinoids, but we know of no member of either group in
which their arrangement is at all like that which occurs in the Blastoids.
In this class they are restricted to the radial and interradial plates,
where they lie with their slits parallel to the ambulacra, and except
in the genus Codaster, there are always five interradial pairs of
hydrospire-groups. No Cystid whatever presents anything like this
regular distribution of the hydrospires, which often extend down on
to the basals, and even on to the under-basals, when such are present.”

‘Considered as a whole, the Blastoids have the most regularly

424 Etheridge and Carpenter—Catalogue of the Blastoidea.

constructed calyx of any Pelmatozoa, and in fact of any Echinoderms.
Under-basals may occur in all the brachiate forms, while the basals
of Crinoids may vary in number from two to five, and the develop-
ment of the interradials varies extremely among the different groups.”

(p. 119.)

There is a persistent number of thirteen plates in the Blastoids,
with the single exception of Eleacrinus, which has the posterior
deltoid divided into two by the anal plate; and with the exception
of three genera, Eleutherocrinus, Astrocrinus, and Pentephyllum, the

UPPER CarBON-
EcHINODERMATA. Rpae eee DEVONIAN. || pEROUS,
Ht os a :/e]) . a| .|q/=
Branch PELMATOZOA. 3 S Si4 = 2/2) S| /8/8
Class B s8) 2 ESSE lee eg
ass BLASTOIDEA. AO) Sla| al Eye oO] o
Fin Bel 0 Js Jn | 1 A
Order RecuLAREs, E. and C.
PENTREMITIDZ, D’Orb.
Pentremites, Say ... 1.0 0. «| 49 900 Biialla sel Belltyl lage 354] 23 {Ioa9|boo/aac
Pentremitidea, D’Orb. ... ... ...| 18 nce P| 8 || 23/5 I0001| £5 [[loadlooollaoq]|
Mesoblastus, H. and C.... ... ...| 7 204 Psa ool Bs kno aoe 203i els [le loo
TROOSTOBLASTID#, H. and C.
Troostocrinus, Shumard... ... ...| 2 “ betel Kohl Sees PL B® flocolloodllooe
Metablastus, E. and C.... ... ...| 7 ale oball lloos|ooall & {fll es Hooellooallac
Tricelocrinus, M. and W. See liero Bes eal eee eel eae eae =96l[| ¥|laoolbe
Nucteopiastip#, KE. and C.
Eleacrinus, Roemer Se acacte hoc aust) ga0 sg alee Sellaee tee Son | sedliacolisealloac
Schizoblastus, KE. and C.... ... ...| 10 200 Falcoclemel selon spall) 3 |e llocdlloo
Cryptoblastus, K. and C. ‘ 3 000 pie eel lgeel yet ee soll 4 floc
Acentrotremites, K. and C. ... 1 COE | liccolBacyIaaeliace| lao Meelis
GRANATOBLASTIDE, E. and C.

Granatoc inus, Troost ... 10 P e | ok
Heteroblastus, KH. and C. 2 0 Weaallacdfaoe bellies
CopAsTERID#, E. and C.
Codaster, McCoy ... ... 15 Re calles dlocelfl {lie
Phenoschisma, H. and C. ... 7 ea tepces all =. IPP ie,
Orophoerinus, von Seebach ... ase enh se Io eee ents ollea | beryl} ys
Cryptoschisma, K. and C. PANG ete ol illo sa| baa) loae dll 5 [Ileos)Jas0 coc
Order IrREGULARES, E. and C.
ASTROCRINIDZ#, T. and T. Austin.
Astrocrinus, T. and T. Austin ...| 2 ane sodjcodfoonocullaed|lacalllasa|l es llace
Eleutherocrinus, Shum. and Yand. | 3 000 Pall dalleciatisaet day
Pentephyllum, Haughton a, a aah

1
Total ... .../162

Reviews—R. Lydekker—Fossil Mammalia. 425

contour of the calyx is always perfectly symmetrical, consisting as
it does of five equal and similar radials, and five deltoids of the

same nature.

The foregoing table (from p. 186) is extremely valuable as
showing the Distribution of the Genera of the Blastoidea in Space
and Time. We have added a column with the probable number
of species referred to each genus.

From the foregoing list, it will be seen that only two (American)
generic forms, Zroostocrinus and Codaster, occur in the Upper
Silurian, about six or seven genera in the Devonian; whilst the great
majority occur in the Carboniferous series both in England and in
America.

A careful description of each species is given by the authors,
illustrated by twenty quarto plates and 399 figures, most beautifully
and accurately drawn by Messrs. C. Berjeau and P. Highley, re-
quiring not only great artistic power, but a large store of patience
in making out such minute and very elaborate details.

All Biologists who are interested in the Echinodermata must feel
grateful to the authors of this very elaborate and exhaustive Memoir,
which clears up so many points in the anatomy of this ancient class,
that has hitherto been but very imperfectly understood.

We trust they may be so well satisfied at the favourable reception
which this volume is sure to meet with, that they will take up and
work out in the same earnest and painstaking manner the still more
important and interesting Brachiate division, which has remained
far too long neglected by paleontologists.

IJI.—Caranocus or THE Fosstn Mammatia 1n THE British Museum
(NaturaL History), Cromwett Roan, §8.W. Parr III.’ Con-
TAINING THE ORDER UNGULATA, SUB-ORDERS PrRISSODACTYLA,
Toxopont1a, ConDYLARTHRA AND AmBiypopa. By R. LyDEKKeEr,
B.A, F.G.S., ete. S8vo. pp. xvi. & 186. (London, 1886, printed
by Order of the Trustees.)

HE present part of Mr. Lydekker’s Catalogue of the Fossil Mam-
malia completes the order Uneuxata with the exception of a
single group, the Prozoscipua. This group, it is announced, will
form Part IV. of the Catalogue, which is now in the press. Although
embracing only a small section of the Mammalia, this part is of
special interest to the paleontologist ; for out of the eighty species
recorded in its pages, all are extinct save four, namely, Tapirus
Americanus, Equus caballus, Rhinoceros sondaicus and Rh. unicornis.
Furthermore, of the seventy-eight extinct species, no fewer than
thirty-two species, belonging to as many as twelve genera, date back
to the Hocene Tertiary formation, namely, Zophiodon (5 species) ;
Hyracotherium (3 species) ; Pachynolophus (4 species) ; Palgotherium
(8 species) ; Anchilophus (2 species) ; Rhinoceros (2 species); Cadur-
cotherium (1 species); Periptychus (1 species); Haploconus (1 species);

1 Part II. was noticed in the Grotogican Macazine, April, 1886, pp. 175-177.

496 Reviews—R. Lydekker—Fossil Mammaiia.

Coryphodon (1 species); Tinoceras (2 species); and Dinoceras (2
species )—represented in the collection.

The genus Lophiodon nearly approaches the Tapir and Rhinoceros
in the structure of its teeth. Like the Tapir the lower true molars
have simple transverse ridges, but the premolars are more or less
longitudinally tuberculated, and in this respect it differs from its
near ally, the Palaotherium, i in which the whole series of the lower
molars are longitudinally bi-crescentic in form. It had also, like the
Tapir, which it preceded in geological time, four toes on the fore-feet
and three on the hind-feet.

Many species are enumerated, ranging in size from the Pig to the
Rhinoceros. Their remains have been met with in several localities
in Europe, and also in this country, in Eocene Tertiary strata.

Its dentition may be expressed as follows :—

Incisors 3, canines +, premolars 3, molars $, x 2 = 40.

Hyracotherium was a small animal, about the size of a Hare,
principally known in a fossil state by its dentition. Its remains are
comparatively rare and have been found in the Lower Eocene
(London Clay), Herne Bay; at Kyson in Suffolk; and also as a
derived fossil from an older deposit in the Suffolk Crag.

Pachynolophus is an allied genus of small animals, whose remains
are only found in Kocene deposits. Four species are represented in
the collection by teeth and jaws from France and Switzerland. The
dentition is complete, viz. :—

Incisors 3, canines +, premolars #, molars 3 x 2 = 44.

Palotherium is well represented in the Aotineon: It was a Tapir-
like animal, first described by Cuvier, from skulls, teeth and bones,
of numerous individuals, representing several species, which were
discovered in the Gypsum quarries (Upper Eocene) of Montmartre,
Paris.

Paleotherium magnum was as large as a Horse, four or five feet in
height ; whilst P. curtum was about the size of a Hog. They all had
a short fleshy snout or proboscis, like the Tapir; but, unlike the
Tapir, they had only three toes on each foot, whilst the Tapir had
four toes on the fore-foot.

Mr. Lydekker (following Prof. Flower) treats Paloplotherium as
identical with Palgotherium. P. annectens was about the size of a
Sheep and is well represented in the collection from the Upper
EKocene of Hordwell, Hants, and from Vaucluse in France.

Anchilophus, a small Paleotheroid, is represented by jaws and teeth
from the Upper Hocene at Bembridge, Isle of Wight, and from
Vaucluse and Caylux in France.

The Rhinoceroses are now all placed in a single genus, which
includes five or six known living species. No fewer than twenty-four
species are represented by fossil remains in the collection, mostly
from Pleistocene, Pliocene or Miocene Tertiary deposits; but two
forms, Jth. croizeti and Rh. lemanensis, occur in the Upper Hocene
phosphorites of France, thus carrying this remarkable living genus
back in time to the older Tertiaries. Four other genera, of which at

Reviews—R. Lydekker—Fossil Mammalia. 427

present we possess only imperfect materials for study, are provision-
ally referred to the family Rhinocerotide, namely : Hyracodon, Cadur-
cotherium, Homalodontotherium and Elasmotherium. Of these four
genera, one only (Cadurcotherium) dates back to the Eocene period.

Periptychus and Haploconus are both Lower Hocene genera from New
Mexico in North America. They are characterized by the grooved
and ridged sculpture of the teeth. They form a part of the sub-
order ConDYLARTHRA, in which are placed a number of those primi-
tive Mammals having a bunodont or lophodont type of cheek-
dentition, foreshadowing both the Artiodactyla and Perissodactyla ;
there are usually five digits in both the manus and pes, the terminal
phalangeals being acuminate. The best-preserved example of the
family is the genus Phenacodus, of which a figure was given in the
GeoLocicaL Magazine for February, 1886 (Plate II. p. 49).

Under the suborder Ampiypopa is placed the remains of the
genus Coryphodon, from the Lower Eocene of Harwich, Essex, and
from Dulwich, near London. It also occurs in the Hocene of France
and North America.

Coryphodon was the largest of the early Eocene Ungulates, and the
relative smallness of its brain, together with its five-toed feet, which
resemble in structure those of the Dinocerata, indicate some affinity
to that group, which it also preceded.

The section Drinocerata is included in the same suborder, and
completes the series of Hocene Mammals represented in the collection.

We are indebted for our very perfect knowledge of the genera
Tinoceras and Dinoceras to Professor O. C. Marsh, whose labours in
exploring the Hocene Tertiary deposits of the Wyoming Territory
have opened up an entirely new chapter in Tertiary paleontology.

For a full account, with figures, of these interesting genera, see
the Grotocicat Magazine for May, 1885, Decade II]. Vol. II. pp.
212-228 (with 18 Woodcuts).

The fore and hind limbs had feet with five well-developed toes,
each terminating in a hoof; the femur and tibia were placed
vertically in a line, as in the hind-leg of the Elephant. The nasal
bones were elongated, having two small pre-nasal bones in front of
them ; the animal does not appear to have been furnished with a
proboscis.

The most striking feature is the skull, which is surmounted by
three pairs of rounded protuberances or horn-cores, which were pro-
bably enveloped in horny sheaths. There are no upper incisors,
but the upper canines are developed into large and powerful flattened
tusks, directed downwards, and protected on each side by the broadly-
expanded margin of the lower jaw.

These early Eocene types have so important a bearing upon the
question of the derivation of our existing Mammalian fauna, that we
cannot but welcome every addition to our knowledge concerning
them, and we have to thank Mr. Lydekker for this further instal-
ment of his Catalogue, and to express the hope that we may soon
have it before us in its completed form.

428 Reviews—Guide to Geology and Paleontology.

IV.—British Musrum Guipe to tHE Department oF GEOLOGY
AND Panmontontocy. 4th Hdition. (1886, Printed by Order
of the Trustees.)

N this neat little volume (which contains 117 pages of text and
49 excellent woodcuts) the amateur palzontologist can obtain

for the small consideration of fourpence a concise synopsis of the
chief divisions of the Animal Kingdom. The greater portion of the
book, which has been written by Dr. Henry Woodward, F.R.S.,
Keeper of the Department, with the aid of his valuable Assistant the
veteran Mr. William Davies, F.G.S., of the same Department, is
devoted to the Vertebrata, and since the Fossil Fishes have been
treated of in a separate ‘Guide,’ attention is mainly concentrated on the
Mammalia, Aves, and Reptilia; the Amphibia coming in for a more
limited notice. The Mammalia are divided into the following 12
orders :—Primates, Carnivora, Insectivora, Chiroptera, Dermoptera
(Galeopithecus), Rodentia, Ungulata, Sirenia, Cetacea, Hdentata,
Marsupialia, and Monotremata. By far the largest space is assigned
to the Ungulata, which is split up into the Proboscidea, of which the
Museum contains the finest collection in the world ; the Hyracoidea,
at present unknown in the fossil state; the Amblypoda, containing
the Coryphodon; the Dinocerata, represented by a fine series of casts
presented by Prof. O. C. Marsh ; the Condylarthra, a primitive group
of five-toed forms from the Eocene of N. America; the Toxodontia,
which includes the peculiar Rodent-like Typotherium of 8. America ;
the Perissodactyla; and the Artiodactyla. We may especially notice
in this order the excellent figures illustrating the difference in the
structure of the molars of the African and Indian Hlephants, and
also those showing the characteristic dentition of the existing Hippo-
potamus and of the extinct species from the Siwalik Hills of India.
A special feature in the Ungulate collection is the series of skulls of
the peculiar group of ruminants from the Pliocene of India and
Greece, comprising the Sivatherium, Bramatherium, Hydaspitherium,
and Helladotherium, which appear to connect the modern Deer with
the Antelopes, and are more or less closely related to the existing
Giraffe. The Museum possesses the type skull of the first-named
genus, while of the second and third genera casts of the skulls have
been respectively procured through the courtesy of the Council of the
Royal College of Surgeons and the Director of the Geological
Survey of India. Full justice is also done in the work to the splendid
collection of Edentata from the Post-Tertiaries of South America,
and of Marsupials from those of Australia; and we are glad to
notice a good figure of Sir R. Owen’s Tritylodon from the Secondary
strata of South Africa, for which we believe Dr. Woodward is in-
debted to the courtesy of Prof. E. D. Cope, of Philadelphia. The
remarkably fine skeleton of Steller’s Sea-Cow (Rhytina), which was
recently acquired for the Museum, is also figured, and compared with
that of the existing Manate. Seven pages are devoted to the class
Aves, and include figures of Archgopteryx, Hesperornis, Odontopteryz,
and Dinornis. Save in the table of contents, no mention is, indeed,
made of the subdivisions of the class, and this is perhaps wise,

Reviews—Guide to Geology and Paleontology. 429

since it is very difficult to make its divisions accord in importance
with those of the other vertebrate classes; we think, however,
that it will be advisable eventually to rank the divisions of
Carinate, Ratitee, and Saurure as orders, and to relegate to the
rank of suborders the so-called orders into which the Carinate are
divided by students who confine their attention to existing forms.
Pages 70 to 87 are assigned to the Reptilia, and we note with
satisfaction the classification which has been adopted in this difficult
class, as being one of the best that has come under our observation.
The orders adopted are the Pterosauria, Crocodilia, Dinosauria,
Anomodontia, Ichthyosauria, Ophidia, Lacertilia, Plesiosauria, and
Chelonia. The divisions of the second order proposed by Prof.
Marsh are adopted with a subordinal value; while the Anomodontia
includes the Theriodontia, Dicynodontia, Rhynchocephalia, Crypto-
dontia, Endothiodontia, and Placodontia. According to this arrange-
ment it will be necessary to retain Prof. Dollo’s group of the Simz-
dosauria for Champsosaurus, since that genus seems more distinct
than Endothiodon from the typical Rhynchocephalia ; we should, how-
ever, have preferred to have placed the last-named genus in closer
proximity to that suborder. In the Lacertilia the Mosasauride are
ranked merely as a family, which avoids the necessity of the intro-
duction of Prof. Cope’s Pythonomorpha. In this class there are
figures of Rhamphorhynchus, Pterodactylus, Dimorphodon, Iguanodon,
Megalosaurus, Ichthyosaurus, Plesiosaurus, Megalania, and Chelone.

Skeleton of Iguwanodon Bernissartensis, Boulanger (restored after Dollo) from the
specimen in the Brussels Museum.

The Invertebrates occupy pp. 92-107, but as the notice of these

classes is necessarily brief, we need not refer further to them on this

occasion. The last page of the text mentions the extensive collection

430 Reports and Proceedings—Zoological Society of London.

of Fossil Plants, which is not yet arranged ; and also calls attention to
the ;valuable series of type collections now in course of arrangement.
Since the latter includes the collections of Dr. William Smith, Mr.
S.<V. Wood, J. and J. de Carle Sowerby, Mr. F. E. Edwards, and
Dr. Thos. Davidson, their interest to all paleontologists must be
of the greatest. The volume concludes with an excellent plan of
the Paleontological Galleries and a well-arranged Index.

With the publication of this series of popular “ Guides” for the
nonscientific, and of the “Catalogues” for the scientist, the British
Museum is rendering its unrivalled collections of the best possible
advantage to all classes of visitors ; ; and we beg to offer our hearty
congratulations to Dr. Woodward and his able coadjutors on the
successful completion of the present ‘ Guide” to one of the most
interesting branches of the whole collection.

Iss SOusyayS) VAIS b) IS 1S O\SE aI AID IFINKE TS.

>
ZooLocicaL Society or Lonpon.

June 29th, 1886.—Osbert Salvin, Esq., F.R.S., V.Pres., in the
chair.—The following communication was read :—

“‘Note on the Presence of a Columella (Epipterygoid, Parker) in
the skull of Ichthyosaurus,” by A. Smith Woodward, F.G.S. Com-
municated by the President.

In this paper, the author recorded the presence of a “columella”
(epipterygoid) in the skulls of several Liassic Ichthyosaurs in the
British Museum, and offered a brief account of the main features of
the bone. The communication was suggested by Sir Richard Owen’s
statement (Foss. Rept. Lias Form.” p. 96) that he had observed no
trace of the element in question in the British fossils; and the fact
became still more worthy of note, since Prof. Cope (Proc. Amer.
Assoc. Adv. Sci., vol. xix. p. 200) had already determined the pre-
sence of a columella in the skull of an American Ichthyosaur, and
this circumstance was evidently overlooked by Sir Richard Owen.
As pointed out by Prof. Cope, the bone is long and slender, with
expanded extremities ; and in the present communication the author
showed that it was a distinct element, although a suture at its upper
end in the American specimen appeared to be wanting. It was
further remarked that the lower extremity of the Ichthyosaurian
columella exhibits a striking resemblance to its homologue in Sphe-
nodon, in the fact that the expansion shows two distinct articular
facettes upon its inner aspect as is well seen in the specimen figured
in Hawkins’ “Book of the Great Sea-Dragons,” pl. 19, fig. 1. In
the living Rhynchocephalian genus, the articulation is contracted
both with the pterygoid and an inward extension of the quadrate ;
in Ichthyosaurus, however, its nature cannot yet be determined, and,
according to Prof. Seeley, there is no inwardly-directed process of
the last-named bone.

Erratum.—Geou. Maa. August, 1886, p. 341, legend to woodcut, for ‘‘ Interior,”
read Huterior.

CORRESPONDENCE. 431

—————— en

ON THE TERM NEOCOMIAN.

Str,—When my article on the use of the term Neocomian
appeared in this Macazinz, I felt conscious that I had provoked
a formidable antagonist, and when I saw Prof. Judd’s long letter in
the July Number, I felt like the captain of a frigate about to receive
the broadside of a three-decker; but it seems to me that the utmost
damage IJ have received is a few shot through my sails, and that the
hull of my little vessel is left perfectly water-tight.

A large part of Prof. Judd’s letter is devoted to showing that I was
mistaken in crediting him with being the first to apply the term
Neocomian to British strata, and he says that the author who had the
chief honour (as he esteems it) of introducing that term was the late
Mr. R. A. Godwin-Austen. Well, this is perfectly true. I admit that
Godwin-Austen was the first to use the term; in 1843 he employed
it for what we now call the Atherfield Clay of Surrey, and in 1856
he speaks of the ‘‘ Lower Greensand or Neocomian group;” but in
the first paper (Proc. Geol. Soc. vol. iv.) he correlated the Surrey
clay with the argile ostréenne of the Vassy section, and in the
second he makes the Lower Greensand of North Wilts correspond
with the Urgonien of D’Orbigny. Now subsequent researches proved
these correlations to be erroneous. Renevier and Marcou, writing in
1856 and 1858, showed that the English Lower Greensand was not
the equivalent of the Neocomien or of the Urgonien, but of the
Rhodanien and Aptien; consequently the use of the term in England,
having originated in a mistake, ought to have been abandoned.

So indeed it might have been but for the intervention of Prof.
Judd, who is certainly responsible for its revival in 1864, and for
urging its more extended application in 1870. His article “‘ On the
use of the term Neocomian” (Gon. Mag. Vol. VII. p. 220) was
written with the special object of recommending the adoption of the
term for the whole series of beds between the Gault and the
Jurassic strata, and of raising this series to the rank of an in-
dependent system. J maintain therefore that if Prof. Judd had not,
introduced this name for the second time, it is highly probable that
it would never have found a place in British nomenclature.

Prof. Judd next refers to Godwin-Austen’s arguments for the
Necomian age of the Lower Greensand fossils. I repeat that by the
increase of our knowledge these arguments have been shown
to be fallacious; of course the fossils of the Lower Greensand
resemble those of the Urgonien more than those of the Gault
and Chalk! if it were otherwise, we should class the Lower Green-
sand with the Upper and not with the Lower Cretaceous rocks.
If Prof. Judd cannot formulate a better reply to the arguments
adduced by me on p. 818 of this Macazinz, I think I may look upon
my case as proved.

I am told that “scientific names go through a struggle for
existence,” and that the fittest survive; maybe they do, but in my
opinion the name Neocomian is not yet out of the struggle, and has
not yet definitely found its proper place. Surely, Sir, geology is a

432 Correspondence—Rev. P. B. Brodie.

rapidly progressive science, and our nomenclature is always under-
going modification; old names must sometimes be limited or dropped,
and new names must be created as the progress of knowledge
demands. Why in point of fact Prof. Judd and I are actually dis-
cussing the desirability of dropping an old name (Lower Greensand),
and of finding another to take its place; he prefers to borrow a
foreign term and to extend its application ; I point out the objections
to this plan and prefer to use a new name altogether. Let us argue
the matter clearly and fairly, and then leave the readers of this
MaGaztne to decide between us, but I do not see why my opponent
should deprecate the idea of my ‘formulating a new nomenclature ”
for the Cretaceous rocks either in my private or official capacity.
Lastly, let me offer Prof. Judd my hearty thanks for drawing my
attention to the passage which he quotes from Dr. Fitton, and which
I had been careless enough to overlook. I am delighted to find my-
self anticipated by so great a master as Fitton, and to be relieved of
the responsibility of introducing a new name; it is remarkable that
Fitton should have foreseen the very want which has since arisen
and | feel that I shall have a much stronger case in referring to the
term Vectine or Vectian as_ his proposal, suggested in 1845, and
revived by myself in 1885. A. J. Juxes-Browne.
August 10,

ON A REMARKABLE SECTION IN DERBYSHIRE.

Sir,—During the meeting of the Warwickshire Field Club at
Matlock, we visited a remarkable sandpit at Longcliff, four miles 8. W.
of Matlock Bath, on high ground near Brassington. Our attention
was drawn to this by Mr. Howe, of Matlock, as one of the most
interesting geological features of the district. The section exhibits
a series of variegated and highly coloured sands and clays, here and
there containing a few pebbles of small size, chiefly of white quartz
and in places lignite. These are not pebble-beds at all resembling
the ordinary ‘Bunter pebble beds,’ nor do I remember any Bunter
section showing such a peculiar succession of variegated sands and
clays. They lie in a trough or hollow of the Carboniferous Lime-
stone, and there are several other smaller pits in the same neighbour-
hood and under similar conditions, though not sunk at present to
any great depth; at Longcliff the total thickness is thirty feet. The
sands and clays are of various colours, yellow, white and red, and in
some cases a dark vermilion, giving a very remarkable appearance
to the section. Lithologically they resemble the variegated sands
and marls in the Tertiary (Middle Bagshot) series, especially
at Alum Bay in the Isle of Wight; and the question is whether they
should be assigned to the Bunter or the Tertiary, and if they should
prove to belong to the later period, I believe it is the first remnant
of the kind recognized in Derbyshire. ‘The occurrence of lignite
leads to the possibility of this deposit being of Tertiary age: but of
course no absolute decision can be given without further investigation,
which Mr. Howe has promised to undertake. This pit was opened
after the visit of the Geological Survey to Derbyshire, so that the
section was not exposed at that time. P. B. Broprx.

Decade III. Vol. Ill. Pl. XI.

Geol. Mag. 1886.

AOU US ucake

ree

)

West, Newman & Co. imp.

del

W.K. del.
C. Knight lith.

Carboniferous Ostracoda.

4
SN
“ .
x
-
a. ; ne, cae
7 7 an! a < 7 iy | i

Geol. Mag. 1886. Decade III Vol. Tt Fe ar

N

TW ery wets

poe

W. K. del.

J.
EC. Knight lith.

Carboniferous Ostracoda,

THE

GEOLOGICAL MAGAZINE.

NEW “SERIESS DECADE IN VO Ii.
No. X.—OCTOBER, 1886.

Oren GaaNe As) Ase sees sess Se
ebeesee Je

I.—On some FRINGED AND OTHER OsTRACODA FROM THE CARBON-
IFEROUS SERIES.

By Prof. T. Rupert Jones, F.R.S., and James W. Krrxesy, Esq.
(PLATES! XI. anp XII.)

A YEAR or two ago we received from Mr. James Bennie, of the
Scottish Geological Survey, a washing of Lower-Carboniferous
shale from Plashetts, Northumberland, which was very rich in the,
remains of Ostracods. Among other species occurring therein was
a Beyrichia-like form, ribbed as in Kirkbya, and with a wide fringe

about the free margins of each valve.

About the same time Mr. Bennie kindly sent us another washing
from the Lower-Carboniferous series, Staneshiel Burn, Roxburgh-
shire, containing numerous examples of similar fringed and ribbed
carapaces.

Since then the same or nearly allied forms have been found by us
in material from other localities, chiefly in the lower portion of the
Carboniferous formation.

These forms, though evidently coming near to Beyrichia and
Kirkbya, can scarcely be placed in either genus, and we propose to
group them under the generic name of Beyrichiopsis.

With them we also place a fringed species (Pl. XI. Fig. 7) that
several years ago we found in an impure limestone or cement-stone
of the Calciferous Sandstone, at Billow Ness, in Fife. This species
has been referred to by us as identical with or nearly allied to
Beyrichia crinita, J. and K., in recent papers;” and it is evidently
the same as one of the forms from Plashetts, though in a different
state of preservation.

Lastly, we include B. crinita in the new genus, for, though as yet
but imperfectly known, it is a fringed species, and thus nearest to
the forms under notice.

Beyrichia radiata, J. and K., which has a curious marginal expan-
sion or plate, somewhat akin to the fringes of the present species,
we scarcely know what to do with, though we leave it in Beyrichia.

The following is a brief and provisional description of the genus.

1 These Plates have been drawn with the aid of a grant from the Royal Society
for illustrating fossil Ostracoda. ers
2 Quart. Journ. Geol. Soc. vol. xxxvi, 1880, p. 567; and Proc. Berwickshire

Nat. Club, vol. x. 1884, p. 328.
DECADE 111.—vVOL. III.—NO. X. 28

434 MM. Jones and Kirkby—Carboniferous Ostracoda.

BEYRICHIOPSIS, gen. nov.

Carapace-valves outlined and lobed more or less after the fashion
of Beyrichia; either unisulcate, with two ronndish separate lobes, or
with one subcentral and more pronounced lobe, defined by a faint
sulcus on one side and a deeper furrow between it and the swollen
posterior part of the valve. The anterior end rather the highest, as
in Beyrichia. Two or more thin, curved or sinuous, outstanding
ribs pass along the valves (as in some specimens of Kirkbya), one of
which is usually placed near the dorsal edge and developed into
a crest. The surface is smooth, punctate, or finely granulate. A
broad, fimbriate or spinous fringe extends along and a little outside
of the free margin of each valve; this and the ribs form the charac-
teristic features of the genus, so far as known.

1. BryRIcHIOPsiIs FIMBRIATA, Sp. nov. Plate XI. Figs. 3-10, and
Pl. XII. Fig. 5?

Valves ovate-oblong in outline, lobed, bearing two or more longi-
tudinal ribs, and with the free margins curiously fringed and spined;
height half the length, or less. The dorsal border is straight and
nearly three-fourths of the valve’s length; the ventral border is
almost straight or slightly incurved; the extremities are rounded,
the anterior being rather the highest. A large globose lobe or boss
occupies the posterior third (or more) of the valve; a much smaller
circular or ovate boss is dorsally placed near the anterior third ;
and a third, but slighter, swelling is sometimes developed in the
ventral region between those already named. A thin lamella-like
rib runs parallel and near to the dorsal margin; a shorter, though
similar, rib is usually present along the middle of the posterior lobe ;
and a third (more or less sinuous) traverses the ventral region of
the valve; all these ribs run out to nothing anteriorly, and end
abruptly posteriorly, often with curved points. At the antero-
dorsal angle of each valve, and a little outside of the exact margin,
there commences a broad and delicate wing-like fringe, directed
slightly outwards, and regularly marked with radiating lines or
grooves. This fringe extends round the anterior extremity to beyond
the centre of the ventral border, where (the groovings becoming
more pronounced) it gradually breaks up into a series of flattened
spines that extend, on the same plane, round the posterior extremity
as far as the postero-dorsal angle. Seen from above or below, the
carapace has a lobate-cuneiform outline, the anterior end being the
thinnest, and the posterior almost symmetrically rounded. Surface
apparently smooth. Length 3; inch.

Examples of this species vary very little except in relative height
and length.

The marginal fringe is never perfectly seen in testiferous examples,
—as might be expected from its delicate character, the valves having
lost it if at all knocked about before imbedment. Many specimens,
however, show it more or less imperfectly, so that synthetically a
very fair idea of it can be arrived at. At Billow Ness, where this
species is abundant on certain planes of the cement-stone before

——

MM. Jones and Kirkby—Carboniferous Ostracoda. 435

mentioned, the external impressions of the valves show this feature
very beautifully.

Pl. XI. Fig. 7 is an internal cast of a valve with the external im-
pression of the fringe.

Fig. 8 is a very fine testiferous example, from Staneshiel Burn,
with a well-developed and ornate crest, and a curious palmate
spine (?) near the postero-dorsal angle.

This species is always found in deposits of marine origin. At
Plashetts it is associated with marine fossils, besides other Ostracods
in abundance, such as Kirkbya costata, Beyrichia radiata, Leperditia
Okent, Cytherella valida, etc.

At Billow Ness it occurs along with Bellerophon decussatus, Mur-
chisonia striatula, Leda attenuata, Sanguinolites abdensis, etc., and
with Leperditia Okeni and other Ostracods.

Pl. XII. Fig. 5 represents a fringed form from Cultra, County
Down, Ireland, which probably belongs to this species, though the
crushed state and general bad preservation of the specimens leave
the reference doubtful.

Localities. — Calciferous-Sandstone series. Plashetts, Northum-
berland; Tweeden Burn, and Staneshiel Burn, Roxburghshire ;
coast to the west of Billow Ness, Fifeshire’; ? Cultra, County Down.

Carboniferous-Limestone series. Murrayfield Pit, Linlithgow-
shire; and Sunnybank Quarry, N.W. of Kirkcaldy, Fifeshire.

2. BryRIcHIopsis FoRTIS, sp. nov. Pl. XII. Figs. 1-3.
(Var. glabra, Figs. 1,2; Var. granulata, Fig. 3.)

Another fringed form, nearly related to jfimbriata, occurs in the
Lower-Carboniferous Shale at Staneshiel Burn, Liddlesdale. It is
larger than the latter, and, were it not for the marginal fringe and
longitudinal ribs, would have a very Beyrichian style of valve. We
have been in some doubt whether to consider it a variety of fimbriata
or a distinct species, but adopt the latter view, and describe it as
follows :—

Obliquely subovate, lobed, longitudinally ribbed, and with a
marginal fringe; height less than half the length. Dorsal border
straight and three-fourths of the valve’s length; ventral border
boldly convex ; extremities rounded, but with well-marked dorsal
angles, the anterior extremity oblique and larger than the other.
The posterior half of the valve is swollen and forms a large rounded
lobe, in front of which, and separated by a deep and narrow sulcus,
is a small oval boss; the ventral portion of the valve is tumid. A
thin, sinuous rib passes obliquely across the valve from near the

1 The thin limestone or ‘ cement-stone’’ at this locality is only about one foot
thick. It is a compact and very hard grey stone, showing scarcely a trace of fossils
as it occurs unaltered between tide-marks. A little higher up, where it runs into
the soil and a recent shell-bed (old beach), it becomes decomposed, especially about
the joints, and takes the character of a soft, yellow ochre, that is easily split up with
a pocket-knife or needle. The rock is then seen to be literally full of the remains
(casts or impressions) of Mollusca and the carapace-valves of Ostracods. The con-
trast of how much is to be seen in a piece of this rotten stone in comparison with
how little in a piece of the unaltered stone is most surprising and very instructive.

436 MM. Jones and. Kirkby—Carboniferous Ostracoda.

antero-ventral angle diagonally upwards, terminating abruptly, with
a downward bend, before reaching the posterior extremity ; another
long curved rib, commencing a little below the first, passes along
the ventral portion of the valve; and occasionally another appears
not far from, and parallel with, the ventral fringe; and near to the
antero-dorsal angle there is a short, curved rib, sharply pointed
behind. The free margin of each valve is ornamented with a radi-
ating fringe (and spines) similar in character to that of jfimbriata.
The surface in Fig. 3 is granulated (var. granulata). Length, 5 inch.

Good examples of this species have a granulated surface, but some
occur that are smooth (var. glabra, Figs. 1 & 2). In the latter state,
and particularly when the valves are rather worn, or flattened by
pressure, they simulate Kirkbya plicata, and are not always easy to
be distinguished from it.

The ribs vary a little in development. The small one near the
antero-dorsal angle is often absent; and that immediately below
occasionally extends across only the posterior half of the valve.

This species is, as already stated, nearly allied to B. fimbriata ;
but differs from it in its larger size, less elongated form, more
decided Beyrichian style of lobes, the granulated surface of its best
form, and the absence of the dorsal rib or crest of that species.

Localities.—Calciferous-Sandstone series. Staneshiel Burn and
Tweeden Burn, Roxburghshire.

3. BEYRICHIOPSIS CORNUTA, sp. nov. Plate sah Epica

From localities in the Carboniferous-limestone series (Lower) we
have a third fringed Beyrichia-like form. It is smaller than the
preceding species, has a spinose fringe all round the free margin,
possesses no ribs, but in their place has one or two large spines or
spikes projecting from each valve. Some of the specimens have
only a spine on the large posterior lobe or boss; others have one on
the anterior lobe as well. The surface is smooth; and the length is
from +4; to 4 inch.

We name this form cornuta, and include it in Beyrichiopsis on
account of its fringe.

It occurs at Linlithgow Bridge, Linlithgowshire ; Woodend Quarry,
Fifeshire; and Dun Quarry, Lowick, Northumberland.

é 4, BryRICHIOPSIS cRinITA, Jones and. Kirkby.

Beyrichia crinita, J. & K. 1884, eee Berwicksh. Club, vol. x. p. 322, pl. ii.

g. 10, 11.

This species was described by one of us (from specimens collected
by Mr. George Tate) in the Proceedings of the Berwickshire Nat.
Club, as above quoted. We have nothing to add to this, as no
additional specimens of it have been discovered. It is from the
Lower Carboniferous rocks of Alnwick Moor, Northumberland.

Prof. Emmons notices and figures a fringed Beyrichian form from
the Trenton Limestone, of New York State, in his ‘“‘Manual of
Geology,” 2nd edit. 1860, pp. 95 and 100. Probably this may belong
to our new genus.

MM, Jones and Kirkby—Carboniferous Ostracoda. 437

5. BeYRICHIOPSIS SUBDENTATA, sp. nov. PI. XI. Figs. 1, 2.

Along with B. fimbriata in the Plashetts shale are numerous
examples of another form, having longitudinal ribs, a reticulo-
punctate surface, and occasional traces of denticles on the ventral
and posterior borders.

It is smaller than B. fortis, but of similar outline, and with the
valves lobed much in the same manner. A sinuous rib passes
across the lower half of the valve concentric with the ventral and
extreme borders; and a short dorsal rib is sometimes present on the
posterior half. The surface is regularly, and somewhat coarsely,
punctate, rather than reticulate. The posterior half of the free
margin of some specimens is denticulated, but there are no traces of
a fully-developed fringe. Length, 3'> inch.

We have examined many valves of this species, but can find
nothing to show that it ever possessed a perfect fringe. The valves
we meet with of fimbriata and fortis very often are without this
appendage ; but this is accidental, for close examination invariably
shows where it has been broken off, by removal from the matrix or
otherwise. In subdentata, however, the margins show no indication
of fracture, and they are evidently found as they were originally.

Locality.—Calciferous-Sandstone series. Plashetts, Northumberld.

Neither of the last two species exactly agree with our definition
of the genus: B. cornuta having the marginal fringe, but not the
longitudinal ribs; #. subdentata possessing the latter character, but
the fringe only in a very incipient state. Still we are inclined to
look upon them as belonging to the same natural group as the others,
though less advanced perhaps in the process of differentiation from
Beyrichia. In fact, by taking another and less elastic view of the
subject, it would be easy to look upon all the forms as but the varietal
or individual differences of one species; for they certainly run very
near to each other. This, however, would scarcely be in accordance
with modern biological ideas; nor could we ignore the probability
of the soft parts of the various forms having differed materially one
from the other.

6. BEYRICHIOPSIS SIMPLEX, sp. nov. PI. XII. Fig. 4.

A very short time ago, Mr. Hugh Miller, of the Geological Survey,
sent us a series of Ostracodous specimens from the Carboniferous
rocks of Northumberland. Among them is a fringed form from the
Lower Carboniferous of Warksburn, North Tynedale, that appears
to be different from those already described. It occurs in single
valves, imbedded in a matrix of dark grey shale, along with species
Kirkbya, Cytherella, and other marine fossils.

It has a neat Beyrichian outline, with rounded extremities and a
convex ventral margin. The anterior portion of the valve is much
higher than the posterior. There is a well-marked subcentral sulcus,
with a round, but rather faint boss in front. The surface has no ribs;
but is sparsely and finely granulated. A narrow fringe bounds the
free margin, and breaks up into spines posteriorly, as in other species ;
and at the base of the fringe runs a beaded line. Length, zz inch.

438 MM. Jones and Kirkby—Carboniferous Ostracoda.

We name this form B. simplex. The full locality for it is ‘above
Ramshaugh, Longlee Ford, Warksburn, North Tynedale.”

BEYRICHIELLA, gen. nov.

There is another species (probably more than one) which comes
near those described above, but which has no fringe, although it
possesses a dorsal crest on each valve with a well-marked area be-
tween. It has a strong free-marginal overlap; and is quite unisul-
cate. This may be regarded as typical of a new genus and species
under the name Beyrichiella cristata (Pl. XII. Figs. 6a, 6b).

This form is abundant in some of the shales and cement-stones of
the Calciferous Sandstones in the Hast Neuk of Fife,—as at Rander-
stone and Billow Ness.

Note on some Bryricsiz.
1. Beyricnta arcuata, Bean. Pl. XII. Figs. 12—14.
Cypris arcuata, Bean, 1836, Mag. of Nat. Hist. vol. ix. p. 377, woodcut, fig. 55.

BS. arcuata was figured roughly by Bean in 1886; but, for the
purpose of making comparison easy, we figure it here anew. It is
a well-known and characteristic species of the Coal-measures proper,
in some of the shales and ironstones of which it is found in great
numbers.

It is comparatively large, being from 315 to +45 of an inch in length ;
subovate in outline, with convex valves; the dorsal margin is
straight, the ventral margin arched; and the posterior end is the
smallest (lowest). A deep sulcus marks the anterior half of the
valves, and in front of it, close to the antero-dorsal angle, there is
often a small, nearly obsolete notch, more strongly marked on
internal casts. The valves are rimmed, and the surface is polished
and finely punctate.

Among other localities, it occurs in Coal-measure strata at Ashby-
de-la-Zouch ; Agecroft Colliery near Manchester; Chesterfield ;
Ryhope Colliery and Claxheugh near Sunderland; and at Shotts
and Carluke in Lanarkshire.

2. Beyricuta rastrerata, Jones and Kirkby. Pl. XII. Figs. 8, 9, 10.
B. fastigiata, J. & K., 1867, Trans. Geol. Soc. of Glasgow, vol. ii. p. 220.

This species is smaller and has the valves more broken up into
lobes than B. arcuata. Seen from above the outline is sub-cunei-
form,—widest behind, pointed in front. The surface is punctate.

Length 4; of an inch. It was discovered by Mr. John Young,
F.G.S., of Glasgow. .

It occurs in the Carboniferous-Limestone series at Bathgate
(Linlithgowshire) ; Craigenglen, Campsie (Stirlingshire) ; Crossgate-
hall (Edinburghshire); Hast of St. Monans (Fifeshire); and in the
Calciferous-Sandstone series West of Billow Ness (Fifeshire).

3. Bryricuia Brapyana, sp. noy. Pl. XII. Fig. 11.

B. Bradyana is a small subovate form, with the left valve strongly
overlapped by the right. It has a well-marked subcentral sulcus,
and in some specimens a fainter and smaller anterior impression,
with a roundish boss between. Seen from above, the outline is

MM. Jones and Kirkby—Carboniferous Ostracoda: 439

compressed-ovate, pointed at the ends. Surface smooth; length 31;
of an inch. Many specimens are relatively higher and shorter than
the one figured. Discovered by Mr. John Young, F.G.S.

It is found in the Carboniferous-Limestone series at Charlestown,
Sunnybank Quarry, and near St. Monans, in Fifeshire; at High
Blantyre, Lanarkshire; and Whitebaulks, near Linlithgow.

4, BeyRICHIA CRATERIGERA, G. S. Brady, MS. PI. XII. Figs. Ta, 7).

Another species with a strong free-marginal overlap may be
described thus. Obliquely oblong ; equal in height, dorsal and ven-
tral borders, being nearly parallel; extremities rounded, with a
forward swing; a deep sulcus near the anterior third, and another
passing forward to the antero-dorsal angle. Valves convex, the
right overlapping the left very strongly ; lateral contour cuneiform ;
shell thick; surface strongly reticulated. Length 31> to 315 inch.

This fine species was discovered by Mr. David Robertson, F.G.S.,
of Glasgow, in the Carboniferous-Limestone series, at Calderside
Quarry, Lanarkshire; it also occurs in Lower-Carboniferous rocks
at Woodend Quarry and Plashetts, Northumberland ; and at Arnside,
Westmoreland.

EXPLANATION OF PLATES.
Puate XI.
(All the Figures, except Figs. 7 and 8, magnified 25 diameters.)
Fig. 1. Beyrichiopsis subdentata, J. and K.; left valve; 2, right valve. Plashetts.

» 9d B. fimbriata, J. and K.; left valve; fig. 4, left valve. Plashetts.
ADAG) ne right valve. Tweeden Burn.

np Oe ho ventral edge of left valve; 6. dorsal edge of right valve.
Plashetts.

stants 53 cast of left valve, with impression of its fringe; magnified
40 diameters. Billow Ness, Fife.

Sb bates ‘ right valve; magnified 30 diameters. Staneshiel Burn.

5p Oke a ventral edge of left valve; 94. dorsal edge of left valve; 9c.
hinder end view ; @ and ¢ showing the fringe.

», 10a. DS carapace, showing left valve; 104. dorsal view. ‘Tweeden
Burn.

spe lile B. cornuta, J. and K.; right valve. Linlithgow Bridge.

Puatse XII.

(All the Figures, except Fig. 3b. magnified 25 diameters.)

Fic. la. Beyrichiopsis fortis, var. glabra, J. and K., left valve; 14. dorsal edge
of right valve; lc. ventral edge. Staneshiel Burn.
Su os cs. 5 i left valve. Staneshiel Burn.
ney oe is » var. granulata, J. and K.; right valve; 3d. hind end
view, magnified 30 diameters. Staneshiel Burn.
», 4. B. simplex, J. and K., right valve. Warksburn.
. B. fimbriata (?), J. and K., left valve. Cultra, Ireland.
6a. Beyrichiella cristata, J. and K., carapace showing left valve; 6d. dorsal
view. Randerstone.
», 1a. Beyrichia cratigera, G. S. B., carapace showing left valve; 7. ventral
view. Arnside.
», 8. B. fastigiata, J. and K., thick-shelled carapace showing cast of left valve.
Sunday-night Cleugh.
9) gael IO, gp right valves (thin-shelled). :
lla. B. Bradyana, J. and K., carapace showing left valve; 110, ventral view.
» 12. B. arcuata (Bean), right valve. Stylton, Durham.
Sy ck 3p a cast of right valve. Carluke.
» 14. a 36 left valve. Longton, Staffordshire.

440 Dr. Traquair—New Species of Paleoniscide.

II.—New Patmonisoip From THE Eneiise CoaL-MEASURES.
By R. H. Traquair, M.D., F.R.S., F.G.S.
Elonichthys Aitkeni, sp. nov., Traquair.

ENGTH, 6 to 7 inches, shape fusiform. Oranial roof bones sculp-
tured with undulating ridges passing at times into elongated
tubercles. Mandible sculptured externally with slightly undulating
longitudinal ridges, which run tolerably parallel with the upper and
lower margins of the jaw; dentary margin finely tuberculated.
Maxilla of the usual form, its dentary margin likewise finely tuber-
culated, the rest of the surface covered with undulating ridges.
Scales of moderate size ; those of the front of the flank are higher
than broad; posteriorly they become more oblique and equilateral,
while towards the dorsal and ventral margins they become rather
lower than they are broad. Their ornament consists of sharp strong/y-
marked ridges, nearly straight and parallel, and only occasionally
bifurcating or intercalated. On the scales of the anterior part of the
flank these ridges run rather diagonally over the surface of the
scale from above downwards and backwards, but over the greater
part of the body they are parallel with the upper and lower margins of
the scale, and seldom does any greater obliquity of the ridges in the
anterior and lower part .of the scale give any indication of the
diagonal division of the pattern which is so common in striated scales
in the family Palezoniscide. Posteriorly, a peculiar and highly-
ornamental character is given to the squamation by the fact that
the lowermost ridge, uniting or not with the one next above it, is of
unusual breadth, and stands prominently out. On the V-shaped
ridge-scales of the caudal body-prolongation, the ornament becomes
speedily obsolete, and the small lozenge-shaped lateral scales are
at most marked by only one or two slight longitudinal furrows.

The length of the pectoral fin is about two-thirds that of the
head, its principal rays are unarticulated for about one-third of their
length. The ventrals are badly preserved, but their position seems
to be intermediate between the pectorals and the anal. The dorsal
is situated opposite the interval between the ventrals and the anal;
both dorsal and anal fins are pretty large, and of the usual triangular
acuminate shape; their rays are delicate and slender, distantly arti-
culated, ganoid and smooth, save that now and then a single longi-
tudinal furrow is seen especially just before bifurcation sets in. The
caudal is large and deeply cleft ; the articulations of the rays of the
lower lobe are a little closer than those of the dorsal; in the upper
lobe the joints become so short as to look nearly square-shaped.

Remarks.—Though hitherto undescribed, this fine species is
pretty well known to collectors in the West of England, and cannot
be confounded with any other. I have named it after the late
Mr. John Aitken, of Bacup, Lancashire, who lent me the beautiful
specimen, of which a figure will shortly appear in my memoir on
Carboniferous fishes in course of publication by the Palzeontogra-
phical Society.

Geological Position and Localities.:—Lower Coal-measures. Copy

Dr. Traquair —New Species of Paleoniscide. 441

Coal Mine, Cliviger (collected by the late Mr. Aitken) : Arley Mine,
Burnley, Lancashire (coll. of Mr. J. Wilde, Ashton-under-Lyne) :
Dalemoor Rake Ironstone, Stanton, Derbyshire (British Museum and
Museum of Practical Geology): Millstone Grit Shales, Danebridge
(Mr. J. Ward). There is a specimen in the Museum of Practical
Geology, labelled from Ladieswell Colliery, Staffordshire, but in Mr:
Ward’s opinion the specimen more probably came from the Lower
Coal-measures of the Cheadle district.

Elonichthys microlepidotus, sp. nov., Traquair.

I have only seen two specimens of this interesting form, which
have been kindly lent to me by Mr. Ward.

The length of the more perfect of the two is 33 inches; but as
it is broken off immediately behind the anal fin, we may justly esti-
mate the original length of the fish at not less than fiveinches. The
external markings of the head-bones are not well seen, except in the
case of the lower jaw, which is ornamented by wavy longitudinal
branching and anastomozing ridges. In this specimen the mouth is
wide open, as is also the gill-cleft, owing to the drawing forward of
the suspensorium ; the opercular bones are rather narrow, and beneath
them and the mandible the branchiostegal rays may be counted.
The scales are small in proportion to the size of the fish, and their
markings consist of only a few strong ridges passing horizontally or
with only a slight obliquity across the scaie. Only the base of the
pectoral fin is seen, the other fins are large, and have the form and
relative position characteristic of this genus. ‘Their rays are very
numerous, fine, and closely set; their joints longer than they are
broad, and their surfaces show traces of fine longitudinal striation.

Remarks.—The relative smallness of the scales and their peculiar
simple bold ornament distinguish this species from any other with
which I am acquainted.

Geological Position and Locality.—Knowles Ironstone Shale, Long-
ton, Staffordshire, in the collection of Mr. John Ward, F.G.S.

Rhadinichthys macrodon, sp. nov., Traquair.

The specimen upon which this species is founded measures five
inches in length, but it is broken off just behind the commencement
of the caudal fin, as indicated by the dorsal ridge scales; the length
of the head is 14 inch, and the depth of the body nowhere exceeds
one inch. Consequently, the general aspect is that of a fish of slender
form, but the specimen cannot be relied on as showing the original
shape, as the scales are broken up and confused, and the fin-rays
almost entirely wanting. The head exhibits the typical paleeoniscid
structure,—the suspensorium being very oblique, the gape wide, and
the usual arrangement of opercular and branchiostegal plates being
shown ; the bones are, however, seen almost exclusively from their
internal surfaces. Both jaws are armed with stout, conical, incurved
teeth of unusually large proportional size, those of the maxilla
measuring ;'y to ;’5 inch in length ; the small external ones are not
visible. The scales are of comparatively large size, those of the
anterior part of the flank having their exposed areas covered with

442 S. S. Buckman—The Lobe-line of Ammonites.

delicate ridges and furrows, which are nearly parallel with the upper
and lower margins of the scale, though they tend to turn upwards
anteriorly ; the posterior margin is sharply and prominently denti-
culated. As we proceed backwards, the scales lose the sharpness of
their ornament, and become nearly smooth towards the tail, though
the caudal V scales remain prominently striated. The origin of the
pectoral fin is present, though not well shown, and here the principal
rays seem unarticulated. A few broken up ray-joints mark the
position of the dorsal and anal fins, the former occurring 8 inches, the
latter 8% inches behind the front of the head.

Remarks. —The condition of the specimen renders its generic
determination a matter of great uncertainty, but I am inclined to
place it in Rhadinichthys for the following reasons:—(1), the
apparent elongation of the body, on which, however, little weight
can be placed; (2), the resemblance of the scales, in shape and
ornament, to those of the typical R. ornatissimus, Ag. sp.; (8), the
appearance of the broken rays of the root of the pectoral fin.
Specifically I designate it as new, as I am not acquainted with any
other form in which teeth of such large proportional size occur with
scales of similar conformation and markings.

Geological Position and Locality.—Knowles Ironstone Shale, Fen-
ton, Staffordshire, in the collection of John Ward, Esq., F.G.S.

(Lo be continued.) 2

I1I.—On tue Lops-iine oF Certain Sprcizs or Lias AMMONITES
_ Descripep rn THE MonoGrapH BY THE LATE Dr. WRIGHT.
By 8. 8. Buckman, F.G.S.

Nc recently turning over the plates of this Monograph, my
attention was arrested by the lobe-line figured on plate 63,
and on looking at the explanation of the plate given on the opposite
page, I was much surprised to see that it was stated to be the
“« Lobe-line of Harpoceras ovatum, magnified.” On the same plate,
just below (fig. 4) is a side view of the Harp. ovatum with its lobe-
line in situ, and I suppose it to be this lobe-line that is magnified.
But there must surely be some mistake here. Compare ake lobe-
line, fig. 7, with that on fig. 4, and notice the much greater width
of the siphonal saddle in fig. 4 (than in fig. 7), where, on account of
the curvature of the fossil, it would be really smaller. To say
nothing of the obliquity of the inner portion of that on fig. 4, where
is the first auxiliary lobe (nearly as large as the inferior lateral in
fig. 7) to be found in fig. 4? I think it will be apparent that for
some reason or other the two lobe-lines are different. But is the
lobe-line, fig. 7, the correct lobe-line for such a species as the Harp.
ovatum here figured? I must say No! Turning for a moment to
Wright’s description of the lobe-line of Harp. ovatum, page 446, we
find it stated, “ The suture-line is of the radians type.” ‘This is true
enough of the suture-line shown on fig. 4, but I think any one who
has paid attention to the suture- lines” of this class of Ammonites

could not possibly say that fig. 7 was a lobe-line of “the radians type.”
The further description given is accurate as regards fig. 7, but it

R. F. Tomes—Inferior Oolite Madreporaria. 443

cannot be said to apply to fig. 4. In fact the suture-line fig. 7
belongs to that group of shells of which the specimen of H. elegans
(figs. 1, 2, 8 on the same plate) is characteristic, and that by some
means or other an oversight has occurred and the suture-line of this
specimen (Harp. elegans) has been figured in mistake for the one of
H. ovatum. ‘That it is no fault of delineation I feel positive, because
fig. 4 is characteristic of the group to which Harp. ovatum would
belong, while fig. 7 is characteristic of the group to which Harp.
elegans belongs. Compare for confirmation of this opinion the suture-
line, fig. 7, with the suture-line given by D’Orbigny (Pal. frang. Terr.
jurass. plate 62) to Am. primordialis—otherwise Am. opalinus
(Reinecke) ,—a very near ally of Am. elegans, or compare it with the
suture-line of a specimen of Am. concavus, Sow. These shells belong
to a group having a practically identical suture-line not at all like
that of Harp. radians. Now turn to plate 80, and at first sight the
evidence appears against me. Here we have in fig. 3 a suture-line
which I consider is of the opalinus type, called the suture-line of
Harp. aalense, and in fig. 5 the suture-line of apparently the radians
type called the suture-line of Harp. opalinum ; but let us now look
at his description of the suture-line of Harp. aalense, page 499, and
Harp. opalinum, p. 464, and we see that the descriptions do not in any
way agree with the figures. It is in figure 3, not 5, as stated, that we
find the siphonal saddle divided into two unequal portions, and the
auxiliary lobes large and two smaller auxiliaries, because there are
no auxiliary lobes in fig. 5. The fact is Wright has correctly described
the lobe-lines belonging to the two species, but has never noticed
that they were wrongly numbered, whilst on page 446 (plate 68) he
has described as the suture-line of Harp. ovatum a suture-line belong-
ing to a different group of species altogether. I have proceeded no
further at present, as I only happened to notice these suture-lines
because they were necessary to me in my own work. But having
noticed the errors mentioned, I have penned these remarks, not with
the intention of detracting in the least from the excellence of Wright’s
monograph, but to call attention to the subject, so that it may not
mislead others or be the unsound basis of argument should any
discussion arise concerning the validity of suture-lines as a means of
identification.

TV.—On Some New or Imperrectty Known MapDrePoRARIA FROM
THE INFERIOR OoLITE OF OXFORDSHIRE, GLOUCESTERSHIRE AND
DorsETSHIRE.

By Rozzrt F. Tomss, Esq.
(Continued from p. 398.)
ADELASTRHA consoBrina, Hdw. and Haime, sp.
(not Synastr@a consobrina, d’Orb., Prodromus).

WwW" are informed by M. Ferry that d’Orbigny was supplied with

the greater part of the Corals of his Bajocien by M. Eugene

Beabeau, of Langres, who has stated of the present species that it was

first named Calamophyllia glomerata by d’Orbigny, and afterwards by

an error Synastrea consobrina, and further, that he at the same time

444 R. F. Tomes—Inferior Oolite Madreporaria.

described in his Prodromus another species under the same name.
MM. Milne Edwards and Haime, it appears, were misled by this
error, and referred the Coral sent by M. H. Beabeau, to the Synastrea
consobrina of the Prodromus. This in brief is the statement of
M. Ferry, and it is obvious that the Synastrea consobrina of the
Prodromus, and the Clausastrea consobrina of MM. Milne Edwards
and Haime are not the same, and that the latter is the Coral for-
warded by M. E. Beabeau from Langres.

As Confusastrea had been proposed as a generic name as long ago
as 1849 by M. d’Orbigny, and several species placed in it by him in
1850, and recognized by Milne Edwards and Haime, M. Ferry ap-
pears to have entertained no doubt about the generic relationship of the
present species, and he therefore unhesitatingly places it in the genus
Confusastrea. An allied species C. ornata occurs also at Langres,
which differs only from C. consobrina in having larger calices. Of this
M. Ferry gives a description, in which mention is made of some
peculiarities which may here be noticed. The corallum, he in-
forms us, is formed of a successive aggregation of corallites, with
lateral and marginal buds, joined with one another by a rudimentary
wall. He further observes that the corallites are often superposed,
the young calices frequently implanted in the old ones, and that
they start from a common base, formed sometimes of a single
individual. :

No description is given of C. consobrina, but it is said to resemble
the last species, but with calices which are constantly of smaller
diameter.

The specimens from the Cheltenham district correspond with
great accuracy with the description given of C. ornata by M. Ferry,
except that the calices are smaller, and their diameter agrees very
well with that given of those of Clausastrea consobrina by MM.
Milne Edwards and Haime, which is undoubtedly the same species
as the Confusastrea consobrina of M. Ferry. Budding occurs laterally
and in the depressions between the calices of these Cheltenham
examples, and the growth of one calice within another (rejuve-
nescence) is not unfrequent in them. This Coral appears to be
plentiful in the Lower Coral-bed in the Sheepscombe valley, near
Painswick, and I have seen a specimen taken from the Oolite marl
at Leckhampton Hill.

Of Adelastrea tenuistriata IT may remark that although when un-
worn it is quite unlike an Isastrea, yet when the septa are worn
down, it is difficult to distinguish from Isastrga tenuistriata. With
the latter it has often been confounded. The marginal budding will,
however, always identify it. Its relationship to the fissiparous
genus Cladophyllia, suggested by Professor Duncan, is entirely un-
supported by evidence.

IsaSTRHA TENUISTRIATA, Hdw. and Haime.

Since the appearance of my former paper I have examined a
number of specimens of this species from the Lower Coral-bed at
Crickley Hill and Birdlip Hill, from the Lower Trigonia Grit at
Juniper Hill near Painswick, and from other localities in the

an

R. F. Tomes—Inferior Oolite Madreporaria. 445

Cheltenham district. I have also obtained it from the Upper Coral-
bed in the Slad Valley near Stroud. It is now therefore obvious
that it has a considerable vertical range in the Inferior Oolite. A
specimen from Birdlip shows its method of gemmation very clearly.
It takes place either on the exposed margin of the wall between the
-calices or a very little within the calice, as even when still very
small it is impossible to say from which calice the young one
proceeded.
IsASTRHA DEPRESSA, Tomes.

Besides the localities already mentioned in my communication
on Inferior Oolite Corals, I have now seen examples from the Lower
Coral-bed at Birdlip, and at Juniper Hill in the Painswick valley.
I have also a specimen which was given to me by the late Dr.
Bowerbank, with the information that it had come from Dundry Hill.
Another specimen from the same locality is in the Northampton
Museum. There is also one in the Museum at Oxford, which was
taken from the Inferior Oolite in the Hook Norton cutting of the
Banbury and Cheltenham Railway. The presence of this species
at the latter place might lead to the conclusion that the lower beds
of the Inferior Oolite are not unrepresented there.

CHORISASTRHA GREGARIA and C. oBTUSA.

I enter with some reluctance into a repetition of what I have
already insisted on respecting some corals which I placed in the
genus Chorisastrea. So far as the two English species, C. gregaria
and C. obtusa, are concerned, everything depends upon their mode
of increase. If it is by fissiparity, then are these species simply
Thecosmilians, but if accomplished by means of gemmation, some
other genus than Thecosmilia must be chosen for their reception.
Now, Professor Duncan himself, speaking of these same corals
(Quart. Journ. Geol. Soc. vol. xlii. p. 128), says, “An attempt was
made to include the well-known species of Thecosmilia, which at
first increase by gemmation and then by fissiparity ” (7.e. to include
them in Chorisastrea). The words have been given in italics by
me. A few pages further on (p. 113), he refers to one of my own
figures in proof of fissiparity in Chorisastrea gregaria. That figure
represents the earliest period when increase takes place, just at the
time when the corallum ceases to be simple and becomes compound.
This, according to Professor Duncan’s own words, should be the
period for gemmation, instead of fissiparity. .The two statements
are of course inconsistent with each other. The real fact is, gem-
mation and nothing else takes place, and we have exactly the same
process which is represented by the figures of Chorisastrea corallina,
From., C. neocomiensis, From., and C. dubia, Becker. One of the
figures of the latter species (from the Corallien of Nattheim) bears a
strong resemblance to some of the more simple examples of C. gre-
garia, and answers to the descriptive words of MM. Milne Edwards
and Haime which they applied to their Thecosmilia gregaria. They say
that the corallites of that species differ from those of Thecosmilia by
“remaining in general grouped in fasciculi to a considerable distance

446 R. F. Tomes—Inferior Oolite Madreporaria.

from the parent calice.” This is precisely what takes place in the
various speices of Chorisastr@a, and had those celebrated palzon-
tologists seen and examined young examples at various ages, I do not
for a moment believe that they would have placed C. gregaria in the
genus Thecosmilia.

Chorisastreea obtusa from the Great Oolite differs chiefly from
the preceding in being smaller. But some of the dwarfed examples
of C. gregaria very closely resemble it. However, C. gregaria may
at all ages be known by the greater thickness of its septa outwardly,
that is, near the mural region. This peculiarity is observable in
individuals, the corallum of which is so young that it has only the
thickness and size of a small coin. The specimen of C. obtusa figured
by Prof. Duncan is not very characteristic, one of that height would
commonly have four or five calices, or even more.’ Such examples
as the one figured are however common in the Fairford Coral-bed.

In support of Chorisastrea as a genus I may only remark that
if not Thecosmilian, the species I have here mentioned must be placed
either in Chorisastrea or Latimeandra, and it can hardly be said that
they fall properly into the latter.

CHORISASTRHA, Sp.

Peduncular portions of a species of coral referable to this genus
have been obtained from the beds under the Pisolite at Crickley Hill,
and from a sandy bed overlying the Upper Lias sands at Dover’s
Hill near Chipping Campden. All the specimens examined have
very numerous, thin, and uniform septa, and they are probably
attributable to some undescribed species.

Genus Puyiiocyra, Tomes, Q. J. Geol. Soc. vol. xxxvili. p. 430.

Since the definition of this genus appeared, I have examined some
young examples of Phyllogyra Htheridgei from the Trigonia Grit of
Leckhampton Hill, which enable me to confirm the characters I have
before assigned to the genus. The smallest of these is not more than
an inch in diameter. It has a flattened lenticular form, with a central
Jarge calice and a thin lobular outer margin, in the lobes of which
gemmation is actively taking place, precisely as it does in the margins
of small examples of Chorisastrea gregaria. Between the marginal
lobes are subcristiform ridges, just as in that species, and such as I
have figured in plate xviii. illustrating the paper above quoted. It
is obviously by gemmation, and not by fissiparity, that increase in
this genus takes place, as the central calice is not in any way
interfered with by the simultaneous growth of a circle of new calices
in the distal ends of the surrounding septal coste. Gemmation as
it takes place in Phyllogyra is precisely as in Latimeandra, and as it
has been figured by Prof. Duncan himself in his Supplement to the
British Fossil Corals, plate v. fig. 7 of part il.

It is by no means improbable that Phyllogyra Htheridgei and
Chorisastrea gregaria may prove to be forms which differ only from
each other; the one by having a depressed and expanded growth,

1 Since writing the above the specimen figured by Prof. Duncan as Thecosmila
obtusa has come into my hands. Of it I shall have more to say on a future occasion.

R. F. Tomes—Inferior Oolite Madreporaria. 447

and the other by having a subdendroid form. For the present I
leave them where they are, but must enter my earnest protest against
there being any near affinity with Symphyllia in the Oolitic form
now under consideration.

PHYLLOGYRA SINUOSA, Tomes.

I have lately met with several examples of this species in the
Lower Trigonia Grit near Cheltenham, but in no instance in the
Coral-bed at Crickley. It has not, indeed, been observed in the Lower
Coral-bed at any locality, though it most frequently occurs in the
Oolite marl, or third Coral layer.

-PLATASTRH#A ENDOTHECATA, sp. nov. (Plate X.' Figs. 1, 2, 3, 4.)
Clausastrea Conybeart, Tomes, Proc. Geol. Assoc. vol. vi. no. 4.

The present species, the occurrence of which I have already
recorded, under the name of Clausastrea Conybeari, must, with the
allied species from the Great Oolite of Bath, be referred to the new
genus Platastrea. Specimens from the Inferior Oolite of Hook
Norton are for the most part fairly preserved, and sometimes when
broken through, show the structure of the septa and the dissepi-
mental tissues very clearly.

The corallum is rudely lenticular, and not very large. The upper
surface is moderately convex, sometimes almost flat, and never much
elevated, and the outer margin is rather thin, but rounded rather
than angular. The under surface is much more prominent than the
upper surface, in some specimens almost subpeduncular, with a
central point indicating a former attachment. The common’ or
basal wall is rudimentary, and has intermittent and narrow rings
of epitheca. The radiating mural costze are thin, and the spaces
between them are wide and filled with dissepiments. The calices
have a more or less quadrangular or rounded outline, and are shallow.
The septa are all of them continuous with those of other calices, but
- they often form an angle where they meet and unite between the
calices. They are very stout over the mural region, but speedily
become thinner as they approach the visceral cavity. The margins
of all of them are denticulated, the teeth consisting of rather large,
regular, and rounded tubercles, the greater diameter of which is
across the septum. There are four cycles of septa in six systems.
In some systems the fourth cycle is incomplete, while in others there
are a few very rudimentary septa of the fifth cycle. The primary
septa extend to the fossula and meet, the secondary ones are very little »
shorter than the primary ones, and those of the tertiary cycle are

1 This Plate was published in the September No. with the first part of this paper.

2 I must differ wholly from Prof. Duncan when he says that there are never two
rudimentary cycles in the same calice. There are not ever, to the best of my know-
ledge, two rudimentary cycles in the same system, but there may be, and often are, in
the irregularly developed calices of Jurassic Madeporaria, rudimentary septa of quite
different ages in different systems. ‘The third cycle may be rudimentary in one and
complete in another, in which a fourth may have even commenced its growth. Such
irregularities are frequent after recent rejuvenescence, one side of the calice having
perhaps the full complement of septa, while the other may have only the earlier
developed cycles.

448 Rk. F. Tomes—Inferior Oolite Madreporaria.

a little more than half the length of those of the primary cycle,
while those of the fourth cycle are quite short.

The dissepiments are very numerous; stout, arched, and they
completely fill up the loculi. They continue so high up in them
that they are seen almost close beneath the denticulations of the
septa. The diameter of a large corallum is from three to four
inches, and the height about one inch. The diameter of the calices
is half an inch. Increase takes place by gemmation in the interval
between the calices.

Although allied to Platasirea Conybeari from the Great Oolite, the
present species may be readily distinguished from it by its much
smaller size and regularly lenticular form. Again, the septa of
P. Conybeari meeting in the centre of the visceral cavity, are much
thickened quite low down in it, and these form a mass which, when
those parts of the septa which are above it have been worn down,
comes in view, and has so much the appearance of a columella as to
have led MM. Milne Edwards and Haime to place the species in
the genus Plerastr@a. Nothing of the kind is observable in Pla-
tastrea endothecata.

I take the present opportunity of making a few remarks on Pla-
tastrea Conybeari. It is not rare at Coombe Down, from which
place the type-specimens were obtained. It is sometimes of great
size, and although, generally speaking, of a globose form, is often
extremely irregular in its outline, and the calices on some parts have
a corresponding irregularity in shape. When these irregular calices
are worn down, they present precisely the appearance of those shown
in the figure of Clausastrea Pratti figured in the History of British
Fossil Corals. But the more regular calices of Isastr@a Conybeart,
figured on the same plate, would never by any condition of fossili-
zation or any amount of wear resemble those of the then supposed
Olausastrea. But indeed no one except Prof. Duncan has suggested
such a possibility.

Of the type-specimen of Clausastrea Pratti (afterwards Plerasirea
Pratti) the original describers observe that it is so ill preserved that
they could not give a complete description of the species from it.
Notwithstanding this, no doubt seems to have crossed Prof. Duncan’s
mind as to its fitness to furnish a satisfactory description, and he
has accordingly entered quite recently into its details.’ I also have
lately examined the type-specimen, and can confirm what has been
said of its unfavourable condition by MM. Milne Edwards and
Haime. It is a young example and bears a very close resemblance
to many of the specimens from Coombe Down. The supposed papillose
columella observed in some of the calices is nothing more than the
blending of the septa in the centre of the calice, the denticulations of
which, resembling in shape those I have figured on the plate accom-
panying this communication,’ are yet traceable in that part of the
calice which has been subjected to the least wear—that is to say, in
the centre. All other parts of the septa have been worn down quite
smooth.

1 Quart. Journ. Geol. Soc. vol. xlii. p. 138. 2 Plate X. Figure 3.

a

R. F. Tomes—Inferior Oolite Madreporaria. 449

In the description of the so-called Clausastrea Pratti by the
original describers it is stated that the calices are not separated by
a distinct wall; all the Coombe Down specimens J have seen,
whatever their condition, accord in this particular with the type.
They are equally destitute of surrounding wall, whether they
have the irregular form of those of Clausastrea Pratti, or the more
regularly defined ones of Isastre@a Conybeart. Turning to the de-
scription of the genus Plerastrea by MM. Milne Edwards and
Haime, M. de Fromentel, and Prof. Duncan, I observe that special
mention is made of the presence of walls surrounding the calices. I
must therefore still contend that Platastrea is generically distinct
from Plerastrea, which has distinct walls bounding the calices.

Further, I must continue to assert the identity of the two species
Isastrea Conybeari and Plerastrea Pratti, the latter being nothing
more than a small specimen having an irregular growth, and a cor-
responding irregularity in the development of the calices. And I
must repeat my assertion that the same specimen of this variable
species will on different parts present the appearances represented
by the figures given by MM. Milne Edwards and Haime of Isastrea
Conybeari and Plerastrea Pratti.

Genus LepropHyLira, Reuss.

The conclusions of M. Pratz respecting the structure of the coral-
lum of the genus ZLeptophyllia were based on the examination of
specimens of the very species on which Reuss established the genus.
They were obtained from the Cretaceous formation at Gosau, and he
observes that proof is yet wanting that these Cretaceous and other
subsequently described species from the Oolites are generically
identical. At present my knowledge of the Oolitic Leptophyllie is
confined to the examination of a few examples of a small species
from the Inferior Oolite. In these I observe the same form of
pseudo-synapticule as in the Gosau Leptophyllie, and in the
genus Thamnastrea ; they therefore, very probably, appertain to the
genus Leptophyllia. One of these small and malformed Oolitic
Leptophyllia, from the Inferior Oolite of Dorsetshire, has been figured
and described by Prof. Duncan under the name of Podoseris constricta.

LepropHytiia Fioursstt, H. de From.,
Pal. France. Terr. Jurass. Corall. p. 93, pl. 27, figs. 1-4, Oct. 1866.

One example of this species has been taken from the Oolitic Marl
at Leckhampton by me, and I have another given to me by my
friend Mr. W. C. Lucy, which he obtained from a bed of angular
oolitic gravel near Painswick. The Painswick specimen is mis-
shapen, and has a curiously close resemblance to figure 3 of the
plate above quoted.

Genus Tuecoserts, HE. de From.
Paleoseris, Duncan.

Since the publication of my paper in which the description of
Thecoseris polymorpha appears, I have examined a specimen of that
species which had been split through vertically, showing the sides

DECADE III.—YOL. IlIl.—NO. X, 29

450 R. F. Tomes—Inferior Oolite Madreporaria.

of the septa with great distinctness. The so-called pseudo-synapti-
cule are very clearly shown, and appear as ledges passing con-
tinuously across the septa in lines parallel to the septal edge. There
is not the slightest indication of perforations between these ledges,
but there are well-defined dissepiments low down in the corallum.
The genus Thecoseris differs wholly from Leptophyllia in having im-
perforate septa and an investing wall with a well-developed epitheca,
giving to the calice a clearly-defined and prominent margin. These
differences sufficiently characterize Thecoseris, and at the same time
distinguish it from Leptophyllia. They also afford good reasons for
declining to accept the position of a subgenus assigned to them by
Prof. Duncan. :

When I stated my belief that Palzoseris would be found to be
identical with Thecoseris, I did not know that Zittel had already
referred it to that genus. That Thecoseris should be a Cretaceous
as well as a Jurassic and Tertiary genus, might be anticipated, and
accordingly a species has been described in Stoliczka’s work on the
Cretaceous Corals of Southern India.

THAMNASTRHA EXPANSA, Sp. NOV.

IT have met with a Thamnastrea at Birdlip Hill, Gloucester, in a
Coral-bed which is an extension of the one at Crickley Hill, having
characters which do not accord with those of any species I am ac-
quainted with, and I therefore describe it under the above name.

The corallum is broad and saucer-shaped, very thin, and has a
slight peduncle. The margin is extremely thin and wavy. The
epitheca is well developed and concentrically wrinkled. The calicular
surface is very slightly concave, and a little deeper in the centre.
The calices are extremely small, circuiar, and regularly distributed,
and there is very little disposition in the septal coste towards the
parallel arrangement observable in so many species of Thamnastrea.
About twenty-four septa enter into and form the calice, twelve of
which unite in pairs at the fossula. The others are short. The
fossula is small, round, but not very deep. All the septa and septal
coste are very delicately papillated.

Diameter of the corallum, 3 inches; its thickness, 4 inch.

Distance from centre to centre of the calices, 1 line.

THAMNASTR#A HETEROMORPHA, Sp. NOv.

The corallum has a very complicated outline, somewhat resembling
that of Dimorphophyllia, but much more irregular and less compact.
Proceeding from a common centre, it expands upwards and outwards
into a considerable number of leaf-like and lobular parts, which are
in clusters, and have openings through and between them. The
calicular surfaces are horizontal and divided; they are numerous,
and having their margin turned up, present extremely irregular
shallow cavities. All the under parts of these leaf-like lobes have
a well-developed and rugose epitheca.

The calices are for the most part in rows corresponding with the
outer margin of the lobes. They are shallow, but have a well-
defined and rather large fossula. There are from sixteen to eighteen

a a

RL. F. Tomes—Inferior Oolite Madreporaria. 451

septa, of which twelve are of equal length and form the fossula.
The rows of calices are connected by septal coste, which are nearly
parallel, and run towards the outer margin of the lobe. Very few
anastomoze, but all, as well as the septa, are regularly papillated.
In the fossula is a well-defined columella consisting of about
twelve regular styliform papillee.

Height of the corallum, about 14 inch, and its greatest diameter
about 34 inches. The calices are distant from each other about one
line.

I have met with a few specimens in the Oolite Marl at Leck-
hampton Hill, but not at any other place.

DIMORPHARZA EXPANSA, Sp. NOV.

I possess four specimens of Dimorpharea, from the Inferior Oolite
of Hast Coker, they are very distinct from Dimorpharea Oolitica,
which I describe as follows :—

The corallum is very broad and thin, and the upper and under
surface have about the same degree of convexity. The largest
specimen has a diameter of four inches, while in thickness it does.
not exceed half an inch. The outer margin of all the specimens is
quite thin. In all of them the mural coste are visible on the under
surface, only a very small quantity of epitheca being present. This
is distributed in patches. These coste are straight, uniform in size,
and they radiate from a centre.

The middle or parent calice has very little prominence, and is only
a little larger than the surrounding ones, which are ranged around
it in circles, so irregularly that they look almost scattered.
There are, however, three circles of secondary calices, and outside
the external one the septal cost are prolonged to a length exceed-
ing the distance between the circles. From this it might seem that
three is the full complement of circles, unless the distance between
the circles increases rapidly as the corallum enlarges.

From twelve to sixteen septa enter into and form the calices.
In the most regularly formed there are twelve, of nearly equal
length and thickness, extending to the fossula, but they do not enter
into it. They have perforations, which are not numerous, but are
large and distinct. The septal costee are of equal thickness with the
septa, as well as equally thick throughout; they are straight or
wavy, rarely curved, and have a radiate arrangement. The breadth
of the intervals between them rather exceeds their own thickness.

At present I have been unable to examine specimens having the
septal edge complete.

CoMOSERIS VERMICULARIS.

A specimen of Comoseris which I took from the friable Pisolite at
Crickley Hill is obviously specifically identical with the specimen
I have already referred to C. vermicularis obtained from the over-
lying Coral-bed at that place. It is a young and worn example, but
is very instructive as to the habit of growth of the species. A short

1 Quart. Journ. Geol. Soc. vol. xxxviil. p. 448.

452 R. F. Tomes—Inferior Oolite Madreporaria.

peduncular foot is surmounted by a tuber-shaped top, which is com-
posed of overlapping leaflets, and where the lateral margins of these
meet on the upper surface, they curl up and form ridges having
precisely the same sinuosity as the margins of the leaflets. It is
only, however, at the outside of the corallum that the outline
of the leaflets can be satisfactorily traced. On the whole of the
central part they are too much fused together to be followed except-
ing as sinuous ridges, which being worn down, reveal the hidden
wall within.

In 1884, when Prof. Duncan published his Revision of Families
and Genera, he did not admit that there was any wall in the collines
of Comoseris; but in his recently published paper in the Journal of
the Geological Society he acknowledges that there is a false wall.
This is a step in the right direction. With patience and further
research a true mural structure may yet be arrived at.

This is the only species I have met with which is common to the
Pisolite and the overlying Coral-bed; but as the specimen from the
former deposit was found in the friable or disintegrated part, it may
have fallen from above and have been embedded.

PHYLLOSERIS INCRUSTATA, Mich. sp.

Alveopora incrustata, Mich. Icon. Zooph. p. 111, pl. 26, fig. 8, 1840-47.
Microsolina incrustata, M. Edwards, Hist. Nat. Corall., tom. 11. p. 201, 1860.
Phylioseris, sp. Tomes, Q. J. G. S. vol. xxxvill. p. 448, 1882.

The species of Phylloseris which I indicated at page 448 of my paper
on Inferior Oolite Corals is obviously identical with the Alveopora
incrustata of Michelin. Although described by that author as a
dendroid species, and having the “‘rameaux”’ partially covered by an
irregular “croute,” it is obvious by the figure that it has more of
a digitate than a dendroid growth. That it is a second species of
Phylloseris, differing chiefly from P. rugosa in the form of the coral-
lites and the size of the calices, I have no doubt. The epitheca
extends upward by degrees and obliterates the calices, just as it does
in Phylloseris rugosa.

LATIMHANDRARIA CONCENTRICA, Tomes.
Oroseris concentrica, Tomes, Quart. Journ. Geol. Soc. vol. xxxviii. p. 441.

In a paper on the Madreporaria of the Coral Rag (Quart. Journ.
Geol. Soc. vol. xxxix.) I suggested that a species of Oroseris which
I had before described as Oroseris concentrica, probably appertained
to another genus. I now place it in Latimeandraria, and I do so
tor the following reasons. As clearly pointed out by me, Oroseris
may be recognized by its mode of gemmaparous increase, which is
calicular or marginal, while in Latimeandraria, Thamnastrea, and
some other genera, it is intercostal. As it is also intercostal in the
present species, I now place it in the former of these genera.

In conclusion J wish to render my very sincere thanks to Mr.
Hudleston, Mr. Buckman, and Mr. Jas. Windoes for their liberal
assistance in the use of specimens from their several collections.

W. J. Harrison—Deep-Boring in Keuper Maris. 453

V.—On a Deep Borine 1n THe New Rep Marus (Keuper Marts)
NEAR BrrMINGHAM.'

By W. Jerome Harrison, F.G.S.

HE Triassic strata which form the country surrounding Birming-
ham consist of the usual divisions of sandstone and marl; the
sandstones predominating below, the marls above. In the immediate
neighbourhood of the town, the sandy beds are divided from the
marly or clayey strata by a dislocation or line of fault which runs
from north-east to south-west, taking a line from Erdington to
Rubery, and traceable altogether for a distance of about twenty
miles. The fault runs through the town of Birmingham nearly
parallel to the River Rea, and from a quarter to half a mile west of
the present bed of the river. The Lower Keuper sandstone, which
forms a surface band one to two miles in width on the west of this
fault, is a porous stratum about 200 feet in thickness. It is under-
lain by the Bunter Pebble Beds, 300 to 400 feet in thickness, which
crop out further to the west, and which contain an inexhaustible
supply of water. From three deep wells in the suburbs of Birming-
ham—two on the north at Perry and Witton, and one on the south
near Selly Oak—the Corporation Waterworks obtain daily a supply
of over eight million gallons of water, most of which comes from
the Pebble Beds, which occupy the lower portion of each well or
bore-hole. The water is of good quality, showing from nine to fifteen
degrees of hardness.

On the east of the line of fault a very different state of things
prevails. The rocks on this side have been dropped vertically some
six or seven hundred feet. Here the surface is composed of the
Keuper Red Marls, which form a broad band ten or twelve miles in
width, extending from Birmingham to Shustoke. The water-supply
of this tract—which has a considerable extension to north and south
from Tamworth to Warwick and Redditch—is wholly derived from
superficial sources, such wells as exist drawing their water from the
post-glacial sands and gravels which lie here and there in hummocks
on the Red Marls.

As the population on this agricultural plain of Warwickshire
is comparatively small and scattered, and as there are no manufactur-
ing towns in the district, it is, perhaps, not surprising that until quite
recently no attempts have been made to reach the buried waters
which probably exist in the Bunter and Keuper Sandstones that
underlie the Red Marls on the east of the line of fault. The chief
obstacles to such an undertaking are the unknown—certainly consider-
able—thickness of the Red Marls; and the fact that no one likes
to be the first to experiment in a matter in which—while there is
certainly a possibility of failure—any good result obtained would
be quite as much for the benefit of one’s neighhours as for one’s self.
It would seem that such borings might be executed by Government,

1 Read before Section C. (Geology), British Association, Birmingham, September
3rd, 1886.

454 W. J. Harrison—Deep-Boring in Keuper Marls.

or by the County Boards which it is proposed to establish, the cost
being defrayed by a small tax levied on the landowners of the district.

The work of the Geological Survey has given us some information
as to the probable thickness of the Red Marls. Prof. Jukes, writing
of South Staffordshire,’ says:—‘“ The total thickness of this sub-
formation cannot be much less than 600 feet;” and Mr. Howell,
speaking of this very district,” states that “south of Birmingham the
Keuper Marls attain a thickness of nearly 600 feet,” and again adds
“in this district, the Red Marl attains a maximum thickness of about
600 feet.” However, he gives a section of a boring on the Lindley
Hall Estate (four miles north of Nuneaton), about which, although
a depth of 660 feet was attained, he says, “it does not seem certain
that they got through the Red Marl series; some of the lower beds,
however, may belong to the Lower Keuper Sandstone.” In a deep
boring for water, at Rugby, after passing through 400 feet of Lias
and seventy feet of Rheetic Beds, the New Red Marls were pierced,
and found to be 670 feet in thickness; at a depth of 1140 feet the
Keuper Sandstone was reached, and a rush of water flooded the
bore-hole; unfortunately this water was so impregnated with salt
and with gypsum as to be unfit for domestic purposes.

About eight or ten years ago the Birmingham Corporation put
down a bore-hole in Small Heath Park (a southern suburb of Bic-
mingham), in search of water for certain baths and wash-houses
which it was proposed to build there. A depth of 440 feet was
attained, entirely in the Keuper Red Marls, before the boring was
abandoned. I have seen numerous specimens of fibrous gypsum
obtained from varying depths in this bore-hole.

Harly in the present year Messrs. Bates, of the King’s Heath
Brewery, three miles south of Birmingham, resolved to make a deep
boring for water through the Red Marls on which their buildings
stand, at a distance two miles to the east (down-throw side) of the
line of fault already described. They entrusted the work to Messrs.
Le Grand and Sutcliffe, of 100, Bunhill Row, London, who have
successfully carried out similar undertakings in many parts of the
country. The work has been rapidly carried forward, and the latest
statement of results is as follows :—

Contractor’s Notes. Depth in Feet. Geological Notes. Feet.
aL Nl ridepryiin San oh \ Postglacial Sandam.aaih-th, atomic
Red Marl and Pebbles ... ... 8
Rough Ballast... ... ... 12 Boulder Clay ... ... .. ... 20
Red Marl cee dines pene pace LOSI
Red Marl and Gypsum... ... 131 |
Marl, Shale, and Gypsum ... 309 $Keuper Marls... ... ... ... 611
MarlkandeShalehaternt mel ast. = |
Red Stone and Shale ... ... a)

Total depth reached ... 667 667

There is no thick bed of gypsum, but this mineral occurs per-

1 Warwickshire Coalfield, Survey Memoir, 1859, pp. 41-44.
* South Staffordshire Coalfield, Survey Memoir, 1899, p. 4.

————

="

Re ae

W. J. Harrison—Deep-Boring in Keuper Maris. 455

sistently in streaks and fibrous deposits throughout the greater part
of the strata. Many of the cores of marl brought up are remarkably
hard, affording a great. contrast to the ordinarily soft and crumbling
nature of the strata as we usually see them in a weathered condition
in brick-pits, ete.

It is possible that the “red stone and shale ”»—a hard sandy marl
—which forms the bottom bed now reached, marks the incoming of
tho Lower Keuper Sandstone. Similar strata were found at the
bottom of the Lindley Hall boring. Certainly the depth already
reached—667 feet—is the point at which our previous knowledge
would lead us to expect the change to occur. For although the first
56 feet is occupied by surface-deposits, leaving 611 feet for the Red
Marls, yet it must be remembered that we are only two miles east of
the fault, and that the upper portion of the Marls—to what extent
we cannot precisely tell—must have been removed by denudation.

Just as the boring has reached this most interesting point, an

unfortunate accident has temporarily delayed its progress. A tool
has broken in the very bottom of the boring, and the removal of the
broken piece is a difficult operation. But doubtless this obstacle
will quickly be overcome. As to the quality of the water to be
obtained from the Keuper Sandstones, the promoters of the boring
doubtless hope that it will be similar to that at Burton, where the
presence of a moderate amount of gypsum in the water from deep
wells sunk through the Red Marls is found to be of great value in
brewing operations.
_ The action of a fault when it brings a thick bed of impervious
material like clay or marl side by side with a porous sandy stratum—
the sandy beds dipping towards the line of fault—is strikingly
shown both at Birmingham and Stourbridge. In Birmingham there
is any quantity of water to be had from the Sandstones and Pebble
Beds right up to the line of fault. The artesian well, about 200 feet
deep, in Digbeth, must be within a few yards of the fault-line, and
the water obtained is used in the manufacture of mineral waters,
and is so highly prized that it may frequently be seen conveyed in
a large barrel on wheels to various establishments in the town.

At Stourbridge exactly the same thing happens. A north and
south fault brings Permian Marls on a level with the Bunter Pebble
Beds and Keuper Sandstones, the latter dipping towards the Marls.
The water is banked up by the Marls and yields an unlimited
supply to the wells of the Stourbridge Water Company, which lie
just on the right (west) side of the line of fault.

The railway company occupies the land on the marly side of the
fault, and in years gone by they sank well after well in the marls in
vain search for water, and the officials were much chagrined and
surprised at its absence, seeing that any quantity of the precious
fluid was being pumped up within a few yards of their land!

456 Prof. T. Rupert Jones—On the Paleozoic Phyllopoda.

VI.—On Patmozotc Puytiopopa.
By Pror. T. Rurerr Jonzs, F.R.S., F.G.S.1

Se: the publication of the Third Report on Paleeozoic Phyllopoda

(Brit. Assoc. Report for 1885), we have examined many
additional specimens in the Museums of the Edinburgh and Glasgow
Universities, and in the Braidwood Museum belonging to Dr. J. R. 8.
Hunter, of Braidwood, near Glasgow. Mr. James Thomson, F.G.S.,
has given us a quantity of nodules, containing remains of Ceratiocaris,
from the Lesmahago district; and other friends have lent us several
interesting specimens.

We have also again critically examined the fossils enumerated
under Ceratiocaris, in the Third Report, and, having had numerous
finished drawings carefully made for illustration of a forthcoming
monograph for the Paleontographical Society, we have been able to
compare them more perfectly and with more precise results.

Thus we find that—

1. Ceratiocaris leptodactylus (M-Coy), see Third Rep. pp. 11-14,
as known by its caudal appendages (Cambr. Mus. a/923, a/924, and
a few others), is distinct from C. Murchisoni, M‘Coy, both as to size
and proportions. We have traced two rows of pits (bases of prickles)
on a/924, as exposed. Some similar caudal appendages, M.P.G. 44,
occur in the Lower Wenlock rock of Helm Knot, Dent, Yorkshire.

2. C. Murchisoni (Agass.), founded on some specimens figured in
Sil. Syst. and Siluria, but unfortunately lost (Third Rep. p. 11,
etc.), is represented by several analogous fossils, such as Oxford Mus.
Band C; Ludlow Mus. C; M.P.G. 22 and 23. We find only one
row of pits on the styles, as exposed. We have been unable to deter-
mine its carapace; but a fragment lying in the same slab with 23
may belong to it. The carapaces formerly assigned to C. leptodactylus
and C. Murchisoni (Third Rep. pp. 12, 15) are now regarded as
belonging to distinct species.

3. The caudal appendages of C. Murchisoni have a slight curva-
ture; there are others much like them, but straight, and associated
with a large ultimate seement, much broader than that in M.P.G. 2%.
(For instance, Oxford Mus. F; M.P.G. X 4; Ludlow Mus. T.) One
of these (X 4) has been labelled ©. gigas by Mr. Salter; and there-
fore we adopt that name.

4. The specimens from the Wenlock beds of Dudley and Kirkby
Lonsdale, described and firured in the Guor. Mac. 1866, p. 204,
Pl. X. Figs. 8 and 9, as belonging to C. Murchisoni (Third Rep.
p- 12), are too thick and strong for that species, and the Dudley
example (Fig. 8) has different proportions. We propose to distinguish
them as C. valida.

5. Some abdominal segments (Oxford Mus. E; Ludlow Mus. L;
B.M. 39403; M.P.G. 2% and 32; Third Rep. p. 20, ete.), narrow in

1 Being the substance of the Fourth Report of a Committee consisting of Messrs. R.
Etheridge, F.R.S., H. Woodward, LL.D., F.RS., and Prof. T. Rupert Jones,

F.R.S. (Secretary), on the Fossil Phyllopoda of the Paleozoic Rocks, read before
Section C, British Association, Birmingham, Sept. 8, 1886,

Prof. T. Rupert Jones—On the Paleozoic Phyllopoda. 457

proportion to those in other specimens marked 2%, and referred to
C. Murchisoni, and very much narrower and smaller than in C. gigas,
we separate as a new species, to be called C. attenuata. They have
straight styles and stylets, very much shorter than in either of the
foregoing.

6. Two small specimens of crushed telsons (one in Mr. Cocking’s
collection, and the other M.P.G. X 3x, both from the Ludlow series),
probably smaller than C. Murchisoni, have a fluted or channelled
sculpture on their upper part, instead of either wrinkles or leaf-
pattern; hence they may be regarded as belonging to a distinct
form, for which the name canaliculata will be convenient.

7. One fine large carapace (M.P.G. X +) and others smaller and
less definite in some respects (M.P.G. X4+; X4%; X4%:; Ludlow
Mus. A; Oxford Mus. K and J), and associated with segments and
appendages, we regard as distinctive of a new species, though hitherto
referred to C. leptodactylus (Third Rep. pp. 12, 15). The test
appears to have been of an unusually solid consistency.

These carapaces in some instances have been much modified by
pressure, but we trace a close similarity throughout the series, allow-
ing for probable differences of age. The shape approximates to that
of Dr. James Hall’s species C. acuminata and F. Schmidt's C.
Noetlingi (Third Rep. p. 30). There are marked differences, how-
ever, and we intend to designate this form C. Halliana, in honour of
our old friend, who began working at these Phyllocarida as early as
1852.

A perfect specimen of C. acuminata, Hall, has been lately described
and figured by Dr. Julius Pohlman in the Bulletin of the Buffalo
Society of Natural Sciences, vol. v. No. 1, 1886, pp. 28, 29. pl. 3,
fig. 2. Its caudal appendages are much like those of C. papilio and
C. stygia, the style being relatively short, and the stylets broad and
blade-like. The appendages in M.P.G. X +, X4, and Ludlow Mus.
A are different from these, being thinner, tapering slowly, and pitted
in at least one row, as exposed.

8. C. Pardoeana, La Touche. Two carapaces with segments and
parts of appendages from Ludlow (Ludlow Mus. B and 1D; Third
Rep. p. 12) differ from any other form. One of them (B), with a
wrong caudal appendage attached to it, in the Ludlow Museum, has
been labelled ‘ C. Pardoensis,’ and as such is referred to in J. D. La
Touche’s Guidebook to the Geology of Shropshire. We retain this
name (altering the termination, as it refers to a person, and not a
place) for the two carapaces here referred to. One of them (B) is of
special interest as having its rostrum still in place.

9. The fine large specimen of C. ludensis, H. W. (Third Report,
p- 16), has been again carefully studied, and we find reason to believe
that the caudal appendage which appears longest in the fossil was
not really the longest, or the true telson, but was one of the ‘laterals’
or stylets. Hence the whole animal was probably much longer than
our former estimate made it.

10. C. robusta, Salter (Third Report, p. 24), being based merely
on some small caudal appendages (Cambridge Museum a/925 and

458 Prof. T. Rupert Jones—On the Paleozoic Phyllopoda.

a/926) without carapaces, is troublesome and unsatisfactory to deal
with. We find some equivalent styles and broad blade-like stylets,
like long scalene triangles, in C. papilio, stygia, acuminata, etc. ; but
none of these seem small enough for the several little sets of trifid
appendages, more or less perfect, which we have met with. C. robusta
takes in some of these; but Oxford Mus. T is relatively broad, and
might be termed lata; B.M. 58878, from Muirkirk, has very narrow
members (angusta) ; and one set in the Owens College is so neat,
symmetrical, and small that it might be called minuta.

11. The specimens Ludlow Mus. S. and M.P.G. X-3;* have each
a long style and a strong stylet attached to a broken ultimate
segment, and were regarded as var. longa in the Third Report,
p- 25. Although not showing the lattice-pattern so often seen on
the segments of C. papilio and C. stygia, they may well belong to one
of those species, and the ornament may have flaked off from the
ultimate segment. The study of C. papilio and stygia (Third
Report, pp. 16-20) we have not yet exhausted by any means. We
know, however, that the abdominal segments were delicately sculp-
tured with leaf-like or lattice-pattern ornament, the points of the
triangles pointing upwards, or rather backwards, towards the cara-'
pace, and one limb of the triangle, where free, running downwards
and outwards in the other direction. These oblique lines are often
visible when the triangles have disappeared from wear or decom-
position. Among many others the segments M.P.G. X 7;'; B.M.
41900; Oxford Mus. A and H exhibit fine examples of this leaf-like
ornament; and it is visible in several more complete individuals in
those collections. In the Braidwood and Glasgow Museums numer-
ous specimens show it well. See also Third Report, p. 31.

12. A small and very delicate specimen, B.M. 59648, has a thin
subovate carapace, with excessively fine parallel longitudinal striz,
and shows 14 or 15 segments, some within and five outside the
carapace, ending with a neat trifid set of appendages. ‘This differs
from any other form we know; and probably some small loose
bodies, of numerous segments, occurring in the Lesmahago shales
(Third Report, p. 20) may be of the same species. Its looseness
of structure would suggest the name laxa.

13. Of C. Salteriana, noticed as a new species in the Third
Report, p. 28, we have not yet seen any additional specimens.

14. The specimens which we referred to in the Third Report
pp. 23 and 24, as C. cassia, Salter, are separable into two forms.
C. cassia proper is recognized on an interesting slab, of which one
counterpart is in the Ludlow Museum (HE and F) and the other
in the Museum of Practical Geology at Jermyn Street, London (X+).
The other, somewhat similar, but larger and otherwise different,
specimens are not unlike in the characters of the carapace, but they
have more abdominal segments exposed and proportionally longer
caudal appendages—M.P.G. X;; B.M. 389400; Ludlow Mus. K ;
Oxford Museum L and Q. These might be conveniently named
C. cassioides.

Jn all the specimens of both kinds the carapace has been ap-

Prof. T. Rupert Jones—On the Paleozoic Phyllopoda. 459

parently thin and tough, so as to allow of their being crumpled very
much. This condition and the presence of harder parts of their
internal organs beneath give rise to various tubercular irregularities
of the surface, in some cases simulating ocular tubercles. There are,
however, no real eye-spots. There may have been irregularities of
the surface, due to the attachment of the muscles of the jaws within
the body.

15. An ovate carapace, represented by a mere film, and five
abdominal segments, with a neat trifid tail, all flattened but very
distinct, have no close ally among the known forms. The segments
are delicately striate, with oblique lines on each side, suggesting
the name compta, which we propose for this specimen—Ludlow
Museum HE.

16. To C. inornata, M‘Coy (Third Report, pp. 20, 21), we have
nothing to add, except that some large specimens (so named,
Cambridge Mus. b/35) have a greater proportional depth (height)
at the ventral border than smaller individuals, and yet have the same
general outline and posterior slope, as well as the longitudinal lineate
ornament. (The presence of this sculpturing is not in accordance
with the trivial name.) These large specimens may belong to
C. stygia.

In the Cambridge Museum is a specimen (0/36) of two abdominal
segments, with a style and a stylet in good preservation, being
convex and not injured by pressure. The penultimate segment
is smooth, but shows faint traces of oblique lines; the ultimate is
quite smooth and cylindrical; the telson (style) is attached by an
apparently rounded joint; and the two uropods much resemble some
of those referred to C. robusta. This specimen is from Benson Knot,
and is labelled C. inornata ; but the evidence of its specific relation-
ship is supported only by its having been found in the same rock,
and by its size suiting the large form of C. inornata? (b/85). It
belongs possibly to C. stygia.

17. From the list for C. inornata, given in the Third Report, we
have to remove one of the specimens found at Benson Knot, and
marked ‘44342’ in the British Museum, being decidedly different
in outline (more ovate), though similarly marked with longitudinal
strie. It might well be named C. Ruthveniana, in memory of the
old geological collector who laboured for very many years in the
Kendal district for Professor Sedgwick and others.

18. C. oretonensis and truncata, H.W. (Third Report, pp. 21, 22),
though near to C. inornata in shape, hold their distinct places as
species.

19. Of C. solenoides and C. gobiiformis (Third Report, p. 22)
there is nothing new to be stated.

20. As intimated in the Third Report, pp. 27, 28, the presence
of the ocular tubercle has an important signification, showing that
the animal must have had an organ equivalent to the eye sufficiently
developed to affect the external covering, whether it was adapted
for clear vision or not. It may bea family distinction ; at all events,
the oculate carapaces have to be removed from Ceratiocaris and we

460 Prof. T. Rupert Jones—On the Paleozoic Phyllopoda.

propose that M‘Coy’s C. elliptica be referred to a new genus under
the name Hmmelezoe.'

E, elliptica, M‘Coy, is described in the Third Report, p. 27, as
represented by the type, Cambridge Mus. 6/15; but Ludlow Mus. G,
and M.P.G. X+'5 and 34 differ from it considerably. The first of
these is shorter and broader (higher), nearly semicircular in outline,
with an acute and projecting postero-dorsal angle; and its surface
has a fine, almost silky, linear ornament. As a new species this
might be known as HE. tenuistriata. The specimen X-j; is subovate,
larger than either of the other two, and is coarsely striate, with
longitudinal anastomosing wrinklets and might be named EL. crassi-
striata. M.P.G. 33 is smaller than any of the foregoing, somewhat
boat-shaped, between the last and elliptica in shape, but not identical
with either; and it is rather coarsely striate longitudinally. To
this form we propose to give the name H. Maccoyiana, in honour of
the first describer of any member of this genus.

21. At page 26 of the Third Report, we described Salter’s Ceratio-
caris ? ensis,and now we are still more confirmed in the opinion that
it belonged to a distinct genus. Its large size, its curvature, and the
serration on both the upper and the lower edge, and the profuse
Spination (as shown by pits) on the latter distinguish it from other
telsons; and more particularly its lozenge-shaped sectional area, of
an unequal rhombic form, blunter at the outer (upper) and convex
edge than on the other, the ridge along the sides not being quite on
the medial line, but nearer the outer than the inner edge. We pro-
pose the name Xiphocaris? for this rare genus.

M. Barrande’s Ceratiocaris primula (Third Report, p. 82) has a
style (or stylet?) with lozenge- or diamond-shaped section; but this
uropod, though curved, is of different dimensions, and is pitted
all over.

22. Physocaris vesica, Salter (Third Report, p. 28) we consider
as having had its abdominal segments shifted from below upwards,
and turned over on their axis, after death; and therefore as having
been figured upside down.

23. Of C.? lata, insperata, and perornata we have no further
evidence at present.

24, Ceratiocaris ? longicauda, D. Sharpe (Third Report, p. 29),
a foreign (Portuguese) form within our reach has been studied in
the Geological Society’s Museum, Burlington House, and shows some
interesting features. Its scientific name was given under the suppo-
sition that the fossil was a Dithyrocaris, with a longer abdomen than
usual ; but its cylindrical ultimate segment, its somewhat bayonet-
shaped’ style, and blade-like stylets clearly remove it from that
genus, as intimated in our former notice. It is probably distinct
also from Ceratiocaris; it has some analogy with the Devonian
Elymocaris ; but at present we cannot fix its generic place.

25. In the Sitzungsh. K. bohm. Ges. Wiss. 1885, M. Ottamar
Novak, Keeper of the Barrande Collection at Prague, has described

1 -Eupedns, elegant ; (wh, life (a termination common in some of M. Barrande’s
genera). 2 Bipos, a sword; kapls, a shrimp.

Prof..T. Rupert Jones—On the Paleozoic Phyllopoda.

461.

a new Phyllocaridal genus from the étage F, f 2, in Bohemia, as
Ptychocaris, with two species Pt. simplex and Pt. parvula, character-
ized by a strong and obliquely longitudinal ridge or sharp fold on
each valve, and by an anterior group of three small nodules, an
ocular tubercle behind them, and some larger but less distinct

30.
36.

37.

. CO. angusta
. C. minuta

. C. cassioides
RIC COMUDUG) peasene- ioe

. OC. decora
. C. oretonensis
. C. truncata

. C. inornata

. O. solenoides

. C. perornata

. C. 2 insperata

Species of
CERATIOCARIS,
PHyYsoCcARIS,
XIPHOCARIS,
and
EMMELEZOE.

Ceratiocaris lepto-

dactylus
C. Murchisoni
C. gigas

eee c eens eee
ee eeee

ee ccc eee cene

C. Halliana
C. Pardoeana
C. ludensis
C. robusta
C. lata

ee eas
C. stygia
C. laxa

ee eee eee eeee
woe ncesenees

sews ceree

C. gobiiformis ......
a a

stew eee eeees

Cb 2 SDs dcceesssosngose

. Physocaris vesica ...
. AXiphocaris ensis
. Emmelezoe elliptica

EE. tenuistriata
Ei. crassistriata

eeeeee

EL. Maccoyiana

Carboniferous Limestone ;
Oreton.

Reet ce oe eS Tre

Ludlow Beds.

Wenlock Beds.

Upper Ludlow;
Ludlow.

= S 5
3 he ey
SBS Nita
BSies| 33
Seles Ee
BM /S6 = 3
ac | 3 OA
EXOR |S. Ea
PE} om og
oO) 2s As
1s)
—|— x
— | — x
a al eer x and
Knighton.
—|— x
a x
—|— x
—|— x
—|— x
—|— x
— x
— || —= x
sare lexol
Pll se i
== || x
——) | — 5
—|— x
— |— x
— | — x
Freshwater
Sat |i Ebemproke=
shire.
x
X
x
x
x
= = x
= — x
x
= | — x
= | — x

fe} ll , aes
oo AO Rie a 48
eyles/=./8a
aSei/So]/Ho]a
NA|N= 146) 8s
ae | SS oS
inl ao So =
oo oe ont |\=s fl
BE|EP MS] M
EWS pS
PAA en Sa]
i) a)
Se = Ho
Dudley.
DS
|
_— x x
x

Upper Llandovery ;
Onny River.

x

Tremadoc Slates ;
Portmadoc

462 Notices of Memoirs— Geological Survey of India,

swellings further back, but still in the antero-dorsal region. M.
Novak supplies also a table of the vertical distribution of the Phyllo-
carida in Bohemia.

In the Annales XIII. Soc. Géol. du Nord, 3™° Livr. April, 1886,
p. 146, M. E. Canu gives a résumé of the results of M. O. Novak’s
researches in the Phyllocarida, with some woodcuts of Aristozoe
regina, Bactropus longipes, and Ceratiocaris debilis (see Third
Report, pp. 82-84), and of Ptychocaris simplex (see above).

26. Dr. A. S. Packard, jun., has described and figured some
peculiar appearances on an internal cast of a Carboniferous Phyllo-
podous carapace from Illinois, as traces of four pairs of lamellate
limbs (thoracic feet), probably “ the homologues of the exopodites of
Nebalia.” He has defined the genus and species as Cryptozoe pro-
blematica (American Naturalist, Hxtra, Feb. 1886, p. 156; and
Proceed. Americ. Philosoph. Soe. vol. xxiii. No. 123, pp. 880-383).

27. In a Geological Report, Assembly Document, No. 161, 1885
(or 1886), Mr. J. M. Clarke has defined the localities and geological
succession in Ontario County and New York, where the Phyllopods
which he previously described (see ‘Second Report,’ 1884, pp. 80-86,
and ‘Third Report,’ p. 5) have occurred with or without Goniatites.

28. A list of the British Paizeozoic Phyllocarida described in the
Third and Fourth Reports is given on the preceding page (p. 461).

INGSmEaChS) - Gist aye vieSnsySt

So

J.—Recorbs or THE GrotoeioaL Survey or Inpia, vol. xix. pt. 2.

WO short papers in this part relate to the disputed age of the
beds in the Salt Range, containing species of Conularia. The
first is “A Note on the Olive Group of the Salt-range,” by R. D.
Oldham, A.R.S.M., and the other ‘“ Memorandum on the Discussion
regarding the Boulder-beds of the Salt-range,” by H. B. Medlicott,
F.R.S. Mr. Oldham visited the locality in the Salt-range, in which
the Conularia beds occur, and states that the thin band of gravel in
which they appear is the last kind of rock in which one would
a priori expect concretionary nodules to be formed. At the same
time he believes that for the most part these fossiliferous pebbles
were originally concretionary nodules, and that they have been
transported into their present position. From the character of the
associated pebbles in the beds beneath, he believes that the original
position of the beds from which the Conularias come must have been
to the southward of where they now are. He further concludes
from the stratigraphical relations of the beds, that the Olive group
(including the gravel-bed with Conularia) is homogeneous, and must
be associated with the overlying nummulitic beds, rather than with
the underlying Paleeozoic or early Secondary beds.

Mr. Medlicott does not admit that the petrological evidence brought
forward by Mr. Oldham is altogether conclusive as to the transported
origin of the fossiliferous pebbles, though it would be “almost absolute
if he could assert that the ground-mass of the gravel-bed is quite

Notices of Memoirs—Carboniferous Limestone. 463

different from that°of the fossiliferous pebbles in the bed.” Further,
even supposing the correctness of Mr. Oldham’s theory, that the
fossiliferous pebbles are concretionary nodules, it does not at all
explain the presence of this small special fauna in a distinct bed by
itself. Mr. Medlicott asks the following pertinent question: “Is it
conceivable that in Upper Cretaceous time, when the abundantly
fossiliferous Permian and Secondary deposits were in force in the
neighbourhood, and presumably exposed to denudation, if older
deposits were so, a special collection of fossils from those older
fossils can have been raked together, transported together, and
deposited together at a distance, by the promiscuous process of
detrital agency?” “So long as special Paleozoic fossils only are
found in these beds, their Upper Cretaceous age will be open to
doubt.”

This argument has great force; and evidence of a more decided
character will be required, before the relative age of the Conularia
beds, and the boulder-beds underlying them, can be regarded as
settled. G. J. H.

IJ.—Memoirs oF THE GrotocicaL Survey or Inpra. Patmonro-
Locica Inpica. Ser. xiiii Saut Rance Fossits, by Wititam
Waacen, Ph.D., F.G.S., and Joserpa Picut. IJ. Propuctus-
Limestone Fosstis: 5. Bryozoa—AnneLipA—EcHINoDERMATA.
With ten plates, 87—96.

HE authors reject from the Bryozoa, and regard as Corals, such
forms as Stenopora, Monticulipora, and allied genera. The

Bryozoa described belong to the families of the Fenestellide and

Thamniscide. In the first of these families the following species

are recorded: Venestella perelegans, Meek, F. jabiensis, n., Polypora

Koninckiana, n., P. megastoma, Kon. sp., P. gigantea, n., P. ornata,

n., P. sykesi, Kon. sp., P. biarmica, Keyser, P. vermicularis, n., P.

transiens, n., Phyllopora jabiensis, n., P. cribellum, Kon., P. haimeana,

Kon., Synocladia virgulacea, Phill., Goniocladia indica, n. In the

family Thamniscide are ranged Thamniscus dubius, Schlot., T. serialis,

n., and Acanthocladia anceps, Schlot. In the Annelide, Spirorbis

helix, King, and Serpulites indicus, n., are described. Fragmentary

plates and species of Hocidaris Forbesiana, Kon., are noted. The

following species of Crinoids are present : Oyathocrinus goliathus, n.,

C. virgulensis, n., C. indicus, n., C. Rattaensis, Hydriocrinus ? sp. indt.,

Poteriocrinus, sp. indt., and Philocrinus cometa, Kon. The descrip-

tions of these species are very carefully and fully drawn up, and

they are excellently illustrated in the accompanying plates. G.J.H.

IlJ.—Nortcz sur LE PaRALLiLIsME ENTRE LE CALCAIRE CARBONIFERE
DU NORD-OUEST DE L’ ANGLETERRE ET CELUI DE LA BELGIQUE;
par L. G. pe Koninox et Maximin Louzst. (Bruxelles, Bulletins
de Académie royale de Belgique, 3™° série, t. xi. No. 6, 1886.)
NE of the authors has lately examined the horizontal beds of

conglomerate of white quartz pebbles in a calcareous matrix,
which, in the neighbourhood of Ingleborough, rest unconformably
on Silurian strata, and form there the base of the Carboniferous

464 Notices of Memoirs— United States Geological Survey.

system. The fossils in these beds comprise, amongst others, Zitho-
strotion basaltiforme, species. of Amplewus and Zaphrentis, and teeth
of Placoids, some of which are recognized as Lophodus levissimus,
Ag., and Copodus cornutus, Ag. Resting on the conglomerates are
grey limestones with an abundance of Chonetes papilionacea, Phill.
In these, and the beds below, Productus gigunteus is conspicuously
absent, whilst it is extremely abundant in the limestone beds of the
series above. In the Belgian Carboniferous Limestone series there
are no conglomerates like those at Ingleborough, but at the base of
the limestones with Productus giganteus and P. cora, forming the
‘Calcaire de Visé,’ there are some beds distinguished by the abun-
dance of Choneies papilionacea, and between these and the Upper
Devonian strata there is a great thickness of beds containing Corals and
Placoid teeth, analogous to those in the Ingleborough Conglomerates,
and the authors therefore conclude, that these Lower Limestones,
beneath the Caleaire de Visé, are represented in part by the Yorkshire
Conglomerates, which are not more than about 180 feet in thickness.
On the other hand, the zone of Productus giganteus in the north of
Yorkshire attains a much greater thickness than in Belgium.

G. J. H.

TV.—Firra Annuat Report or THE Unitep States GEOLOGICAL
Survey, 1883-84. By J. W. Powertt, Director. 4to. pp. 469,
58 Plates and 143 Figures. (Washington, Government Printing
Office, 1885.)
T the beginning of this massive volume the Director of the
Survey gives an epitome of the work carried out, together
with the financial statement, from which it appears that the year’s
expenditure for the Survey amounted to nearly 380,000 dollars, or
about £67,300. This is followed by brief administrative reports of
chiefs of divisions and heads of independent parties, from which
an idea may be formed of the extent and variety of the operations
included in the Survey. Thus, the chief geographer, Mr. Henry
Gannett, reports that topographical field work had been actively
carried on by different parties in Northern California, Arizona, New
Mexico, Montana, the Yellowstone Park, Massachusetts, the Denver
District of Colorado, and part of the Elk Mountains. The party
under the charge of Mr. Arnold Hague was engaged in working out
the geology of the Yellowstone National Park, and studying the
physics of geyser action in that district. Mr. T. C. Chamberlain
reports on the investigations made by himself and others under him
in tracing out the moraines and other glacial deposits in the upper
valleys of the Mississippi and Missouri, in Dakota, and also in
Tllinois, Indiana, Ohio, and Kentucky. ‘The division under Prof.
Roland D. Irving is engaged in a general investigation of the
Archean formations of the North-western States, and its field of
operations extended from Northern Michigan to the country on the
north-west of Lake Superior. Dr. F. V. Hayden studied the relations
of the Laramie Group and other Cretaceous rocks, exposed between
the Missouri at Bismark, Dakota, and the Yellowstone at Glendive,
Montana. Mr. G. K. Gilbert and his assistants carried on their

Reviews—Prof. Cope—Tertiary Vertebrata of the West. 465

work of investigating the Quaternary Lakes of the Great Basin in
Utah and California. Mr. W. J. M‘Gee reports on the progress made
in preparing a general geological map of the United States, as well
as on his studies of the superficial deposits of the district of Columbia
and adjacent territory. Captain C. KE. Dutton is engaged in studying
the chain of volcanoes constituting the Cascade Range in California,
Oregon, and Washington Territory. Mr. 8. F. Emmons reports on
mining geology of the Rocky Mountains, and Mr. G. T. Becker on
the quicksilver mining district of Knoxville in California. Prof.
O.C. Marsh states that eight different parties were engaged in collect-
ing fossils in Oregon, Wyoming, Kansas, and Nebraska, and that his
monographs on the Sauropoda and the Stegosauria were in course of
completion. Dr. C. A. White was engaged in studying the Laramie
Group on the Upper Missouri, and on various paleontological
investigations in Washington and California. Mr. C. D. Walcott,
assisted by Prof. H. 8. Williams and others, has studied the Devonian
and other Paleozoic rocks of New York, Tennessee, Virginia, Vermont
and Alabama. Mr. Lester F. Ward has been collecting and arrang-
ing the fossil plants of the Fort Union Group on the Yellowstone
and Upper Missouri rivers. The chemical work of the Survey is
directed by Mr. F. W. Clarke, whilst Mr. A. Williams is engaged on
the statistics of metals; and, finally, Mr. G. W. Shutt traces the
course of a preliminary geological investigation in Virginia.

These administrative reports, however, only occupy sixty-six pages
of the volume; the remaining 400 pages contain a series of elaborate
essays on different branches of geological science, each of which is
treated in considerable detail, and abundantly and beautifully illus-
trated. We can here but mention the titles of the different treatises
and the authors’ names, and refer the reader to the volume itself.
The first treatise is on ‘‘ The Topographic Features of Lake Shores,”
by G. K. Gilbert. This is followed by ‘The Requisite and Qualifying
Conditions of Artesian Wells,” by T. C. Chamberlain; “ Preliminary
Paper on an Investigation of the Archean Formations of the North-
Western States,” by R. D. Irving; “The Gigantic Mammals of the
Order Dinocerata,” by Prof. O. C. Marsh; “Existing Glaciers of
the United States,” by T. C. Russell; and “Sketch of Paleobotany,”
by Lester F. Ward. G. J. H.

BEY) G2 VG dE Ja OWN Se

DEPARTMENT OF THE INTERIOR. Report oF THE Unirep Sratss
GEOLOGICAL SURVEY OF THE TERRITORIES. F. V. Haypen, Unitrep
Srares GEoLocist-In-CHarce. Votume II]. Tur Vertesrata
or THE TrRTIARY Formations or THE West. Boox I. By
Epwarp D. Cort, Member of the National Academy of Sciences.
(Washington, Government Printing Office, 1883.)

(Continued from p. 419.)

ATS are scantily represented in the Bridger fauna, the only
American species described by Professor Cope being Vesperugo
anemophilus, which has the inferior molars like those of Didelphys.
DECADE I1I.—VOL. III.—NO. X. 30

466 Reviews—Prof. Edward D. Cope—

We now turn to the group division of hoofed mammals. The first
order, which the author names TaxEopopa, comprises animals, in
which the carpus and tarsus form two rows, with the bones of the
first row supported by the second row, each for each, so as not to
alternate. The order is defined as having the scaphoid bone supported
by the trapezoid, and the lunar bone supported by the magnum. The
cuboid bone articulates proximally only with the calcaneum. This
group comprises the Hyracorpga, in which the fibula articulates with
the astragalus, and the ungual phalanges are truncate; secondly,
the ConbDYLARTHRA, in which the fibula does not articulate with
the astragalus or calcaneum, and the ungual phalanges are pointed.
A third group may be formed by the Toxovontta, or the Toxodontia
may belong to the Proboscidea.

The Amptypopa is an order which is subdivided into two groups,
first, Pantodonta, which has a third trochanter to the femur, and
incisor teeth in the upper jaw; and secondly, Dinocerata, which
has no upper incisors, and no third trochanter. The Amblypoda
are defined from the Proboscidea, chiefly by the shortness of the
navicular bone, which allows the cuboid bone to articulate with the
astragalus.

The name Dretartura is used as an ordinal name for the Perisso-
dactyla and Artiodactyla, in place of the name Ungulata, which is
made to include all hoofed mammals.

This classification is exhibited in the following diagram :—

' TAXEOPODA.
| |
Condylarthra Platyarthra
(hypothetical).
Hyracoidea
PROBOSCIDEA AMBLYPODA
|
Taligrada
|
Hyodonta Pantodonta
(hypothetical).
| Dinocerata
DipLARTHRA

Perilebdactyla heehee

The carpal modification which characterizes the Diplarthra is
explained as a rotation of the bones of the second carpal row upon
those of the first row, in which they move to the inner side, a con-
dition attributable to the loss of the pollex, by which the weight of
the body is thrown chiefly on the third and fourth digits. And
seeing that this condition has brought about the alternation of the
two rows of carpal bones, producing a stronger carpus, the author is
disposed to regard the modification as accounting for the survival of
the Diplarthra, while most of the mammals which have a serial
arrangement of the carpal bones have become extinct.

The Amblypoda is intermediate between the Taxeopoda and Di-
plarthra, in having the carpus of the more complicated type. The
Taxeopoda approach most nearly to the Bunotheria, especially the
Mesodonta, from which they are distinguished by their hoofs,

Tertiary Vertebrata of the West. 467

though some Creodonts like Mesonyx have claws which are almost
hoofs in character.

The Condylarthra comprise three families; they are primitive
ungulates, with five-toed, plantigrade feet, with the astragalus like
that of the Creodonta and Carnivora, and have other characters known
only among Unguiculates. The lowest representative of this group
is the Periptychide. It comprises four genera. In Periptychus the
inferior premolar teeth have internal lobes, while in the other genera,
Anisonchus, Hemithleus, and Haploconus, the internal lobes are want-
ing. The crowns of the true molars have seven tubercles; the
canines are of moderate size, and the inferior incisors small.

Upper Jaw (a). Mandible (6). Periptychus rhabdodon.

Periptychus rhabdodon.

The true molars in the mandible have four principal cusps, in
opposite pairs, with accessory median cusps in front and behind. The
angle of the lower jaw is not inflected, and the coronoid process

468 Reviews—Prof. Edward D. Cope—

rises near to the condyle. The cerebral hemispheres are long and
narrow, divided by a long flat crus from the olfactory lobes, which
are nearly as wide as the cerebral hemispheres. The affinities of this
type are not, however, regarded as absolutely determined. ‘The
premolar teeth have a sculpture which is not unlike that seen in the
fourth premolar of Ptilodus, yet there are no other reasons for sup-
posing it to be marsupial. The characters of the astragalus are not
unlike those seen in the Creodonta, but other structures indicate that
it was probably ungulate. Three species are known, among which
P. rhabdodon is fully described. Its cervical vertebra are as short as
in the Elephant. The humerus especially, in its small tuberosities,
suggests the Proboscidea, though the animal was only about the size
of the Collared Peccary, and is thought to have had much the aspect
of the short-necked Bear. The teeth indicate omnivorous habit. It
is the most abundant Mammal of the Puerco beds. Many of the
other types in this family like the species of Hemithleus, Anisonchus,
and Haploconus, are known from little more than the dentition, which
varies in the number and form of the cusps of the upper molar and
premolar teeth.

The Phenacodontide is an allied group of four genera, in which
the teeth have much the same general plan as that just described.
Protogonia has but one external lobe in the upper premolar teeth.
In Phenacodus the fourth premolar has two external lobes, while in
Diacodexis the two external lobes are found in the second, third, and
fourth teeth. .

Upper. Side.

mi

q i

“Nn is

Brain of Phenacodus primevus.

Professor Cope’s earlier and brief account of Phenacodus has
already been reproduced in the February Number of this MaGazinz.
The detailed description now given is a monograph extending to
more than sixty pages. The skull in this type is remarkable for the
anterior shortening of the nasal bones, so as to give a superior aspect
to the nostrils, and these bones extend back closer to the orbit than
is usual in Eocene genera, making a slight approach to the Tapir.
The slender premaxillary bones are not united in front; and the
rami of the mandible have no bony union. The cerebral hemi-

Tertiary Vertebrata of the West. 469

spheres are unusually small, being only one-fourth longer than the
cerebellum, from which they are separated bya thick tentorium. In
the same way, deep grooves divide the hemispheres from each other,
and from the olfactory lobes in front. Nine species are recognized,
seven of which are defined by the characters of teeth in the mandible.
In the description of P. Vortmani indications are given that the
spine of the scapula is recurved, as in the Amblypoda and Proboscidea;
while the bone differs chiefly from that of the Dinocerata and
Proboscidea in the addition of an acromion, which gives a resem-
blance to some Rodents like the Squirrel. The tuberosities of the
humerus are less developed than in most Diplarthra. The propor-
tions of the ulna and radius are similar to those of Hyraz, but the
distal articulation of the ulna is like that of a Carnivore. The
pelvis is intermediate between that of Hyrax on the one hand and
Canis and Ursus on the other. The femur is rather more robust than
that of the Tapir. The astragalus is small, and resembles that of
Hyrachyus. This species was about as large as a Bulldog, but with
a smaller head and shorter neck, which had more the proportions of
a Raccoon. The feet resembled those of the Tapir or Rhinoceros,
but with a pair of short toes on each side which did not reach the
ground. The tail was like that of a Dog.

The third family of Condylarthra, Meniscotheriide, includes the
single genus Meniscotherium. The animal was about as large as a
Fox, less slender than Phenacodus, with a short muzzle and large
eyes, the robust proportions of a Raccoon, and a large tail. It was
one-third larger than the Cape Hyrax, probably a vegetable feeder.
and distinguished by its dentition. The upper molars have inter-
mediate tubercles, of which the anterior are crescent-shaped, the
posterior oblique. The inferior molars and last premolar have two
V-shaped folds. The brain cavity is relatively larger than in Phena-
codus. ‘Three species of the genus are known. The comparisons
chiefly indicate relations with Phenacodus and Hyracotherium.

The Amblypoda next claim attention. This group comprises
mammals with small cerebral hemispheres, which leave the olfactory
lobes and cerebellum exposed. The species have short plantigrade
feet, terminating in the known genera in five digits, which have
flat hoof-bearing terminal phalanges. The seven bones of the carpus
are distinct. The molar teeth have wide crowns and crests invested
with enamel. The structure of the feet indicates an affinity to the
Proboscidea, which is most obvious in the hind foot, the principal
difference being that, while the navicular bone extends over the
distal end of the astragalus in Proboscidea, the navicular bone is sO
short in Amblypoda as to allow the cuboid to come in contact with
the astragalus. The nearest approach to this condition of the
Amblypoda is seen in the Miocene Perissodactylate genus Symborodon,
where the cuboid and navicular facets are flat, and separated by an
oblique line, so as to be similarly incapable of hinge-like movements.
In the fore foot the difference between Amblypoda and Proboscidea
consists in the alternating position of the elements of the two carpal
rows. This alternating condition is usual in the cold-blooded

470 Reviews—Prof. Edward D. Cope—

Vertebrata; and is characteristic of the other existing orders of
hoofed Mammals, while in the Proboscidea and Hyracoidea the
elements of the two rows of carpal bones have an opposite and
longitudinal mode of arrangement. In Amblypoda the plan of con-
struction of the fore foot is about equally related to Proboscidea,
Perissodactyla, and Artiodactyla. The brain shows affinities with
Cheiroptera, Insectivora, and Edentata. In this relation, the forms
of the teeth in some Insectivora show interesting resemblances to the
fossil genera Coryphodon and Bathyopsis; while the small smooth
cerebral hemispheres and relatively large size of the optic and
olfactory lobes in Amblypoda make a nearer approximation to the
Creodonta than to any existing group of Mammals. On the whole,
the Amblypoda are to be classed as the most generalized order of
hoofed Mammalia. They preceded the other groups in time, and
may therefore hold an ancestral relation to them. The order is
divided into two suborders; first, the Pantodonta, which has superior
incisor teeth and a third trochanter to the femur; secondly, the
Dinocerata in which both these characters are absent. Both groups
have short cervical vertebree without ball and socket-joints, inter-
mediate in character between those of Proboscidea and other Un-
gulates,—characters with are repeated in the scapula, ilium and
many details of the skeleton.

y

Of

y Ju) EE
ee ea AL Ca)

sss
Sea =

Skull of Coryphodon elephantopus, 2 natural size, seen from below.

The Pantodonta in America comprises five genera, Bathmodon,
Ectacodon, Manteodon, Coryphodon, and Metalophodon, and are
limited at present to the Wasatch beds in the Rocky Mountain
region. Metalophodon may possibly be identical with Bathmodon,
since its feet are at present unknown. In the Pantodonta the
symphysis of the mandible is furnished with teeth. The upper
surface of the astragalus is flat or concave in the middle, and turned
inward ; it has a large vertical fibular facet,—characters which are
shared with the Dinocerata. The coracoid process of the scapula is

Tertiary Vertebrata of the West. 471

produced into a curved hook. The neck is longer than in the
Dinocerata.

The genus Manteodon has two interior cusps to the last upper
molar tooth, and all the upper molars have a marked V shape.
Ectacodon has only one inner cusp, and one external cusp to the
last upper molar, while only the two anterior molars have the
posterior V form. Coryphodon has no external cusp; and the
astragalus is transverse, with an internal hook. This genus is
thought to have resembled the Bears in aspect more than any living
animals, except that their feet were more like those of the Elephants.
The feet indicate a heavy elephantine type of movement, owing to
the inflexibility of the ankle. The species varied in size between
the bulk of a Tapir and that of an Ox; they were omnivorous, though
armed with tusks in both jaws, which are fully as marked as those of
Carnivora. There are about twelve American species, some of which
are well known from New Mexico. They are distinguished chiefly
by relative length of the premaxillary bones, and variations in
development and form of the cusps and tubercles of the teeth.

The material for an account of this genus is less full than in
Professor Cope’s report in Lieut. Wheeler’s survey. The species
C. elephantopus most nearly approaches the genus Manteodon, and is
defined by the inner half of the posterior crest of the hinder upper
molar, forming a V shape, like that of the penultimate molar. The
profile of the skull is Tapiroid; the frontal and parietal bones are
wide above, so as to overhang the temporal fossz. The jaw is con-
tracted behind the canine teeth, and the expansion of the pre-
maxillary region is rounded. The zygomatic arch widens, so that
the malar bone is carried out laterally far beyond the plane of the
maxillary bone. All traces of sutures are obliterated, and the pos-
terior half of the head is roughened above by shallow pits and
wrinkles like those seen in many Reptiles. The palatal surface
is widest between the posterior incisors. The interspaces between
the incisor teeth are as wide as their roots. The large canine teeth
are well worn on the anterior face, and the molars are well worn by
mastication. Bathmodon is an allied genus, in which the astragalus
is subquadrate, narrower, and wants the internal hook seen in
Coryphodon. At present the skull is unknown, and it is possible
that some species of Coryphodon may belong to this type.

Bathmodon pachypus is the only Coryphodont with the pelvis well
preserved. The wide peduncles of the ilia resemble those of the
Elephant; and if the crest of the ilium of the Camel were more
convex, it would resemble Bathmodon. ‘The peduncle is stouter than
in the Horse, Tapir, or Pig. The limb bones appear to be more
robust than in species of Coryphodon. Metalophodon differs from
Coryphodon in the structure of its molar teeth, though the dental
formula is the same. All the premolars have the single external V
pattern; the first upper molar only has two external Vs, of which
the anterior is represented by a subconical cusp, while the posterior
V is large. The genus is known from two species.

The next suborder, Dinocerata, is especially distinguished from the

472 Reviews—Prof. Edward D. Cope—

Proboscidea by the small size of the cerebral hemispheres, and the
double distal articulation of the astragalus, in which the facets for
the cuboid and navicular bones are nearly equal. There is less
difference between the molar and premolar teeth in this group than
in the Pantodonta. In the upper jaw the crowns of the molars have
crests with a V pattern, and the lower molars consists of a V directed
outward, and a heel. Professor Cope recognizes four genera based
on characters of the mandible; these are named Hobasileus, Lowolo-
phodon, Bathyopsis and Uintatherium. Eobasileus pressicornis and EH.
Jurcatus represent the type in which some of the cervical vertebrze
are flat and short as in Proboscidea. The muzzle is short; the oc-

Loxolophodon cornutus.

Pe)

‘

cipital and parietal crests are remarkably developed, and the propor-
tions of the head somewhat resembled those of Rhinoceros, though
the horns and tusks give it a different aspect. Loxolophodon is one
of those genera concerning which the priority of nomenclature is

Tertiary Vertebrata of the West. 473

disputed, the author claiming to have named it 19th August, 1872,
while he finds no earlier date for the Tinoceras of Marsh than the
following month; but Marsh claims to have published his name on
thesame day. Loaolophodon has a long compressed head with a roof-
shaped muzzle, over which is a bilobed protuberance at the end
of the nasal bone. A second pair of horns stands over the orbits,
each formed externally from the maxillary, and internally from
the nasal bone. Behind this the margin of the temporal fossa rises
in a way that is considered to indicate another horn. Three species,
L. cornutus, L. galeatus and L. spierianus, are distinguished by
characters of the horn-cores.

Loxolophodon cornutus has a narrow cranium four times as long
as its middle width. The diverging horn-cores are in front of the
middle length, each with a triangular base. The frontal bones
descend behind the horns. There is no bony septum between the
anterior nares. The teeth are remarkable for the exposure of their
slender roots, as well as for their small size. The grinding surface
of the first premolar tooth appears to consist of a worn crescent and
an inner tubercle, while the other premolars are transversely arrow-
shaped. All the molars have three roots. This type was similar in
form and proportion to the Elephant, with somewhat shorter stouter
limbs, and a small tail. The neck was a little longer than in Elephants,
but shorter than in the Rhinoceros type. The animal stood almost
six feet high at the rump, while the height at the anterior limb is
estimated at seven feet five inches. The individual from which these
measurements are taken may not, however, have reached its full size.
Teeth indicate it to have been a vegetable feeder. It is remarkable
that the orbits have no distinctive outline, while the eyes were so
overhung by the horns that the view was chiefly lateral, for the
muzzle and cranial crest obstructed the view in front and behind.
This species was found in the bad lands of Wyoming, 8500 feet
above the sea.

Uintatherium has the cervical vertebrae more elongated. This genus
is regarded by the author as identical with that which Professor
Marsh has rendered classical as Dinoceras, though Professor Marsh
separates Dinoceras from it as having three instead of four lower
premolars. Leidy published Uintatherium in August, 1872; Marsh,
Dinoceras, in September, 1872. Three species are here described.
Another genus, Bathyopsis, is founded on a mandible with the three
molar teeth and four premolars constructed on the same pattern.
It differs from Uintatherium and Loxolophodon in the much greater
vertical depth of the inferior expansion of the ramus of the mandible,
along the whole length of which it extends. The inferior molars
are constructed on the plan of those of insectivorous and marsupial
Mammals, so as to suggest that the animals fed on Crustacea, large
Insects, and perhaps thin-shelled Molluscs.

A third suborder of the Amblypoda named Taligrada is believed
to be indicated by a single species of a genus Pantolambda. ‘This
suborder is defined chiefly on the characters of the astragalus, for
while that bone in the Pantodonta has no head, in this type it has a

474 Reviews—Prof. Edward D. Cope—

head distinct from the trochlear and distal articular facets. The
cusps of the upper and lower molars develope into Vs. All the
vertebrae have flat articulations. There is no inter-trochlear ridge
to the humerus; and the femur has a third trochanter. Hxcluding
the characters of the astragalus, there are resemblances to the
Condylarthra in the narrow ilium, and in the molar teeth having but
one internal lobe; but the dentition is especially like that of the
Amblypoda, and there are resemblances to the Pantodonta in the
premaxillary teeth, the short flat cervical vertebrze, and the third
trochanter to the femur; but the characters of the astragalus are
rather like those of the Periptychide and the Proboscidea. In
Pantolambda the brain indicates small nearly smooth hemispheres,
extending with little contraction into a rather large cerebellum,
while the olfactory lobes are produced anteriorly at the extremity of
a rather long isthmus. The dentition would indicate Pantolambda
to be the ancestor of the Coryphodonts. The superior molars are all
triangular from having a single internal cusp. This type of tooth
at the present day is found among Insectivorous and Carnivorous
Marsupials, in the Insectivora, and in the tubercular crowns of some
Carnivora; and among Ungulates it is found in the molars of the
Coryphodonts, and in the last upper molar of the Dinocerata. The
only species is Pantolambda bathmodon, in which the hinder part of
the skull is Opossum-like, and the nasal bones give an obtusely roof-
shaped form to the muzzle.

The Perissodactyla are well represented in the North American
Tertiaries. The group may be described as intermediate in dentition
between the Proboscidea and the lowest Selenodont Artiodactyla.
On dental characters Professor Cope recognizes ten families arranged
into four divisions. First, animals with the anterior crescent of the
upper molars shortened, and not distinguished from the posterior
crescent by an external ridge, with cross-crests to the inferior molars,
and with premolars distinct from the molars. This comprises the
Lophiodontide, in which the toes are 4-8; and the Triplopodide,
in which the toes are 3-3. Secondly, a division in which, while
the exterior crescents of the upper molars, and the cross-crests of
the lower molars, remain as in the first division, while the upper
molars and premolars are alike, and furnished with cross-crests.
Under this type are comprised the Hyracodontidz, in which the
mastoid bone enters into the external wall of the skull; and the
Rhinoceridz, in which the mastoid bone is excluded from the wall
of the skull, by contact of the squamosal bone with the occipital
bone. The third division has the exterior crescentic crests of the
upper molars subequal and distinct, with cross-crests to the inferior
molars. This type comprises the Tapiride, in which the upper
molars and premolars are alike furnished with cross-crests, and with
the toes 4-3. The last division has the nearly equal external
crescentic crests of the upper molars separated by an external
ridge, while the inferior molars are furnished with crescents. First
in this group are placed the families with superior premolars
different from the molars, and with only one internal cusp. The

Tertiary Vertebrata of the West. 475

Chalicotheridz have the toes 4~3, and the Macraucheniide have the
toes 8-3. And secondly come families in which the molars are like
the premolars, but with two internal lobes; and among these the
Menodontidee have the digits 4-4, the Paleeotheriidw have the digits
3-38, while the Equide have the digits 1-1. These families include 46
genera and 192 species. The author remarks that the Lophiodontidee
and Chalicotheride are prevalent in the Eocene; the Rhinoceridee
and Paleeotheriidz characterize the Miocene; while the Tapiride and
Equide are chiefly found in the latest Tertiary epochs. The follow-
ing table exhibits the relations of the families with each other.

Equide
Rhinoceride Paleotheriidee
Hyracodontide
Tapiridee :
Triplopidee Menodontide
|
Lophiodontidee Chalicotheriidee
Hyracotheriine.

The Lophiodontide comprises a large number of species, all of
which, with one exception, are limited to the Eocene rocks. Among
living animals the Tapirs most nearly resemble them. They
range in size from that of a Rabbit to the bulk of anOx. Lophiodon
is limited to Europe; Hyrachyus, Hyracotherium and Pliolophus to
Europe and North America; while Systemodon, Heptodon, Helaletes,
and Colonoceras are only found in North America. All these genera
are classified and defined by dental characters. Systemodon is allied
to Hyracotherium and Pliolophus; but instead of having the wide
diastema behind the canine tooth, seen in Hyracotherium, there is no
interspace at all. The dental formula appears to be the same, and
the differences are in the form and arrangement of the cusps. The
genus is represented by two species.

Hyracotherium is admirably known from six American species ;
it shows three diastemata, behind the third incisor, the canine,
and the first premolar in the upper jaw; and two in the lower
jaw, behind the canine, and the first premolar. The species of
this genus differ in the relative development of the intermediate
tubercles of the upper molars, in the distinctness of the tubercles
of the lower molars, the varying lengths of the diastemata, and
the development of the cingula. The form of the head is very like
Anchitherium, and the cingulum of the upper molar teeth is re-
presented in Anchitherium by a ledge, while the principal bones
of the limbs are much alike in both genera, so that there are some
grounds for suggesting an ancestral relation between them. The
coracoid process of the scapula in Hyracotherium is incurved as
in Coryphodon and Anchitherium, and is larger than in its allies
Triplopus and Hyrachyus. 'The humerus, especially in its proximal
end, has much in common with these genera, and in the simple
groove for the biceps is like Tapirus and Anchitherium. The
carpus includes eight bones, and is more like that of Hyrachyus than

476 Reviews—Prof. Cope—Tertiary Vertebrata of the West.

Triplopus, owing to the second metacarpal having a considerable
contact with the os magnum. The bones of the hind limb have
most resemblance with Hyrachyus ; but the femur of Hyracotherium
has the great trochanter larger, so as to project far above its head.
The third trochanter is large, but not so long as in the Tapir and the
Horse. The species range in size from H. index, which is equal to
the Kit Fox, to H. craspedotum, which is equal to the Coyote. Three
species are found in the Wasatch beds, three in the Wind River beds,
and one in the Bridger beds.

The genus Pliolophus is said to differ from Hyracotherium only
in having two tubercles on the heel of the fourth premolar tooth
instead of one. The genus is intermediate between Hyracotherium
and Lophiotherium. Six species have been defined, including Professor
Owen’s original type, and five of these are North American. The
genus Heptodon is essentially a Lophiodon with seven superior molars:
three species are now described. Hyrachyus has no heel to the last
true molar; its lower canines form a continuous series with the
incisors, but are separated from the premolars by a diastema. The
affinities of the skeleton are, first, with the Rhinoceros type; secondly,
with the Tapirs, and least with the Horses. Equine characters are
seen in the articulation of the lumbar vertebrz, Rhinocerontic charac-
ters in the form of the sternum ; but the affinities are strongest with
Hyracotherium. The carpal articulation of the ulna is not so small
as in Z'riplopus and Anchitherium. Nine species have been recognized ;
three are fully described, and the author points out in detail the
differences between Hyrachyus eximius and Tapirus roulini. Triplopus
is a genus nearly allied to Hyrachyus in its dentition, but appears to
have a third transverse crest in the first true molar, and there is a
difference in the number of digits in the fore foot. The rudimental
character of the fifth metacarpal, which in Hyrachyus is well
developed, and carries a digit, is the ground for making Triplopus
the type of another family. It is regarded as connecting the Lophio-
donts with the Rhinoceroses; but the structure of the true molars
and the character of the feet place it between those families. Only
one species is known with certainty.

A synopsis is given of the generic characters of the Rhinocerida,
based on the number of digits, the dentition and the conditions of
the skull connected with the development of horns. The Tapiride
is in the same way briefly defined, but no species of either group is
described.

The Chalicotheriide is a group of eight genera. The symmetrical
external Vs of the upper molars and the double Vs of the inferior
molars distinguish them from the Lophiodontide; but they are not
so clearly defined from the Menodontide. Among its genera, Pachy-
nolophus and Chalicotherium are found in Europe, Nestoritherium in
Asia, while North America yields Ectocion, Leurocephalus, Palco-
syops, Lymnohyus and Lambdotherium, all of which are defined by
dental characters. Zetocion is only known from the teeth; Palgo-
syops differs from Palgotherium in the isolation of the internal cones
of the upper molars from the external longitudinal crescentic crests,

Reports and Proceedings—British Association. 477

and in having but one inner tubercle instead of two on the last three
premolars. The molar dentition approaches towards Menodus. The
pelvis was more Paleotheroid than Tapiroid. This genus, which is
limited to the Eocene, is illustrated by descriptions of four species.
Limnohyus differs from the type last mentioned in having two conical
tubercles instead of one on the inner series in the last upper molar.
Two species are described. Zambdotherium is only known from its
dentition; and the author remarks that if the ridges which are
rudimented in the molars of Hyracotherium were developed, and the
external cusps of the superior molars flattened externally, the result
would be the dentition of Zambdotherium. Three species are described.
Brief notices follow, without description of species, of the genera
contained in the Macraucheniide, Menodontide, Paleeotheriidee and
Hquidee.

The Perissodactyla in the Hocene rocks of the Western Territories
are thus seen to exhibit many and varied types, but the Artiodactyla
are scantily developed in the Eocene period. Only two or perhaps
three genera of Hogs have come under Professor Cope’s notice, and
Pantolestes is the only type described. The tarsal characters are in
general similar to those of Dicobune, but this genus differs in having
but one inner tubercle to the upper molars and one external tubercle
to the upper premolars, and differs from the Anoplotheres in the
presence of external digits. Seven species are defined and described.
This concludes the account of about 250 species of Eocene Vertebrata,

though supplements include descriptions of a few Fishes, Reptiles,
' Birds, and Mammals, which were received too late to be comprised
in the body of the work. A notice of the Miocene fauna from the
White River and John Day beds must be reserved for another
notice, after which it may be convenient to discuss the scientific
results of the author’s work. H. G. SEELEY.

aE @) ee eS AN) | aes @ @ sage ING Se

—S

British ASSsocIATION FOR THE ADVANCEMENT OF SCIENCE.
Firry-stxtH Merxrrine, Birmineuam, 1886.

Srorion C.—GErOoLoGy.

President :—Professor T. G. Bonney, D.Sc., LL.D., F.R.S., F.8.A., F.G.S.
Vice-Presidents :—Professor C. Larpwortn, LL.D., F.G.S8.; H. Woopwarp,
LL.D., F.R.S., F.G.S.; Rev. H. W. Crossxey, LL.D.; Sir Junius Von
Haast, K.C.M.G., D.Se., F.R.S.; Prof. E. Huzz, LL.D., F.R.S.;
W. Maruews, M.A., F.G.S.; Dr. A. R. Senwyn, C.M.G., F.R.S.
Secretaries :—W. Jerome Harrison, F.G.S.; J. J. H. Tratn, M.A., F.G.S.;
W. Torrey, F.G.S. (Recorder); W. W. Warts, B.A., F.G.S.
Titles of Papers read September 2nd to 8th, 1886.
Address by the President.
Prof. C. Lapworth.—Geology of the Birmingham District.
W. J. Harrison.—On the Discovery of Rocks of Cambrian Age at
Dosthill, in Warwickshire.
Prof. C. Lapworth.—The Cambrian Rocks of the Midlands.
W. ZH. Waller.—-On the Petrography of the Volcanic and associated
Rocks of Nuneaton.

478 Reports and Proceedings—British Association.

A. Strahan.—On the Rocks surrounding the Warwickshire Coal
Field, and on the base of the Coal-Measures. With an Appendix
on the Igneous Rocks of the Neighbourhood, by F. Rutley.

W. Matthews.—On the Halesowen Coal Boring.

F. G. Meacham and H. Insley.—On the Thick Coal and the Trias
north of Birmingham, and on the old South Staffordshire Coal
Field.

Dr. H. W. Crosskey.—Report on the Erratic Blocks of England and
Wales.

Dr. H. W. Crosskey.—On the Glacial Formations of the Birmingham
District.

Rev. W. Tuckwell.—On the Glacial Erratics of Warwickshire and
Leicestershire.

A. T. Evans.—The Fossiliferous Bunter Pebbles contained in the
Drift of Moseley, ete.

Prof. W. Benton—On the Surface Subsidences caused by Coal
Mining.

Dr. H. Woodward and R. Etheridge.—To exhibit some Organisms
met with in the Clay-Ironstone Nodules of the Coal-Measures of
the Neighbourhood of Dudley.

S. A. Adamson.—Notes on the Discovery of a large Fossil Tree in
the Lower Coal Measures at Clayton, near Bradford.

Rev. P. B. Brodie.-—On the Discovery of Fossil Fish in the New
Red Sandstone (Upper Keuper) in Warwickshire.

Rev. P. B. Brodie.—On the Range, Extent, and Fossils of the Rheetic
Formation in Warwickshire.

W. J. Harrison.—On a Deep Boring for Water in the New Red
Marls (Keuper Marls) near Birmingham.

Dr. W. T. Blanford.—Notes on a Smoothed and Striated Boulder
from a Pretertiary Deposit in the Punjab Salt Range.

A. B. Wynne.—On a Facetted and Striated Pebble from, the Olive
Conglomerate of Chil Hill, in the Salt Range, Punjab.

Prof. E. Hull.—Notes on the Problems now being investigated by
the Officers of the Geological Survey in the North of Ireland,
chiefly in Co. Donegal.

Dr. C. Callaway.—Notes on the Crystalline Schists of Donegal.

Prof. C. Lapworth.—The Ordovician System in Shropshire.

Prof. T. McK. Hughes.—On the Silurian Rocks of North Wales.

Prof. T. McK. Hughes.—Notes on some Sections in the Arenig Series
of North Wales and the Lake District.

J. EH. Marr.—On the Lower Paleeozoic Rocks, near Settle.

A. J. Jukes-Browne.—Note on a Bed of Red Chalk in the Lower
Chalk of Suffolk.

Dr. C. Le Neve Foster.—Manganese Mining in Merionethshire.

. W. Davis.—On the Exploration of Raygill Fissure, Yorkshire.

. Beale.—On the Dolerites of Rowley Regis.

J. Woodward.—On the Mineral District of Western Shropshire.

D. Adams.—On the Anorthosite Rocks of Canada.

‘of. H. Carvill Lewis.—On a Diamond-bearing Peridotite, and on

the Genesis of the Diamond.

HOaQS

s

Papers read in Section C.— Geology. 479

J. J. H. Teall.—On the Metamorphosis of the Lizard Gabbros.

Prof. J. F. Blake.—Introduction to the Monian System of Rocks.

Prof. J. F. Blake.-—On the Igneous Rocks of Llyn Padarn, Yr Hifl
and Boduan.

J. H. Player.—On an accurate and rapid method of estimating the
Silica in Igneous Rocks.

J. Hopkinson.—On a new form of Clinometer.

H. B. Stocks.—On Concretions.

W. Pengelly.—On a Scrobicularia Bed, containing Human Bones, at
Newton Abbot, Devonshire.

W. W. Watis.—The Corndon Laccolites.

Prof. T. Rupert Jones.—Report on the Fossil Phyllopoda of the
Palzozoic Rocks.

HE. T. Hardman.—On the Discovery of Diprotodon Australis in
Tropical Western Australia (Kimberley District).

Prof. J. W. Sollas.—On the past and present Bathymetrical Distribu-
tion of the Lithistida.

C. E. De Rance.—Report on the Circulation of Underground Waters.

Prof. G. A. Lebour.—On the Stratigraphical Position of the Salt
Measures of South Durham.

G. H. Morton.—On the Carboniferous Limestones of the North of
Flintshire.

Hugh Miller.—On the Classification of the Carboniferous Limestone
series—Northumbrian type.

W. A. E. Ussher. —The Culm Measures of Devonshire.

A. RK. Hunt.—Denudation and Deposition by the Agency of Waves
experimentally considered.

C. E. De Rance and W. Topley.—Report on the Erosion of the Sea-
Coasts of England and Wales.

Prof. W. I. Macadam and J. S. Grant-Wilson.—On Deposits of
Diatomite in Skye.

Dr. H. Hicks.—Reports on the Exploration of the Tremeirchion
Caves, North Wales.

Prof. T. McK. Hughes.—On the Pleistocene Deposits of the Vale of
Clwyd.

Prof. H. Carvill Lewis.—Comparative Studies upon the Glaciation
of North America, Great Britain, and Ireland.

Henry Johnson.—On the Extension and Probable Duration of the
South Staffordshire Coal Field.

Sir J. W. Dawson.—On the Relations of the Geology of the Arctic
and Atlantic Basins.

Dr. G. M. Dawson.—On the Rocky Mountains, with special reference
to that part of the Range between the 49th Parallel and the
Head-waters of the Red Deer River.

F. D. Adams.—On the Coal-bearing Rocks of Canada.

Prof. T. Rupert Jones.—On the Coal Deposits of South Africa.

Prof. W. Boyd Dawkins.—On the Kerosine Shale of Mount Victoria,
New South Wales.

Sir J. Von Haast.—On the Character and Age of the New Zealand
Coal Fields.

480 Reports and Proceedings—British Association.

E. W. Bucke.—On the Geysers of the Rotorua District, N. Island of
New Zealand. |

Prof. J. W. Judd,—Notes to accompany a Series of Photographs,
prepared by J. Martin, Esq., to illustrate the Scene of the recent
Volcanic Eruption in New Zealand.

E. T. Hardman.—On the Geology of the newly-discovered Goldfields
of Western Australia (Kimberley District).

ftichard Meade.—Statistics of the Production and Value of Coal
raised within the British Empire.

W. A. E. Ussher.—The Relations of the Middle and Lower Devonian
in West Somerset.

W. Whitaker.—Supplementary Note on two Deep Borings in Kent.

Prof. W. Boyd Dawkins.—On the Westward Extension of the Coal-
measures in South-Hastern England.

J. S. Gardner.—Report on the Fossil Plants of the Tertiary and
Secondary Beds of the United Kingdom.

Sir J. W. Dawson.—On Canadian Examples of supposed Fossil Algee.

Prof. T. McK. Hughes.—On Bilobites.

Prof. W. C. Williamson.—On recent Researches amongst the Carbon-
iferous Plants of Halifax.

W. Topley.—Notes on the recent Barthquake in the United States ;
including a telegraphic despatch from Major Powell, Director of
the United States Geological Survey.

Prof. John Milne.—Report on the Earthquake and Volcanic Pheno-
mena of Japan.

Dr. H. J. Johnston-Lavis——Report on the Volcanic Phenomena of
Vesuvius.

Rev. A. Irving.—On the Heat of the Earth as influenced by Conduc-
tion and Pressure.

Rev. A. Irving.—A Contribution to the Discussion of Metamorphism
in Rocks.

J. Gunn.—On the Influence of the Axial Rotation of the Earth on
the Interior of its Crust.

List of Papers bearing upon Geology read in other Sections.’
Section A.—MatTHEmaticanL anD Puystcat Scrmncg.
Address by the President, Prof. G. H. Darwin.— (Geological Time,
etc.)
John Hopkinson.—An Improved Form of Clinometer.

Section B.—CuHEmiIcAL SCIENCE.
Dr. H. R. Mill.—Chemistry of Hstuary Water.
Dr. O. W. Huntingdon.—The Crystalline Structure of Iron Meteorites.

Section D.—Bro1oey.
Address by the President, W. Carruthers.—(Pliocene Plants, etc.)

Sxotion H.—Anruropotoey.
Dr. Henry Hicks. —Ou Evidence of Pre-Glacial Man in North Wales.
Prof. W. Boyd Dawkins.—On the Recent Exploration of Gop Cairn
and Cave.
Charles VV. Bell.—Remains of Pre-historic Man in Manitoba.

»

af

A" bree

aie

scot. Mac., 1886. Decape III., Vor. IIl., Pu. XIII.

Waterlow & Sons Linvited.

AUGEN-GABBRO (NATURAL SIZE) KARAKCLEWS, LIZARD, CORNWALL,

THE

GEOLOGICAL MAGAZINE.

NEW SERIES. DECADE III. VOL. Ill.
No. XI—NOVEMBER, 1886.

OG EN ASE Ary Lee AEE Ss

Seen
I.—Tur Meramorpnosis oF THE Lizarp Gassros.!
By J. J. H. Teatt, M.A., F.G.S,

(PLATE XIII.)

F we take a general view of the present position of geological
science, we are struck by the fact that, although there is sub-
stantial agreement amongst geologists on matters relating to the
origin of the rocks usually designated as aqueous and igneous, the
greatest diversity of opinion prevails with regard to the circum-
stances under which the so-called metamorphic rocks have been
produced. Every fragment of evidence calculated to throw light
on the origin of these rocks, therefore, deserves the most careful
consideration. Of recent years special attention has been directed
to the effects of mechanical energy in modifying the mineralogical
and structural characters of rocks originally formed by aqueous and
igneous agencies ; and a suspicion has been aroused that it is in this
direction that we must look for a solution of many of the problems
connected with the origin of the crystalline schists. A visit to the
Lizard Peninsula of Cornwall during the present summer has con-
vinced me of the immense importance of this view so far as that
district is concerned. That portion of the peninsula which lies
south of a line drawn from Porthalla on the east to Polurrian Cove
on the west is formed partly of igneous rocks—such as gabbro, green-
stone, serpentine, and granite—and partly of crystalline schists. The
igneous rocks, in certain places, become foliated and schistose and
sometimes show a definite banding due to a variation in the relative
proportions of the different constituents. In other words they pre-
sent characters which.are usually regarded as distinctive of the
crystalline schists. There is, moreover, evidence to show that these
characters are mainly the result of a yielding to earth-pressure sub-
sequent to the consolidation of the original rock. At the present
moment, having just returned from the district, I am unable to treat
the subject from a general point of view with any prospect of success;
but it has occurred to me that some details with regard to one of the

rocks may not be without interest to members of the Association.
The gabbros of the Lizard have been noticed by many previous
writers, including Dr. Boase,’ Mr. Majendie,’ Sir Henry de la Beche,*

1 Paper communicated to Section C of the British Association.
2 Trans. Geol. Society of Cornwall, vol. iv. p. 330.

3 Ibid. vol, i. p. 36.
4 Report on the Geology of Devon and Cornwall, 1839.

DECADE III.—VOL. IlI,.—NO. XI, 31

482 J. J. Harris Teati—The Lizard Gabbros.

and Prof. Bonney.’ Their mineralogical composition, geographical
distribution, and structural characters were described by the older
observers. Prof. Bonney added many facts on these points and
gave in addition a description of their microscopic structures. As
I wish on the present occasion to refer to them for the purpose
of establishing a definite proposition with regard to the origin of
certain structures which they possess, I must ask permission to
recapitulate the facts, and at the same time to add one or two from
my own observation.

Gabbro occupies an area of six or seven square miles in the neigh-
bourhood of St. Keverne, and forms the elevated tract of land known
as Crousa Down. This great mass comes down to the sea and forms
the coast-line from Coverack to Manacle Point. It is traversed by
veins and dykes of a fine-grained rock generally known as “ green-
stone.” This greenstone is essentially composed of plagioclase and
hornblende, the latter mineral often belonging to the uralitic and
actinolitic varieties. It is, as Prof. Bonney has pointed out, an
altered plagioclase-augite rock, and must be classed with the
epidiorites (Gumbel) of the Fichtelgebirge and the Hartz. In some
instances the felspars give lath-shaped sections which penetrate the
fibrous aggregates of secondary hornblende in such a way as to
prove conclusively that the parent rock must have been an ophitic
dolerite. :

The amount of this “greenstone” or “epidiorite ” associated with
the gabbro increases towards the north until it exceeds that of the
latter rock. Although the junctions of the gabbro and the green-
stone are perfectly sharp, it is impossible to represent the distribution
of the two varieties on a small scale map in consequence of the way
in which they alternate with each other. Manacle Point, which is
represented as greenstone on the Survey Map, consists for the most
part of gabbro in which veins and dykes of greenstone are very
common.

The northern limit of the gabbro-greenstone area above referred

to occurs in the neighbourhood of Porthoustock. 'The adjacent rock

is hornblende-schist, but the actual junction, which is probably a
fault, is concealed by a small shingle beach. The southern limit
of this mass comes out on the sea-shore by the small village of
Coverack. The geology of this locality has been fully described by
Prof. Bonney, to whose paper reference must be made for details.
The only point that need be mentioned here is that the normal gabbro
is seen to be intrusive in serpentine and also in a rock, intimately
associated with the serpentine, which consisted originally of a basic

felspar and olivine and which appears to be identical with the trocto-

lite or forellenstein of Neurode in Silesia.

South of Coverack the greater part of the district is occupied by
serpentine in which veins and dykes of gabbro frequently occur.
The mass of gabbro which ranks next in importance to that of Crousa
Down is exposed on the sea-coast west of Lankidden Cove. It forms
the headland of Karakclews, and may be followed along the coast

1 Quart. Journ, Geol. Soc., vol. xxxiii. 1877, p. 884.

—— —-

J.J. Harris Teali—The Lizard Gabbros. 483

for a distance of about a quarter of a mile. A mass of precisely
similar gabbro occurs inland at Gwinter. The two portions are
doubtless continuous, as represented on the geological map; and if so,
they form a dyke-like mass running inland in a N.W. direction.
The Karakclews gabbro is bounded on both sides by serpentine into
which it was intruded. Marked signs of disturbance occur near
both junctions and throughout the mass; but, notwithstanding this,
veins of gabbro may occasionally be seen running out from the
larger mass into the surrounding rock.

Another considerable exposure of gabbro occurs on the shore
north of Pen Voose,! near Landewednack. It is bounded on the
north by serpentine with gabbro veins, and on the south by a
remarkable group of rocks which Prof. Bonney terms “the granulitic
series.” The gabbro is here traversed by veins of granite and mica-
diorite which will doubtless repay careful examination, but which
need not be further referred to on the present occasion. ;

The principal mineralogical constituents of the Lizard gabbros are
plagioclase, augite or diallage, hornblende and saussurite. Olivine
is present in certain varieties, but does not appear to have been very
widely distributed in these rocks. In the least altered rocks the
plagioclase occurs in the form of grains of tolerably uniform size and
having nearly equal dimensions in the different directions. The
grains show broad lamellar twinning, and not seldom two sets of
lamella are seen crossing each other at right angles. This is the
feature which is usually regarded as indicating simultaneous twinning
on the albite and pericline types. The extinction angles in thin
sections of the rock show that the felspar belongs to the labradorite-
anorthite series, but I have not as yet been able to make a more pre-
cise determination. In the more or less altered gabbros we see
various stages of the replacement of felspar by white or cream-
coloured saussurite. The first stage consists in the development of
white spots in the glassy felspar substance. These spots appear
snow-white under the microscope by reflected light, and opaque or
brown by transmitted light. They never exhibit any definite form
or cleavages. By the increase in the number and size of these white
spots and by other changes the felspar gradually passes into saus-
surite. This substance sometimes occurs in masses of considerable
size, and it is then remarkable for its toughness and hardness. Its
specific gravity is about 3:1. Microscopic examination shows that
it is an aggregate and not a simple mineral, but it is by no means
easy to determine the precise character of the different constituents.
Cathrein’s* investigations led him to the conclusion that saussurite is
an aggregate of zoisite or epidote and felspar, usually albite; with
variable quantities of actinolite and tremolite as accessory constituents.

1 There is some confusion about the naming of this locality. The small bay to
the north of which the gabbro is exposed is named the Balk on the one-inch map and
Parn Voose on the twenty-five inch map. The inhabitants of this district say\that
this bay is called Pen Voose and that the place where the life-boat is kept, otherwise
known as Church Cove, is Parn Voose. As the maps do not agree, I have followed
the inhabitants,

2 Ueber Saussurit, Zeit. f. Krystallographie, vol. vii. p. 234,

484 J. J. Harris Teall—The Lizard:Gabbros.

IT have not as yet been able to find a saussurite in the Lizard
District answering to Cathrein’s description.’

The felspars of certain gabbros in which the development of
saussurite has not taken place at all, or has only occurred to a very
limited extent, often give evidence of having been affected by pro-
found mechanical disturbances. The twin lamelle are frequently
bent and, when the limit of elasticity has been exceeded, the crystal
grains have been fractured. The extinction is not sharp and definite.
Dark shadows sweep across the sections as the stage is rotated. In
slides exhibiting these characters large felspars are often seen to
break up, in certain places, into aggregates of minute, colourless, and
for the most part simple grains. Such aggregates must certainly
be regarded as of secondary origin, for they are entirely unknown in
the unaltered felspar-diallage gabbros and frequently contain needles
of actinolite, a mineral undoubtedly of secondary origin. They
correspond to the felspar-mosaic of Lossen.?

The pyroxene in the least altered rocks is a pale green diopside.
In microscopic sections it is almost colourless. Cross sections show
an optic axis in convergent polarized light and frequently the two
pinacoidal as well as the two prismatic cleavages. Longitudinal
sections give a maximum extinction of about 40°. The mineral is
therefore a monoclinic pyroxene. In addition to the cleavages above
mentioned, we find occasionally incipient stages of diallagic lamina-
tion. This lamination is not as a rule persistent throughout the
crystal, but limited to the neighbourhood of cracks. In the ordinary
gabbros the pyroxene is a true diallage with a decided bronzy lustre
on the planes of easy separation, which planes run parallel with the
orthopinacoid. In some of the coarse-grained rocks the diallage
crystals often measure two or three inches across.

The change of pyroxene into hornblende has been described and
illustrated by Prof. Bonney. It is a common feature in the Lizard
gabbros and often accompanies the change of felspar to saussurite.
Many different varieties of secondary hornblende may be observed
depending on variations in colour and habit. Sometimes the horn-
blende occurs in the form of homogeneous crystalline grains with
strongly marked cleavages. This variety may be termed compact
hornblende. At other times the hornblende is distinctly fibrous,
and at others it occurs in the form of needles. The two latter
varieties are generally termed uralitic and actinolitic respectively.
Actinolitic hornblende frequently forms radiating fringes round the

1 A saussurite composed of zoisite and albite occurs in Sangomore Bay near
Durness, Sutherlandshire. Under the microscope this is seen to consist of minute
colourless prisms embedded in a colourless felspathic matrix. The prisms possess a
high refractive index, weak double refraction, cross-jointing at intervals, and give
straight extinction. Small fragments of the felspar with which they are associated
may occasionally be obtained and when tested in the Bunsen’s burner give the flame
colouration and fusibility of albite. In the mass this saussurite is white or a very
pale pink. It contains hornblende and is associated with a felspathic gabbro in
which the diallage has been converted into uralite and actinolite.

2 Studien an metamorphischen Eruptiv- und Sedimentgesteinen, Jahrbuch d, k.
preuss. geol. Landesanstalt fiir 1883 und 1884.

J. J. Harris Teall—The Lizard Gabbros. 485

uralitic variety or round a crystal of diallage partially changed to
uralite. The hornblende may be either green, brown, or colourless.
One of the green varieties is remarkably brilliant and of that tint
which led to the introduction of the term smaragdite. The gradual
replacement of diallage by hornblende is a most striking feature in
the Lizard gabbros. The two minerals bear an inverse relation
to each other so far as distribution is ‘concerned. As the one
increases, the other diminishes.

Olivine does not appear to have been abundant or widely distri-
buted in the normal gabbros. It occurs sparingly in an unaltered
rock from Coverack, and in this case is perfectly colourless in thin
sections and traversed by irregular cracks, along which magnetite
has been formed. In some of the more altered gabbros it is repre-
sented by serpentinous pseudomorphs.

The minerals above referred to occur in very different proportions
in the different rocks, and in different portions of the same rock-mass.
We thus have an endless number of mineralogical varieties. The
principal variations are due to the gradual replacement of felspar by
saussurite and of diallage by hornblende. The two extreme types
may therefore be designated felspar-diallage gabbro, and saussurite-
hornblende gabbro ; the former representing the original rock and
the latter the extreme of mineralogical metamorphism. Between
these two extreme types there are innumerable intermediate varieties.
As a rule the change in one mineral is accompanied by a change in
the other; but this is not invariably the case. We may thus have
felspar-hornblende gabbros and saussurite-diallage gabbros. If we
wish to indicate the mineralogical character of any intermediate
form, we can do so by using a compound term made up of the names
of the substances occurring as constituents. The number of actual
varieties present is the number of possible combinations of the four
principal constituents taken two, three, and four together. The
introduction of olivine gives rise to other varieties, but, as already
stated, I am inclined to think that this mineral was absent from
considerable masses of the original rock.

If we eliminate hornblende and saussurite, both of which are un-
doubtedly secondary minerals, then the original felspar-bearing rocks
of the gabbro-type occurring in the Lizard Peninsula must have
comprised plagioclase-augite rocks, plagioclase-augite-olivine rocks,
and plagioclase-olivine rocks. By the gradual disappearance of the
felspar these rocks passed through the picrites into the peridotites,
which are now represented by the serpentines. Felspar-bearing
serpentines occur at the Rill Head near Kynance. Looking at the
Lizard district as a whole, we are struck with many points of resem-
blance between it and the Tertiary volcanic district of the West of
Scotland described by Prof. Judd.

We have now to consider the structural characteristics of the
Lizard gabbros. In the first place, we notice varieties depending
on variations in the sizes of the individual constituents. Such
variations are characteristic of all masses of gabbro. In the coarsest
varieties the individual crystalline grains often measure as much as

486 J. J. Harris Teall—The Lisard Gabbros.

two or three inches across. These extremely coarse varieties are
often distributed with considerable irregularity through large masses
of the finer-grained rocks; not seldom, however, they occur as
narrow veins and dykes in the serpentine. The dominant gabbro is
a rock which would simply be described as coarsely crystalline.
Fine-grained varieties are not known. The junction with greenstone
or epidiorite is always sharp, and there is no evidence in the Lizard
district, so far as I know, of a gradual passage from gabbro into
dolerite and basalt. The ‘greenstones” are undoubtedly altered
dolerites, some of which were ophitic, but their junctions with the
gabbro are, as already stated, always sharp.

The mutual relations of the individual constituents in the un-
altered gabbros are those of typical granitic rocks; in other words,
no single mineral appears to have possessed any special advantage
over any other so far as the conditions favourable to the development
of crystalline form are concerned. Each mineral occurs in the form
of crystalline grains.

In addition to variations of structure depending on variations in
the sizes of the individual constituents, there are others, of a most
important character, dependent on the mode of arrangement of these
constituents in the rock-mass. From this point of view the gabbros
of the Lizard may be divided into two groups: (1) the massive, and
(2) the foliated gabbros. These two varieties are not, however,
separated from each other by any hard and fast line. In the massive
gabbros the individual constituents are not arranged in any definite
manner; in the foliated gabbros a parallel structure is more or less
pronounced. It is convenient in speaking of the foliated gabbros to
recognize two principal types which may be designated by the terms
flaser-gabbro and gabbro-schist. In the flaser-gabbro the parallel
structure, though distinct, is not accompanied by any marked fissility.
The constituents are white saussurite and dark aggregates of
diallage and hornblende. These constituents are more or less
lenticular in form and the flat surfaces of the lenticles lie parallel to
each other, thus producing the foliated structure. The gabbro-
schist is a rock of finer grain, with a strongly-marked schistosity.
It can be broken into flat slabs like a hornblende schist. Indeed the
rock may sometimes be called hornblende-schist without doing any
violence to the latter term. Although it is convenient to use the
expressions flaser-gabbro and gabbro-schist, it must not be supposed
that there is any hard and fast line between the rocks designated by
these terms. They shade into each other by the most insensible
gradations. One very interesting structural variety which is, in
some respects, intermediate between flaser-gabbro and gabbro-schist,
may be termed augen-gabbro. In this variety the streaks which
define the schistosity sweep round “eyes” of diallage, which thus
remind one strongly of the “eyes” of felspar in augen-gneiss. (See
Plate XIII.)

We have now to consider the distribution of the different
structural varieties. The gabbro to the north of Coverack is on the
whole massive; nevertheless here and there foliation makes its

J. J. Harris Teall—The Lizard Gabbros. 487

appearance. In the neighbourhood of the village the veins and
dykes of gabbro are often foliated, and every transition may be
observed from massive gabbro to gabbro-schist. At Karakclews
Headland foliation has been developed in a most striking manner,
and affects, with a few local exceptions, the entire mass, which is
more than a hundred yards in width. The general strike of the
foliation is approximately N.W. and 8.E., but there is no absolute
constancy in the direction; slight deviations occur sometimes on
the one side and sometimes on the other. One important feature in.
the Karakclews mass is the distinctly banded character of certain
portions, particularly those near the southern junction with the
serpentine. Light and dark bands several inches in thickness
alternate with each other, and with the ordinary flaser- and augen-
’ gabbro, so that the mass asa whole simulates a stratified series. The
small dykes of gabbro in the serpentine near. Karakclews are often
foliated, and not seldom one may see the transition from massive
gabbro to gabbro-schist taking place in the space of a few inches.

Another locality where foliation is well developed is north of
Pen YVoose near Landewednack. The main mass of gabbro is
separated from serpentine and other rocks on the north by a well-
marked fault-plane. In the immediate neighbourhood of this plane
the gabbro is foliated, and passes into a fine gabbro-schist. Folia-
tion also makes its appearance in the main mass, which is here
intimately veined with mica-diorite and granite. It is frequently
developed near the junction of the gabbro with one of the other
rocks. Jn the small bay known as Pen Voose alenticular mass of
saussurite-hornblende gabbro, measuring about five feet in the
longest diameter, occurs in Prof. Bonney’s granulitic series. This is
evidently not an intrusive tongue, but a lenticular mass which owes
its form and position to earth-movements acting after the consolida-
tion of the rock. It is conspicuously foliated parallel with the
junction surfaces.

It is instructive to compare the mineralogical with the structural
varieties. TF oliation is absent from the felspar-diallage rocks. As
the foliation becomes more and more pronounced, the diallage is
gradually replaced by hornblende, and the felspar undergoes a change
resulting for the most part in the development of saussuritic aggre-
gates. In the most perfect gabbro-schist the diallage has entirely or
almost entirely disappeared, and its place has been taken by horn-
blende. It must not, however, be supposed that the mineralogical
change is invariably accompanied by the development of foliation.
Many of the saussurite-hornblende gabbros are as massive as the
original rock.. In a paper on the “‘ Metamorphosis of Dolerite into
Hornblende-schist ”’ I have pointed out similar relations between
structural and mineralogical characters in the case of the Scourie
dykes. A molecular rearrangement may take place in a massive
rock without the development of foliation; but there is no reason
to believe that foliation of the kind referred to in this communica-
tion can take place without molecular rearrangement.

The principal question which now remains for consideration is the

488 J. J. Harris Teall—The Lizard Gabbros.

origin of this foliation. Is it an original or secondary structure?
That it is due to a differential movement in the mass after the separa-
tion of the individual constituents will I think be admitted on all
hands. The only question that can arise is whether this movement
was in any way connected with the intrusion of the rock. The facts
appear to me to point very decidedly to.the conclusion that it is a
secondary structure due to earth-movements acting upon the solid
rock. That the Lizard district has been profoundly affected by earth-
movements is apparent on every hand. The rocks have been folded,
faulted, crumpled, twisted, and in some places brecciated by the
intense pressures that have acted upon them. The evidences of
mechanical disturbance are not limited to any one variety of rock or
to any one district. They abound in every portion of the district,
though their effects are more pronounced in certain localities than in
others. If we attempt-to determine the precise nature of the earth-
movement, we are met with considerable difficulty on account of the
superposition of the effects of distinct movements. The earlier
movement, and the one which I suspect produced the greater part of
the foliation in the gabbros, appears to have acted so as to produce
a strike about N.W. and S.H. or N.N.W. and 8.S.H. This earlier
movement was, however, certainly followed by one producing faults
which run approximately in an HE. and W. direction. The latter
direction agrees with one of the great post-Carboniferous disturb-
ances, and the faults which run in this direction probably belong to
those disturbances. That the two sets of earth-movements above
referred to are the only ones that have acted upon the district I am
by no means prepared to say; but that these two have acted is shown
by facts which may be observed at Porthalla, George Cove and
Kynance.

That the foliation in the gabbros is one of the results of the
pressure- or regional-metamorphism which has operated upon the
district, is rendered at once probable when we compare the Lizard
gabbros with those of the West of Scotland. The latter consist
mainly of felspar-diallage rocks, and are not foliated ; the former are
largely composed of saussuritic and hornblendic rocks, and are often
conspicuously, foliated. The Lizard district has been profoundly
affected by earth-movements, whereas the Tertiary volcanic district
of the West of Scotland has not been so affected.

This argument is in itself not conclusive, but it becomes greatly
strengthened when we consider the distribution of gabbros of the
Lizard type. They have been described by Dr. Reusch’ from the
Bergen Peninsula, by Prof. Lehmann? from the granulitic region of
Saxony, and by Mr. Hatch*® from the Tyrol. Hach one of these
districts gives independent evidence of having been subjected to
pressure-metamorphism. Perhaps the most convincing proof that
the structure is the result of movement after the consolidation of the

1 Die Fossilien fiihrenden krystallinischen Schiefer yon Bergen in Norwegen,
Leipzig, 1883.

” Die Entstehung der altkrystallinischen Schiefergesteinen, Bonn, 1884, p. 190.

3 Tsch. Min. Mitth, Band VII. (1885), p. 75.

Prof. T. McKenny Hughes—The Ffynon Beuno Caves. 489

rock is, however, furnished by its relation to fault-planes. A rock
must necessarily be solid before it can be faulted. Now, we find
at Pen Voose near Landewednack, that massive gabbro passes over
into gabbro-schist at a fault-plane, and that the foliation in the
gabbro is such as would be produced by a shearing motion parallel
with the fault-plane. Taking all the facts into consideration, we
appear to be justified in concluding that the foliation in the Lizard
gabbros is the result of pressure- or regional-metamorphism. It
seems also probable that the replacement of felspar and diallage by
saussurite and hornblende has been largely determined by the same
agency.
DESCRIPTION OF PLATE XIII.

The Plate represents the appearance of a polished slab of the augen-gabbro of Karak-
clews. The ‘‘eyes”’ are formed of diallage. The dark bands are formed mainly of
green hornblende; the white bands, of the aggregate generally known as saussurite.
The white spots seen in certain parts of the Plate represent an undetermined mineral
which is almost constantly present in the Lizard gabbros. It appears in the glassy
felspar of the comparatively unaltered rocks, and increases in amount as the felspar
passes into the condition of saussurite. There is much greater detail in the dark

bands than is represented in the Plate. The block is traversed by narrow veins which
cut the planes of foliation at angles of about 15°.

I.—On tHe Frynon Bruno Caves.
By Prof. T. McKenny Hucuss, M.A., F.G.S.

UCH interest has been recently aroused in the exploration of
the caves of the Vale of Clwyd, partly by the enthusiasm of
the principal promoter: of the investigation, Dr. Hicks, but chiefly
owing to the inferences he has drawn from the observations made.
When reading the Report of the British Association Committee for
the Exploration, of which he was Secretary, he assumed the entire
responsibility of those theoretical deductions. In these, however,
he was supported by all the speakers who followed him on the
subject, including the other members of the Committee excepting
myself. He had previously anticipated the report by the announce-
ment in Nature of his discovery of Pre-Glacial Man in the Vale
of Clwyd. I therefore ask leave briefly to state my reasons for
differing from his conclusions.

First, I recognize in the Vale of Clwyd four drifts which must be
distinguished in this inquiry.

1. The Arenig Drift, which contains fragments from the W. and 8.
only, and which is the only true glacial deposit in the Vale of Clwyd,
as there is no evidence of any glacier having ever come down the
Vale.

2. The Clwydian Drift.—(A) a marine deposit due to the sub-
mergence which followed the age of extreme glaciation and contain-
ing, in addition to the re-sorted débris of the older drift, flint and
fragments of granite and other north-country rocks. (B) the still
further winnowed débris belonging to the age of emergence.

I am not very clear about the possibility of often distinguishing

490 Prof. T. McKenny Hughes—The Ffynon Beuno Caves.

between A and B; but there is a Bead deal of evidence in some
localities.

3. The almost universal covering of re-sorted drifts and rain-wash,
the results of subaerial denudation since the submergence.

If the mouth of a cave is said to be blocked by drift, we must be
careful to enquire what drift, before we take it as a measure of the
age of the cave-deposits.

There are some other points also which must be attended to. We
must distinguish between the age of the caves and that of the cave-
deposits. So many changes and modifications go on in some cases
that their history and that of their contents cannot always be read,
even during the most careful excavation.

There are in the Vale of Clwyd many caves representing subter-
ranean channels through which the water running off the Silurian
hills around, drops into fissures on reaching the Mountain Limestone,
and finds its way to lower ground. Some of these caves are being
formed now, and in some of them mud still settles after floods.
Bones and stones still get washed down into the fissures which feed
the cave, and these fissures are often enlarged or new ones opened
where the moisture can get access to the rock. So of course the
wash from the superficial deposits forms a large item in the later
packing of acave. In the Plas Heaton cave, which I explored with
the late Mr. John Heaton, I found pieces of magnums in the
cave-earth which were beyond where man could creep when I first
knew the cave. The other end of that cave was blocked with clay,
full of glaciated boulders: a mass undistinguishable from the clayey
Clwydian drift. In the Pontnewydd cave, on the other hand, I
found felstone implements and flint flakes not far from the surface
near the mouth of the cave.

The limestone on both sides of the little ravine which runs down
into the Vale of Clwyd at Ffynon Beuno, near the village of
Tremeirchion, is perforated with numerous caves and cavernous
places. They very frequently coincide more or less with lines of
joint and small faults, along which calc-spar and various minerals
suggested the possibility of ore. One precipitous face on the north
side had an open cave large enough to furnish a shelter for cattle.
In this trial-holes had been dug, and the cave-earth had been moved
‘in places. The fragments of bone lying about suggested that the
Sheep and Fox of to- day had once been represented by the Stag and
Hyena, and I suggested to the Chester Natural Science Society to
open these caves, and foretold the probability of our obtaining the
remains of Primeval Man. The following year Dr. Hicks excavated
near the mouth of the cave, and obtained such interesting results,
that he obtained a grant from the Royal Society, and afterwards
from the British Association, to enable him to carry on the explora-
tions, the results of which he has laid before the Association and
other scientific societies. A few feet higher up the rock-face is
another opening belonging to the same drainage-system. This also
has been excavated by Dr. Hicks and Mr. Luxmoore, and it has been
supposed that in it evidence has been obtained of the residence of

Prof. T. McKenny Hughes—The Ffynon Beuno Caves. 491

Man in that locality before the close of the Glacial period. Now the
evidence is briefly this. This cave was filled with a clayey or
sandy deposit, containing bones of the extinct Mammalia and
boulders of various material. On excavating this deposit, the other
or N.W. mouth of the cave was found to be concealed under a deep
deposit of sand and sandy clay full of boulders under which, beyond
the overhanging ledge of rock, were fragments of bone similar to
those occurring in the cave, and, close to the mouth of the cave, a
flint flake was found imbedded in red sandy clay, and associated
with the teeth of Rhinoceros, etc.

Now what are the points? Was this drift No. 1, or No. 2 A, or
No. 2 B, or No. 3, of our classification given above on p. 489 ?

Certainly not No. 1, as it contains north country granites, etc.,
which came into that district for the first time with the submergence.
Therefore the drift must belong to No. 2 or 8, and these are Post-
Glacial.

We have next to ask whether it is probable that the drift which
lies on the bones outside the cave can be the drift laid down in the
great Post-Glacial submergence, and the cave-deposits belong to a
time anterior to that submergence. Let those accept this view who
can imagine that the waves dashing against a precipitous rock ex-
posed to the N.W. winds would not have swept such loose débris
into the deep fjord below, and swilled out the cave quite clean in
every tide.

I strongly suspect, though I cannot quite prove it, that the mass
which overlaps the mouth of the cave belongs to No. 8 drift—I
know of no part of the marginal drift at all like it and it differs
much from any of that seen in the central portion of the Vale.
Neither the beds in the cave nor those outside it look like a shore-
deposit.

Again, no notice has been taken of the old fence which runs along
the slope up to the precipice, about 20 feet from the entrance to the
upper cave, where the flake was found. The soil has accumulated
against the upper side of this fence until there is now a drop of eight
feet to the level of the ground on the lower side of the fence. This
tells of a pretty rapid working down the slope of all the soft surface
drift. I think I recognize in some of the stones out of the so-called
Glacial drift that blocked the cave the traces of agricultural imple-
ments as well as true Glacial strie. Yet no distinction has been
made between a newer superficial remanié drift and an older true
Clwydian drift. And rightly so I believe ; it is all remanié as far as
yet explored.

Next as to the flake. It occurred in a sandy clay such as would
be derived from the wash of the Clwydian drift mixed with the
unctuous irony residuum of the decomposed limestone, and not in
a regular layer or laminated deposit like that found more commonly

in the central portion of the cave. It was found in a kind of hori-
zontal fissure after an overhanging corner of limestone had been
removed from close above it. Inside of and more especially at the
mouth of most caves there is a breccia consisting of angular frag-

492 <A. B. Wynne—Striated Pebble from the Salt Range.

ments which have fallen from the rock while the cave was exposed
to changes in the amount of moisture and temperature. The inter-
stices get filled with inwashed clay. Sometimes the mouth is
blocked by a perfect barricade of large blocks which have fallen
from the face of the rock where most exposed. This was very con-
spicuous at Plas Heaton. At Ffynon Beuno, however, the fragments
at the upper entrance were generally small. It was among these
that the flake was found.

I do not, however, attach so much importance as some do to the
questions connected with the flake. It would be difficult enough to
prove that the group of animals found in the Ffynon Beuno caves
were Pre-Glacial, for they are the animals commonly found associated
with Paleolithic Man, and do not even include what we are accus-
tomed to consider the oldest forms amongst them.

To sum up. Firstly, the deposits of the Ffynon Beuno caves
cannot have been formed before the submergence, because rocks first
brought into the district during the submergence are found among
them. They cannot have been formed during the submergence,
because the bone deposits at the mouth would have been washed
away, and the deposits inside would have shown some evidence of
sea-sorting. So they must belong to an age later than the sub-
mergence, and a fortiori later than the Glacial age. Secondly, the
blocking of the upper entrance seems to have taken-place gradually;
and while it was going on, drift material was washed into the cave,
and various objects got into the crevices of the broken limestone
talus; but the lower end of the cave, next the precipice, remained
open. Thirdly, the paleontological evidence is against the Pre-
Glacial age of the deposit, as the bones belong to the newer group of
animals found elsewhere in undoubtedly Post-Glacial river deposits.

Il].—On a Facetrep anp Striatep PEBBLE FROM THE OLIVE
Group ConGLomERATE oF Oxren Hitt in tHE Satt RANGE OF
THE Punsas, Inpra.!

By A. B. Wynne, F.G.S.

Alvis nrc others found by Dr. H. K. Warth, the particular

pebble referred to was picked up by its discoverer on the 10th
of June, 1886, in about lat. 32° 48’ N. and long. 78° 15’ H. Its
size is 84 inches by 21 by 2 inches; and its weight is 10L0z. The
material is felsitic rock, the colour reddish-brown, and its density
= 2-608 (that of albite being 2-59—2:64).

The age of the Olive Group, from which the pebble came, is pre-
Tertiary and probably later Secondary, but has even been assumed as
Carboniferous, upon what the author believed to be inconclusive
evidence.”

The pebble itself is smoothed, polished, and striated upon twelve
different surfaces. Of these about six are perfectly flat, others less .

1 Paper read before the British Association, Birmingham.

* See Grou. Maa. Decade III. Vol. III. p. 232, 1886. The specimen itself is in

the Museum of the Department of Science and Art in Dublin, and the enlarged
photograph referred to was presented to the Geological Society, London.

A. B. Wynne—Striated Pebble from the Salt Range. 498

even. On the largest surface the striation is fine, nearly in the
direction of the longest axis of the pebble, on other surfaces they
cross this direction at various acute angles, ranging from 5° to 25°
and upwards.

An enlarged photograph of the pebble, showing its principal face
and the well-marked striation of this, was exhibited... Some of the
planes show small cavities, once apparently filled by crystals of
pyrites, which, being dislodged and forced, always in similar
parallel directions, became the graving-tools by which the stone was
scored.

Projection of some of the faces of the pebble, by Prof. O’ Reilly, Rl. Col. Sc. Dub.
Reduced to two-thirds nat. size.

SS

SS

SSS

AY
A

\)

A
ANN
Nw

In this figure the pebble’s principal face is shown to the left, and the others con-
secutively in contact in one direction as they adjoin each other on the specimen ;
the figures denoting the angle between each face.

From the position of a group of the facets, all contiguous and of
unequal size, together with the slight difference of direction in their
striation, it appears that this pebble made about a half revolution
nearly around its major axis by six separate stages, being ground and
polished at each stage to a degree closely simulating the most
artificial accuracy.

The conditions which would permit of this result become a question
for consideration. Supposing the pebble to have been grasped by ice,
whatever its bulk, having an effective hold of but two inches;
this being the utmost amount to which it could have been imbedded
while any of these surfaces was exposed: will this account for the
sculpture of the specimens ?

Other questions which the pebble suggested were :—

1. How it became so frequently shifted in the matrix which
produced the resistance that not alone was one-half of it subjected

494 Dr. W. T. Blanford—Striated Boulder from Salt Range.

to grinding processes from different directions, but its exactly opposite
side was even more perfectly smoothed and marked than any other ?

2. On the supposition that ice was an agent in the case, does the
difference in the angles of the faces and the direction of the striation
afford a measure of the plasticity of ice ?

3. What form of ice agency may have been the originating cause,
shore, ground, floe, floating or glacier ice ?

4. Was the pebble continuously frozen in or free at times, and was it
imbedded in a moving ice mass, or held so as to oppose such a force ?

5. Could any other agency than that of ice have produced the
result ?

These questions were laid before the Section, in order to obtain
general and valuable opinions, or elicit suggestions upon a point of
great interest, in any case, but particularly, as bearing upon the
existence of an earlier glacial period than that so well known to
modern geologists ; and one which has left its trace in regions where
glaciers cannot now possibly exist, though these are found, at a
distance, in the higher regions of the Himalayan chain; but even
there entirely dissociated from direct connexion with any rename of
the Salt Range Geological Series.

TV.—Notes on A SmoornEeD AND SrriatED BovLpER FROM A PRE-
TERTIARY Deposit In THE PunsaB Satt Rane!

By Dr. W. T. Buanrorp, F.RB.S., Sec. Geol. Soc.

HE block of stone in question, like another exhibited by Mr. A. B.
Wynne, was obtained by Dr. Warth, at Chel Hill, in the Punjab
Salt Range. This specimen was sent by Dr. Warth to Mr. H. B.
Medlicott, Director of the Geological Survey -of India, who forwarded
it to the present writer, in the hope of learning the views of those who
have most experience of similarly marked boulders, and of ascertaining
whether the peculiar characters of the present specimen are due to any
particular form of ice action or to any other agency.

The stone consists of a purplish-brown porphyry, apparently an
altered felspar-porphyry. This rock is known to occur in Rajputana,
near Jodhpur, between 300 and 400 miles south of the Salt Range,
and belongs to a group of beds supposed to be Archean, and known by
the name of Malani. These rocks may occur nearer to the Salt Range,
but the intervening country is imperfectly known, and is much covered
with river alluvium and blown sand.

The boulder exhibited measures 72” x 6” x 34”. It is subangular,
the two principal surfaces are plane, smooth, finely striated, opposite
to each other, and nearly but not quite parallel. Each of these sur-
faces is bevelled off on one edge by a number of smaller facets, meet-
ing the principal surface and each other at very obtuse angles. Besides
the larger plane surface there are on one side five smaller smoothed
facets, and on the other two, but one in each case is ill-marked, the
angle at which it meets the next surface being so obtuse as to be with
difficulty recognized. All the smoothed surfaces on one side are
striated in the same direction; those on the other side are striated

1 A paper read before the British Association, Birmingham.

J. Starkie Gardner—Fossil Flowering Plants. 495

similarly to each other, but diversely to those on the opposite surface
of the block. Those surfaces of the block that are not smoothed are
somewhat rounded.

The bed from which the block was obtained is said to abound in
similar boulders, but they are not in general smoothed or striated.
They are found in an olive-coloured matrix of fine silt. The bed has
been described by Mr. Wynne, Dr. Waagen, and Mr. R. Oldham, and
a general résumé of its geological relations was given in the Quart..
Journ. Geol. Soc. for the present year, p. 254. The strata immediately
overlying are marine, and contain fossils that are either Paleocene or
very high Cretaceous, but the age of the boulder bed itself is some-
what doubtful. The occurrence of large boulders in a fine silt appears
to indicate glacial conditions as in the Talchir beds of India, of which
there is a possibility that this Salt Range bed may be a representative,
although most of those who have examined the ground think it to
belong to a much later geological period, and associate it with the over-
lying Upper Cretaceous or Paleocene strata,

V.—On Fossit FLowErinG on PHANEROGAMOUS PLANTS.
By J. 8. Garpner, F.L.S., F.G.8.

UR attention has been devoted exclusively this year to the fossil
flowering or phanerogamous plants. The results of our re-
searches point to the conclusion that while that section known as
Gymnospermous, to which the Coniferss belong, is of the highest
antiquity, being almost coeval with the first definite remains of plants
in the Palzozoic age, there are no Angiospermous ‘plants in British
rocks of greater antiquity than the Secondary period, if we except
the problematic plant known as Spirangium. Even down to so late
as the Lias we have been unable to ascertain that any indisputable
Angiosperm has been discovered within our area, for we are led to
the conclusion that the supposed Monocotyledons from the Rheetics,
near Bristol, hitherto referred to the family of Pond-weeds under the
name Najadita, are really cryptogamic plants of the moss tribe,
closely allied to the river moss Fontinalis. This group had not pre-
viously been found fossil, and, so far as it goes, would indicate rather
a temperate climate. It is important to notice that these conclusions
are shared by such high authorities on fossil plants as Prof. Williamson,
Mr. Carruthers, and by all botanists who have examined them, as
well as Mr. Brodie, the possessor of the specimens. The Lilia,
Bensonia, and other supposed Monocotyledons of similar age are
very imperfectly preserved and, doubtless referable to Cycads, a
family which abounded then.

We have examined a large number of specimens of the anomalous
Jurassic plant described by Carruthers as Williamsonia. It is well
known that Prof. Williamson, in whose possession or charge a number
of the finest specimens remain, has devoted a considerable amount

‘ Being the Second Report of the Committee, consisting of Mr. W. T. Blanford,
Professor J. W. Judd, and Messrs. W. Carruthers, EL, Woodward, and J. S.
Gardner (Secretary), appointed by the British Association for the purpose ‘of reporting
on the Fossil Plants of the Tertiary and Secondary Beds of the United Kingdom,

496 J. Starkie Gardner—Fossil Flowering Plants.

of attention to them, without, however, feeling justified in coming
to any very definite conclusion as to their true position in the vegetable
world. De Saporta, on the other hand, has found more perfectly
preserved specimens in France, and has no hesitation whatever in
referring them to the group of Pandanacee. Though there are still
many difficulties in the way, our own examination of the specimens
in London, Manchester, Cambridge, and elsewhere, tends to confirm
Saporta’s view so far as that there do appear to be vestiges, in
some cases at least, of lignitic structure which may represent the
areole or carpels. These rather minute cavities and the lignitic
matter surrounding them fall away on exposure to the air, and
only traces of them are visible. Should Saporta’s contention
be upheld, Williamsonia will be by far the most perfectly known of
the Secondary Angiosperms, since all the organs of fructification
and even of foliation are more or less known.

A still more definite Monocotyledon is the Podocarya, from the
Inferior Oolite, originally figured by Buckland, and redescribed by
Carruthers. Its resemblance to the fruit of Williamsonia, as in-
terpreted by Saporta, is extremely striking, and on suggesting this
to that author, he replied that he was in the act of preparing an
important work on the very subject. The same work is to include
an illustration of the most recent member of the group, obtained
from the Grey Chalk of Dover, and which we thought advisable to
communicate to him.

Next in point of age, among English Monocotyledons, to the
Podocarya is the Kaidacarpum, from the Great Oolite, also described
by Carruthers, and by him referred to the Pandaneew. We have been
able to ascertain that a second species, hitherto supposed to be of
Cretaceous age, from the Potton Sands, is a derived fossil, and un-
doubtedly Jurassic. A third species was originally figured, without
any reference in the letterpress as to its age or lozality, by Lindley
and Hutton as Strobilites Bucklandi, in their ‘ Fossil Flora,’ vol. ii.
p- 129, published between 1833-35, from a drawing made by Miss
E. Benett for Dr. Buckland. In the first edition of Morris’s
‘ Catalogue,’ 1843, it is set down as from ‘Gr. 8. Wilts,’ which cannot
mean either Lower or Upper Greensand, the abbreviations for which
are ‘L. G. S.’ and ‘U. G.S.,’ but which certainly looks like a mis-
print for ‘Gr. O.,’ the sign for Great Oolite. In the second edition
of Morris, 1854, the locality is corrected to ‘U. G. 8S. Wiltshire,’
but it appears likely that the correction may have been made without
ascertaining the facts de novo, for the only entry occurring in Miss
Benett’s ‘Catalogue of the Organic Remains of EL ee published
in 1831, that could possibly refer to this fossil, is a ‘ Cycadeoidea ?”
from the Portland Beds, which occurs under the heading ‘ Woods’ on

9. A journey to Newcastle with the object of examining the
Hutton collection of fossil plants, where it seemed probable the
specimen might be found, has been unsuccessful, and its present
whereabouts is still unknown. We think, it however, far more
likely to prove a Jurassic than a Cretaceous ‘fossil if found, and the
genus should not be included in lists of plants of the latter age.

J. Starkie Gardner—Fossil Flowering Plants. 497

The oldest Monocotyledons thus appear to be referable to the
Pandanex, a group of plants distributed in widely distant and
remote oceanic islands, whose fruits are still met with at sea in drifts
of vegetable matter.

Next to these in antiquity are two very monocotyledonous-looking
fragments from the Jurassic of Yorkshire, which have been fully
described in the GuotocicaL MaGazine for May and August. The
one is apparently an unopened palm-like spathe, and the other a
jointed cane-like stem. Mr. Brodie possesses an undoubtedly mono-
cotyledonous leaf fragment from the Purbeck of Swindon.

The Aroidee have long been supposed to be a group of very high
antiquity, but there are good reasons for believing that the supposed
remains of aroideous plants from beneath the Tertiaries are, without
exception, referable to other groups, and actually there are no known
traces of them earlier than the Middle Eocene, when they become by
no means uncommon.

In a similar manner the fruits once supposed to represent palms
in the Paleeozoic and Mesozvic rocks have been gradually removed
or suppressed, and, unless the fragments of palm-like wood in the
Gault at Folkestone are taken into account, there are no traces of palms
in any of our Secondary strata. They, however, appear as low down
in our Eocene as the Woolwich series.

We are not able to speak with certainty regarding the supposed
liliaceous or Draceena-like stems from the Wealden, so frequently
mentioned by Mantell, since it is not easy now to identify the par-
ticular specimens referred to by him; but it is very probable that
certain stems of Endogenites in the British Museum are those intended,
in which case they are, of course, cycadeous. The Wealden has,
indeed, so far yielded no trace whatever of any more highly organized
plants than ferns and Gymnosperms, and this, when we consider
that Monocotyledons were undoubtedly in existence, is a fact that
should be of great significance to speculative geologists. The sedi-
ments must represent the deposits of the drainage system of a large
area, for they are of vast extent and thickness, varied in character,
and abounding in remains of trunks and stems, fruits and foliage of
plants. In them, therefore, if anywhere, we might reasonably expect
to find at least the traces of reed and rush, but the swamps seem to
have been tenanted only by Equisetum and ferns, and the forests by
Cycads and Conifers.

The same absence of Angiosperms, so far as British rocks are con-
cerned, is continuous throughout the Neocomian and Gault, and it is
only in the White Chalk that we meet with any indications of them,
and these only take the form of a more than suspicious impression
of a net-veined leaf, in the Jermyn Street Museum, and of some
structureless bodies which were apparently some kind of fruit.

When, however, we turn to the gymnospermous section of Phane-
rogams, the records are very different. 'To refer here to the earlier
Secondary Coniferse and Cycadez would be quite beyond our pro-
vince, and it is only those of the Cretaceous, as the last discoverable
ancestors in our area of the Hocene flora, that are of immediate

DECADE III.—VOL. III.—NO. XI. 32

498 J. Starkie Gardner —Fossil Flowering Plants.

interest. These belong, excluding Cycads, chiefly to the newest
section of the Coniferas, the Pine family. We are able to make the
following contribution to our knowledge of these:

Pinites Andrei, Coemans. ‘Flore fossile du Terrain Crétacé du
Hainault,’ 1866, p. 13, pl. v. fig. 1. Gault, Folkestone.

This specimen measures 5 centimetres in length and nearly 3c. in
breadth, though something should be perhaps deducted for the com-
pression undergone. When perfect, it was probably composed of
50 to 60 imbricated leathery scales, about half that number being
visible on the exposed face. The substance of the scale seems to
have been considerable, though the edges are thin; they are smooth
even without stri#, and with the upper margin round to obtusely
pointed. They are apparently variable in size.

The cone is of the same general type as P. Andrei, Coem., from
the Gault of La Louviére, Hainault, though somewhat shorter, more
oval, and with thinner and rounder scales. The form and general
consistence of the scales, as well as their size, the number composing
each whorl, and their disposition are, however, so similar that we
think it better, in the case of so imperfect a specimen, to unite it
rather than claim specific rank on account of distinctions that might
largely disappear with more perfect specimens. If the assimilation

is correct, the apex of the cone, as well as the base, would have been
- somewhat pointed. The cones are most abundant: at La Louvieére,
more than 100 specimens having been collected; and they are stated
to have been frequently curved and highly resinous. The specimen
from Folkestone was found by us, being unique from that locality,
and is now in the British Museum.

Pinites Valdensis, sp. nov., Wealden, Brook Point, Isle of Wight.

This fragment shows the presence in the Wealden flora of a Pine
of the section Strobus with a cone composed of scales as numerous
and thin as in any recent species. The cone was long, cylindrical,
and tapering; the scales very numerous, permanent, imbricated,
leathery, pointed, and lightly thickened at the apex, with entire
margin, striated, and slightly keeled. It somewhat resembles
P. Dunkeri, Carr., also of the Wealden, but is probably a distinct
species. One specimen is in the York Museum, and another, in
which all the scales are mutilated, is in the Woodwardian Museum.
Both these, with several others, are from the Wealden of Brook, so
that it appears to be by no means rare there. It is associated with
Cycadostrobus elegans, Carr.’

Pinites Carruthersi, sp. nov. Wealden, Brook Point, Isle of Wight.

The fragment represents another long cylindrical cone with
very numerous persistent leathery imbricated scales. It tapers like
the one last described towards the base, the scales being much
thicker, though thin at the edge, smooth, without keel, and with
entire rounded margins. It resembles the Gault species P. Andrei
in texture, but there were at least twice as many scales in each
whorl, and these are much more imbricated. It also is quite distinct
from P. Dunkeri, Carr.

1 Journ. of Bot. vol. iv. pl. lvii. fig. 9.

J. Starkie Gardner—Fossil Flowering Plants. 499

It resembles Cedrus Lennieri, ‘Sap. Vee. foss. de la Craie inférieure
des Environs du Havre,’ Mém. de la Soc. Géol. de Normandie, 1877,
but is not apparently the same species.

Pinites cylindroides, sp. nov., Lower Greensand, Potton.

This is an almost perfectly cylindrical specimen, being very
slightly thickened towards the base, 7 centimetres in length and
22 millim. in diameter, composed of about 96 scales, arranged in
12 rows from left to right, and eight rows from right to left, the
arrangement thus being 35. The scales are short and at right angles
to the axis, with a smooth flat half-moon-shaped apophysis or scale-
head, now gaping, but evidently imbricated before the seeds were
shed. The scales become very small towards the base. The summit
is abraded, exposing the end of a somewhat slender axis. Certain
grooved {lines on the sandy matrix between the scales show that
the cone was furnished with foliaceous bracts, and the marks of
a boring insect are visible. The specimen, which is quite distinct
from any other fossil or recent cone, is singularly elongated and
cylindrical, scarcely tapering at all from the base upward. It is
fortunately in excellent condition, certainly not derived from any
older bed, like so many of the Potton fossils, and is well cared for in
the Woodwardian Museum.

Pinites Pottoniensis, sp. nov., Lower Greensand, Potton.

The fragment, though much mutilated, fortunately shows the
characteristically winged seeds of Pinus in the most perfect manner,
entirely removing any lingering doubt as to the occurrence of
representatives of true Pinus as low down as the Neocomian. The
scales were set at an acute angle with slightly thickened recurved
apophyses, the form of which cannot clearly be made out, though
they appear to have been narrow, keeled, and mucronate. It nearly
resembles a type very common in the Hocene, and is of great interest
in many ways. It also is in the Woodwardian Museum, and was
obtained from the same formation.

Another specimen evidently represents a third species from the
Wealden of Brook, with scales very closely resembling a common
Barton and Bracklesham type, but its fragmentary condition scarcely
renders it advisable to attach any specific name to it.

The accompanying list comprises all the British Cretaceous
Coniferee previously known up to the present date, though there is no
doubt that many new and undescribed forms exist in collections.

List or British CRETACEoUS CONIFER PREVIOUSLY DESCRIBED.

Pinites Fittoni, Carr., Purbeck, Fitton, Geol. Trans. 2nd series, vol. iv. p. 280, pl.
xxii, fig. 9. Dammarites, Ung. G. et Spec. Plant. foss. p. 384. Gro. Mac.
Vol. IIL. p. 543.

P. Manteilii, Carr., Geol. I. of W. 2nd ed. p. 452, 3rd ed. p. 377, pl. xlii. ; and
Carr. Gym. Fruits, Grou. Mac. Vol. III. p. 543, Pl. XXI. Fig. 3, Tilgate.

P. patens, Carr. id. p. 543, Pl. XXI. Fig. 4, Tilgate.

P. Dunkeri, Carr. id. p. 542, Pl. XXI. Fig. 1-2, Brook. Abietites, Mant. Geol. I. of
Wight, 2nd ed. p. 452.

P. Sussexiensis, Carr. Zamia, Mant. Quart. Journ. Geol. Soc. vol. ii. p. 51, pl. 2,
fig. 1; Zamites, Morris Cat, Zamiostrobus, Goepp. Ueber Schless, Gesellsch.
1844, p. 129; Pinites, Carr. Grou. Mac. Vol. III. p 541, Pl. XX. Figs, 6, 6.

Cedrus Leckenbyi, Carr. Pinites,Guon. Maa. Vol. VI. p. 2, Pl. I. Fig. 1-5, Shanklin,

500 J. Starkie Gardner—Fossil Flowering Plants.

P. elongatus, Endl, Synops. Conif. p. 286 ; Strobilites, Lind. and Hutt. Foss. Flora,
vol. ii. p. 28, pl. 29.

C. Benstedi, Carr. Abies, Mant. Quart. Journ. Geol. Soe. vol. ii. p. 51, pl. ii. fig.

2, 1846. Pinites, Carr. Journ. Bot. Jan. 1867; Grox. Mac. Vol. III. p.

541; Abietites, Goepp. Foss. Conif. p. 217.

Abies oblonga, Lind. and Hutt. vol. ii. p. 155, pl. exxxvii. Supposed to be from
Greensand, near Lyme Regis; described by a misprint as from ‘ Dresent,’
instead of ‘present’ shore. Elate, Unger, Syn. p. 199. Abietites, Goepp.
Foss. Conif. p. 207. Pinites, Endl, Synops. Conif. p. 248; Carr. Gon. Mac.
Vol. III. p. 541. (Professor Williamson is describing a magnificent specimen
of this or an allied form).

Pinites gracilis, Carr. Gault, Folkestone, Grot. Mae. Vol. VI. p. 2, Pl. I. Fig. 9.

P. hexagonus, Carr. id. Vol, VIII. p. 540, pl. XV.

Sequovites Gardner, Carr. id. Vol. VI. p. 2, Pl. I,

Sequotites ovalis, Carr. id. Vol. VIII.

Sequotites Woodwardii, Carr. Grou. Mac. Vol. III. p. 544, Pl. XXI. Fig. 11-16,

Blackdown.

We have now dealt with the more highly-organized of our
Mesozoic plants, and pass on to those of the Hocene.

Among the most interesting of recent discoveries is that of plant
remains in a small sand-pit at Colden Common, between Bishopstoke
and Winchester, the first locality in the Hampshire basin that has
yielded any of Woolwich and Reading age. This was first com-
municated to us by Mr. Whitaker, who thought the leaves might
prove to be of London Clay age. They are, in fact, actually included
in its basement bed, and mingled with casts of marine shells and
sharks’ teeth, but the blocks of clay with leaves are derived, though
other unfossiliferous clay-seams are in situ. If not of London Clay
age, however, they are much nearer to it than the Reading flora,
which occurs below the great mass of mottled clay, whilst these
lie above it. The plants show in the main, as might be anticipated,
an approach to the Alum Bay flora, which is still higher and
above the London Clay; but whether these leaves are connected
in any closer degree with the fruits of Sheppey than are those
from Woolwich, Croydon, or Bromley, is a question which we
have not as yet the data for answering. There are, at all events,
no remains of Palms among them, and this, so far as it goes,
is against the connection; but on the other hand the fruits of an
Alnus, like that from Swale Cliff, abound. There is no large
variety among the leaves, the majority being large and simple, but
with highly serrate margins, and the species will not be found
to exceed 12 or 14 in number, including Platanus, which is rare.

Though we have continued to collect at Reading, we have been
unable so far to determine any new species. The assemblage of
fruits at Sheppey, on the other hand, becomes of increasing interest,
and has proved unexpectedly rich in Palms, many of them apparently
identical with existing species which are now found growing in the
remotest regions.

Besides the large variety of Nipas, which are still met with in
enormous abundance among the seed-vessels of the New Guinea
drift, we have seeds indistinguishable from Verschaffeltia splendida,

1 A far larger specimen than that originally described, 8 inches long by 14 inches
in diameter, has since been found.

J. Starkie Gardner—Fossil Flowering Plants. 5OL

endemic to the Seychelles, from Sabal Blackburniana of the Ber-
mudas, from a Desmoncus, an Areca, a Monodora, and probably
of many, certainly of some other palms. When we consider that
probably many of the kinds of palm fruits would sink at once, we
realize how great an assemblage of this magnificent family is indi-
cated by the Sheppey drift.

The difficulties we fear of determining anything but a fraction
of the Sheppey fruits must prove insurmountable. Their outer coats
are for the most part destroyed, and some part of their inner structure,
nearly always quite different in form from that which is external, is
revealed. Botanists have been able to determine but few of the
drifted fruits brought home by the Challenger, though these are more
perfect and of living species belonging to definite and known floras.

The Bournemouth cliffs continue to furnish fresh forms, though
the leaf-beds are becoming more and more difficult of access. We
have especially enriched the series of Smilacee, and a complete
account of them has been presented to the Linnean Society. The
series now obtained falls little short of a hundred specimens, and is
by far the richest of fossil Smilaceze, perhaps of any family, ever
brought together. Such a material has enabled us to reduce the
number of distinct species to no more than five, most of which are
represented by foliage in all stages of development, from the largest
leaves measuring several inches, down to quite minute leaves from
near the extreme growing points. The necessity for such extensive
series when dealing with fossil leaves may not at once be apparent,
but the President of the Linnean Society expressed the opinion at
the meeting, that out of less material, not five, but five-and-twenty
Species might have been made.

The leaves of Smilaceze are highly characteristic, and can be
determined with a large degree of certainty ; but it is quite im-
probable that such will be the case with very many of the families
of Dicotyledons. There is, indeed, little hope that more than a very
few can be determined with anything like the precision required for
botanical purposes, unless we can call in aid the fruits or some other
organs. ‘l'hus if we may base a conclusion upon the large number
of the characteristic bracts, which envelope the seed in a section of
Flemingia that are met with in the Bournemouth flora, the leaves of
that genus should be far from uncommon, and they should also be
found in the Swiss Oligocene, yet no species of Flemingia has ever
been recorded from the Tertiaries. The leaves, however, may be
sought for among the supposed species of Populus and Carpinus.

Fortunately fruits and even flowers are comparatively abundant
at Bournemouth, and we consequently anticipate little difficulty in
determining leaves belonging to such easily distinguishable fruits as
Alnus, Tilia, Acer, Carpinus, the Leguminose, and many others, but the
residuum with indeterminable fruits, or fruits that will not float, may
be very large. We are thus brought to the question, whether any
value beyond that of mere landmarks, or aids to the correlation of
rocks, can be attached to the determinations of fossil dicotyledonous
leaves arrived at when fruits are absent. Nearly every Tertiary and

502 J. Starkie Gardner—Fossil Flowering Plants.

even many Cretaceous floras are said to comprise Quercus, and Fagus,
and Corylus, to select these as typical examples. Now we very much
doubt whether the fruits of these genera have been met with in any
strata older than the Upper Miocene, we might almost say the
Pliocene; whilst in the latter the fruits of at least two of them are
very far from uncommon. Fossil hazel-nuts are well known to
abound in forest beds such as the one at Brook, in the Isle of Wight,
and at Carrickfergus. It does appear to us that it would have been
wiser and more consistent, when arriving at these determinations, to
have taken the absence of fruits into account, when these were such
as would naturally have been preserved. The large proportion of
fossil dicotyledonous leaves that have been referred without any
hesitation to living genera must strike every one, in comparison with
the relatively few associated fruits that have been determined other-
wise than as Carpolithes—a name which is a confession of failure.
It will thus be seen that in our opinion the fossil Dicotyledons of our
own Kocene must be dealt with in a manner different from that
pursued by the majority of foreign writers on kindred subjects, and
that a revision of much of their work is urgently needed.

To resume our immediate subject, we have nothing new to record
of the Bracklesham flora except that Mr. Elwes, in excavating in the
New Forest, met with Nipadites in some abundance, and a specimen
he still has proves the species to be the same as that from Bracklesham
Bay, and entirely different from that which forms a conspicuous zone
in the marine series of the Bournemouth group.

At Barton, on the other hand, we have been able to procure nearly
a dozen pine-cones, hitherto a great desideratum, from the Highcliff
beds, which go far to prove that there is only one variety there,
indistinguishable from the Pinus Dixoni of Bracklesham. Along
with these we have branches of apparently the Bournemouth
Araucaria, and an important and entirely new fruit, fortunately
represented by many specimens, which permit us to examine the
details of their structure. These consist of twigs on which are
seated in some profusion clusters of numerous sessile woody peri-
carps with deeply laciniate margin, giving the fruit when closed the
appearance of a large burr. ‘These inclose a nut or seed, rather
smaller, but otherwise resembling that of a cucumber. ‘There has
not yet been time to make the researches necessary to come to a
conclusion regarding it, and Mr. Carruthers and other botanists who
have seen the specimens are unable offhand to pronounce upon its
affinities. A rather large fossil plant from the same locality has
recently been lent us by the Council of the Hartley Institute, and
altogether the plants from this horizon, hitherto very meagrely re-
presented, bid fair to take an important position. On the other hand,
the Hordwell end of the same section, though twice visited since our
last report, has furnished nothing new.

We have fortunately met with a few very distinctly marked leaves
from the Middle Headon of Headon Hill, preserved in the York
Museum, which with those previously obtained from the Lower
Headon of Hordwell, help to bridge-over one of the few gaps in our
really surprisingly complete succession of Hocene floras.

Notices of Memoirs—Sir W. Dawson on Fossil Alge. 503

We have continued to investigate the great series of plant remains
so assiduously collected by Mr. A’Court Smith, and with this object
have visited Gurnet Bay, as well as receiving several packages of
fossils from thence. While lamenting that they are of so fragmentary
a nature, we cannot overlook their importance as almost the last
representatives of the great series of floras which maintained them-
selves in our area throughout the Hocene time. As an illustration of
their value, we may instance the fact that while anything like true
grasses seem to be wholly wanting in the previous floras, there are
many more or less definite indications of them in this. We have
reason to hope that renewed working in the still younger beds of
Hempstead may lead to further discoveries, for, besides the better
known plants described by Heer, pine-cones and a fine aroideous
fruit have been obtained from them.

IN @aniWeintsS|) (Ol AMEIsH IM @ ens

pes Rie wes
Papers read before the British Association for the Advancement of Science,
Birmingham, September, 1886, Section C (Geology).
I.—On Canapran Exameptes oF Supposep Fossum Atem. By Sir
Wituram Dawson, LL.D., F.R.S.

ARKINGS of various kinds on the surfaces of stratified rocks
have been loosely referred to Algee or Fucoids under a great
variety of names; and when recently the attempt was made in
Europe more critically to define and classify these objects, a great
divergence of opinion developed itself, of which the recent memoirs of
Nathorst, Williamson, Saporta, and Delgado may be taken as examples.
The author, acting on a suggestion of Sir R. Owen, was enabled in
1862 and 1864, by the study of the footprints of the recent Limulus
polyphemus, to show that not merely the impressions known as Protich-
nites and Climactichnites, but also the supposed fucoids of the genera
Rusophycus, Arthrophycus, and Cruziana are really tracks of Crustacea,
and not improbably of Trilobites and Limuloids.t| He had subsequently
applied similar explanations to a variety of other impressions found on
Palzozoic rocks.” The object of the present paper was to illustrate by
a number of additional examples the same conclusions, and especially
to support the recent results of Nathorst and Williamson.

Rusichnites, Arthrichnites, Chrossochorda, and Cruziana, with other
forms of so-called Bilobites, are closely allied to each other, and are
explicable by reference to the impressions left by the swimming and
walking feet of Limulus, and by the burrows of that animal. They
pass into Protichnites by such forms as the P. Davisii of Williamson,
and Saerichnites of Billings, and Diplichnites of the author. ‘hey are
connected with the worm tracks of the genus Wereztes by specimens of
Arthrichnites, in which the central furrow becomes obsolete, and by the
genus Gyrichnites of Whiteaves.?

1 <*On Footprints of Limulus,’? Canad. Nat. 1862. ‘On the Fossils of the

Genus Rusophycus,’’ Ibid. 1864. j
2 « On Footprints and Impressions of Aquatic Animals,’’ Am. Journ, of Science.

3 Trans. Royal Society of Canada, 1883.

504 Notices of Memoirs—Arctic and Atlantic Basins.

The tuberculated impressions known as Phymatoderma and Cauler-
pites may, as Zeiller has shown, be made by the burrowing of the mole-
cricket, and fine examples occurring in the Clinton formation of
Canada are probably the work of Crustacea. It is probable, however, that
some of the later forms referred to these genera are really Algz related
to Caulerpa, or even branches of Conifers of the genus Brachyphyllum.

Nereites and Planulites are tracks and burrows of worms, with or
without marks of sete, and some of the markings referred to Pal@o-
chorda, Paleophycus, and Scolithus have their places here. Many
examples highly illustrative of the manner of formation of these im-
pressions are afforded by Canadian rocks.

Branching forms referred to Licrophycus of Billings, and some of
those referred to Buthotrephis, Hall, as well as radiating markings
referable to Scotolithus, Gyrophyllites, and Asterophycus, are explained
by the branching burrows of worms illustrated by Nathorst and the
author. Astropolithon, of the Canadian Cambrian, seems to be some-
thing organic, but of what nature is uncertain.

Rhabdichnites and Hophyton belong to impressions explicable by the
trails of drifting seaweeds, the tail-markings of CRUSE CR and the ruts
ploughed by bivalve molluscs.

Dendrophycus, Dictyolites, some species of Delesserites, Aristophycus,
and other branching and frond-like forms, were shown to be referable
to rill-marks, of which many fine forms occurs in the Carboniferous of
Nova Scotia, and also on the recent mud-flats of the Bay of Fundy.

The genus Spirophyton, properly so called, is certainly of vegetable
origin, but many markings of water action, fin-marks, etc., have been
confounded with these so-called ‘ Cauda-galli fucoids.’

On the other hand, some species of Palgophycus, Buthotrephis and
Sphenothallus were shown to be true Alge, by their forms and the
evidence of organic matter, and Haliserites, Barrandeina, and Nemato-
phycus were shown to include plants of much higher organization than
the Alge. With reference to the latter, it was held that the form to
which the name Prototaxites had been given was really a land plant
growing on the borders of the sea, and producing seeds fitted for
flotation. On the other hand, certain forms to which he had given the
name Vematoxylon were allied to Alge in their structure, and may have
been of aquatic habit ; very perfectly preserved specimens of these last
had been recently found, and had thrown new light on their structure.

The author proposed to apply to all these problematical plants,
having a tissue of vertical and horizontal tubes, the general name
Nematophytee or Nematophyton.

The paper referred to the history of opinion on these objects and the
bibliography of the subject; but this, as well as detailed descriptions,
are omitted in this abstract.

IJ.—Ow tHe Renations or tan Grorocy or tHE Arctic AnD ATLANTIC
Bastys. By Sir J. Wittram Dawson, LL.D., F.R.S.

HE paper relates to the evidence of the specimens brought from the
Arctic seas bearing on the existence of an ancient line of Lauren-

tian Huronian, and other Pre-Cambrian rocks; of the extension of the
marine fauna of the Atlantic and the American continental plateau

Notices of Memoirs—Dr. Dawson—On the Rocky Mountains. 505

into the Arctic, and of the correspondences of the Cretaceous, Tertiary,
and Pleistocene of the Arctic Basin with those of America, and the
bearing of these facts on questions of paleeogeography.

II].—Own tHe Rocky Mountains, WITH SPECIAL REFERENCE TO THAT PART
oF THE RANGE BETWEEN THE 49TH PARALLEL AND HEAD-WATERS OF
THE Rep Drer River. By Georce M. Dawson, D.S8c., F.G.8., etc.,
Assistant-Director, Geological Survey of Canada.

HE term ‘‘ Rocky Mountains”’ is frequently applied in a loose way
to the whole mountainous belt which borders the west side of
the North American continent. This mountainous belt, is, however,
preferably called the Cordillera region, and includes a great number of
mountain systems or ranges, which on the 40th parallel have a breadth
of not less than 700 miles. Nearly coincident with the 49th parallel,
however, a change in the general character of the Cordillera region
occurs. It becomes comparatively strict and narrow, and runs to the
56th parallel or beyond with an average width of about 400 miles only.
This portion of the western mountain region comprises the greater
part of the province of British Columbia. It consists of four main
ranges, or, more correctly, systems of mountains, each including a
number of component ranges. These mountain systems are, from east
to west:—(1) The Rocky Mountains proper. (2) Mountains which
may be classed together as the Gold Ranges. (8) The system of the
Coast Ranges of British Columbia, sometimes improperly named the
Cascade Ranges. (4) A mountain system which in its unsubmerged
portions constitutes Vancouver and the Queen Charlotte Islands.

The present. paper refers to the Rocky Mountains proper. This
system, between the 49th and 58rd parallels, has an average width of
about 60 miles, which, in the vicinity of the Peace River, on the 56th
parallel, decreases to about 40 miles. It is bounded to the east by the
Great Plains, which break into a series of foot-hills along its base; to
the west by a remarkably straight and definite valley occupied by
portions of the Columbia, Kootanie and other rivers.

Since the early part of the century the trade of the fur companies
has traversed this range, chiefly by the Athabasca and Peace River
Passes, but till the explorations effected by the expedition under Capt.
Palliser in 1858-59 nothing was ‘known in detail of the structure of
the range. At the inception of explorations for the Canadian Pacific
Railway, Palliser’s map was still the only one on which any reliance
could be placed, and it applied merely to the portion of the range south
of the Athabasca Pass. During the progress of the railway explora-
tions a number of passes were examined, and in 1883 and 1884 that
part of the range between the 49th parallel and latitude 51° 30” was
explored and mapped in some detail in connection with the work of
the Canadian Geological Survey by myself and assistants.

Access to this, the southern portion of the Rocky Mountains within
Canadian territory, being now readily obtained by the railway, its
mineral and other resources are receiving attention, while the magnificent
alpine scenery which it affords is beginning to attract the attention of
tourists and other travellers.

The results of the reconnaissance work so far accomplished are

506 Notices of Memoirs—Anorthosite Rocks of Canada.

presented in the form of a preliminary map, accompanied by descrip-
tions of routes and passes, and remarks on the main orographic features
of the range.!

IV.—Tue Awnorrnostre Rooxs or Canada. By Franz D. Apams,
Geological Survey of Canada.

fw series of rocks has also been called the Upper Laurentian or

Norian series. The name anorthosite is perhaps preferable, as it
refers to their distinguishing characteristic as compared with the ortho-
clase rocks of the Lower Laurentian, viz. the predominance in them of
plagioclase or anorthose felspar. These rocks form detached areas in
the great Laurentian districts, and bear a strong resemblance in part
to the gabbros and gabbro-diorites of Scandinavia, and in part to the
labradorite rock of the same country. It is, however, by no means
certain that the rocks of the two countries are of the same age. At
least nine of these areas are now known to exist in Canada, and there
is also one in the State of New York. In addition to plagioclase,
which generally predominates largely, these rocks contain rhombic and
monoclinic pyroxenes (including augite, diallage, hypersthene, and
probably enstatite), olivine, magnesia, mica, spinel (including both
pleonaste and picotite), garnet, iron-ores, pyrite, and apatite. Ortho-
clase is seldom or never found, except in veins cutting the anorthosite.
The hornblende, mica, and pyroxenes are intimately associated and
often intergrown, all of them sometimes being found in the same thin
section. Garnet occurs sparingly, and generally near the contact of
the anorthosite with the gneiss. When the olivine comes against
plagioclase, it is always bounded by a double concentric zone, the outer
zone consisting of hornblende, and the inner, or that next to the
olivine, consisting of a pyroxene. While the iron-ores associated with
the Lower Laurentian gneisses are generally free from titanium, those
associated with the anorthosite rocks are always highly titaniferous; a
fact which makes the study of these rocks a matter of considerable
economic interest. The anorthosite varies a good deal in composition,
some areas, for instance, being rich in olivine, while others are destitute
of that mineral, and different portions of even the same area often
showing wide differences in this respect. The rock also shows a good
deal of variation in structure. It is rarely quite massive, frequently
well foliated, but usually consists of a rather coarsely crystalline ground-
mass, through which are scattered irregular strings and masses com-
posed of iron-ore, bisilicates, and mica, as well as larger porphyritic
crystals of plagioclase. ven when it is tolerably constant in com-
position, there is generally a great variation in size of grain, coarse and
fine alternating in rude bands or rounded masses. In the case of some
of the areas there can be but little doubt that the anorthosite is
eruptive, in others, however, it seems to be interstratified with the
Laurentian gneiss, and in one of them to merge imperceptibly into it.
The original relations of the rocks are, of course, much obscured by the
effects of subsequent heat and pressure. The evidence at present, how-
ever, seems to indicate that these anorthosites are the result of some
kind of extravasation, which in those early times corresponded to what
in modern times we call volcanic eruption.

See Reports and Maps Geological Survey of Canada.

Notices of Memoirs—Fossil Fish fiom Keuper. 507

V.—Norrs on tae Crystattive Scaists oF soME PARTS OF IRELAND.
By C. Cattaway, D.Sc., M.A., F.G.S.

HE author gives a summary of results obtained by a preliminary

survey of the principal areas of Irish metamorphic rocks, viz.—

1. Donegal, including parts of the adjacent counties of Londonderry
and Tyrone.

2. Connemara, extending the term to cover the region lying between
Westport, co. Mayo, and the granitic mass west of the town of Galway.

3. The south-eastern corner of the county of Wexford.

In each of these areas the following facts were observed :—

(a) A series of hypometamorphic rocks, consisting typically of
fine-grained schists, altered grits, and quartzites. A clastic structure
is more or less distinct in the three areas, but is least evident in
Connemara.

(6) A group of highly crystalline schists, displaying no trace of an
original sedimentary origin, dipping as if it passed below the hypo-
metamorphic rocks. At Wexford there are true gneisses. In Conne-
mara the rocks are less felspathic, the chief types being quartzose
gneiss, quartz-schist, mica-schist, hornblende-schist, quartzite, and
crystalline limestone. This description will also apply to Donegal.

(c) Granite, underlying (4), and in Connemara and Donegal clearly
intrusive.

The author urges that this analogy is not due to the metamorphic
action of the granite ; for—

1. The mineral characters apparent in the schists adjacent to the
granite are uniformly distributed through the lower series from bottom
to top.

2. The evidence collected is hostile to the view that this lower series
ever graduates into the upper,

It is concluded that the balance of proof is in favour of the Archean
age of the bulk of the Irish schists.

1. In the Wexford district the schists are thrown against Cambrian
and Ordovician rocks by fauits, and do not pass into them in the
localities alleged by the Irish Survey.

2. In Connemara conglomerates of Llandovery age contain large
rounded fragments, not only of the older schistose series, but also of
its intrusive igneous rocks.

3. In the Ulster region the metamorphic area is separated from the
Ordovician rocks of Pomeroy by a ridge of granite and diorite three
miles in breadth.

The lithological analogies between the Irish schists and the Archean
rocks of Anglesey and other British metamorphic districts are also of
weight in the argument.

VI.—On tue Discovery or Foss Fiso 1y tae New Rep Sanpsrone
(Upprr Kevuprr) in Warwicxsuire. By the Rev. P. B. Bronrz,
MEA EGS,

HE author observed that, considering the thickness and extent of
the New Red Sandstone in Great Britain, the paucity and rarity

of fossils was remarkable, especially when compared with the abundant
fauna und flora of the Trias in Europe. In a field so comparatively

508 Notices of Memoirs—Range of Rhetic Fossils.

barren any addition, therefore, to either is interesting to the palzeonto-
logist. Many years ago the author discovered a ganoid fish—the last
apparently of the genus Palgoniscus superstes—figured and described
by the late Sir Philip Egerton (Journ. Geol. Soc. vol. xiv. p. 164) in
the Upper Keuper at Rowington (six miles north-west of Warwick) ;
and he now records another discovery of several small fish near there,
probably Semionotus—at present in Dr. Traquair’s hands—which is the
first time this genus has been recorded from the British Trias. The
remains of small Cestracionts are not unfrequent in one particular band
of sandstone in Warwickshire and Worcestershire, with occasional
footprints in the former county of Labyrinthodon. Ganoid fish are so
rare that these above named are, as far as the author is aware, the only
ones known, with one exception, which cannot be secured, in the Upper
Keuper; the curious Dipteronotus having been found in the Lower
Keuper (waterstones) at Bromsgrove, in Worcestershire. The author
gave a section of the quarry containing the fossils above referred to,
and stated that he considered that the New Red Sandstone in Warwick-
shire, as the Rev. J. Mello has adopted in Cheshire, might fairly and
advantageously be divided into Upper and Lower Keuper, the two
series of sandstones being different lithologically, and being separated
by a considerable thickness of red marl, the lower sandstones being
especially characterized by remains of Zabyrinthodon and other peculiar
reptiles, a fine and unique collection being preserved in the Warwick
Museum. -

VII.—On tHe Rance anp Extent anv Fossits oF THE Rumtic FormA-
TION IN WARWICKSHIRE. By the Rev. P. B. Broprn, M.A., F.G.S.

\HE author in this paper first gives an account of the range, thick-
ness, and fossils of the upper portion of the Rhetic formation—

viz. the ‘White Lias,’ supposing that it really belongs to this, but to
which it is now generally assigned, showing that it is very rarely seen
in conjunction with the underlying shales, and that where they occur
in one or two important sections the White Lias is absent. A list of
the fossils is given, which are few and ill-preserved, Ostrea intusstriata
and a species of Avicula (Monotis) being the most characteristic. A
full account is given of the succeeding grey and black Rhetic shales
with occasional intercalated shelly limestone and sandstone; and though,
as arule, good sections are rare, there were certain railway-cuttings
which laid open several very interesting and instructive ones, and
enabled the author to obtain a series of characteristic fossils, including
the Radiata, by no means common and local, the Ophiolepis Damesti.
It was stated that these occupied a considerable area in the southern
division of the county, appearing again on the north-east, near Kugby,
and as a rule succeeded by the basement beds (insect and saurian beds)
of the Lower Lias, which were in places seen in conjunction with these
shales. It was further observed that they probably underlie the Lias
in its course through the county; and the author concluded by showing
the general range of the Rheetics from the coast of Devon to the coast
of Yorkshire; which, although not comparable either in thickness or
abundance and variety of fossils with the rich, varied, and peculiar

Notices of Memoirs—Pleistocene Vale of Clwyd. 509

Continental series, is still sufficiently marked and important in this
county and elsewhere to make it a distinctive and independent forma-
tion.

VIII.—On tHe Srturtan Rocks or Norra Wates. By Professor T.
M‘Kenny Hueuss, M.A., F.G.S.

HE author begins by describing some sections in the Silurian rocks

of North Wales. Some of them are in the lower part, some in

higher beds. He gives lists of fossils from the various horizons in each.

He then, by means of these and by what he calls syntelism, that is,

the occurrence of similar sequences of beds of the same characters,

lithological or other, points out the corresponding parts of the various
sections described.

He then does the same for the Silurian of the eastern borders of the
Lake district, and, having in this manner constructed a vertical section
of each, compares the two districts and shows that there is an identical
series in each, with all the important zones of one represented in the
other, except that in the part of North Wales which he has worked
out he has not yet detected beds as high as the newer part of the series
in the Lake district.

1X.—NorEts on somME SEcrions IN THE AReENIG SeErRrES or Norru
Wates anp THE Laxe Disrrictr. By Professor T. M‘Krenny
Hueues, M.A., F.G.S8.

N this paper the author describes a number of sections which cross

the Arenig series in different parts of England and Wales, and

endeavours to explain some apparent discrepancies in what is generally
a remarkably constant set of beds.

He starts with the Portmadoc section, where he considers that the
chief differences of opinion have arisen from mistakes in the explana-
tion of the geological structure of the district, especially from the
wrong identification of some grit bands on opposite sides of important
faults.

Following the series to the north he shows that, although they vary
in thickness, the principal zones are still represented near Carnarvon ;
and, discussing the question of the unconformity of these beds on the
Lower Cambrian, he points out that the Lower Cambrian rocks are
seen to vary so much both in character and thickness within short
distances in the neighbourhood of the existing outcrop of the Archean
that any argument founded upon their thinning-out or their different
texture must be received with distrust in an area where they are known
to have been deposited on the flanks of mountain ranges of pre-Cam-
brian age.

He then describes some localities in the Lake district where the
occurrence of the same zones has been determined, and points out the
difficulty of getting rid of such great thicknesses of deposits of fine
mud as would be implied in the usual interpretation of those areas.

X.—On tHE Prerstocenr Deposits or THE VALE oF Crwyp. By
Professor T. M‘Knnny Hucues, M.A., F.G.S.

/Y\HE author cautions observers against inferring too hastily the

glacial origin of beds from their containing glaciated boulders.

510 Notices of Memoirs—Deep Borings in Kent.

He describes the drifts of the western part of North Wales, grouping
them under two heads :—

1, The Older or Arenig Drift, or that in which boulders were trans-
ported from Arenig into the Vale of Clwyd; and

2. The Newer or Clwydian Drift, or that due to the destruction of
the older glacial deposits by marine action, during which boulders
were carried on floating ice from the north, and flints travelled in the
shingle round the coast. All the shells found in it are of species still
living on the adjoining coast: but some of the shells found in what
he considers part of the same series of deposits in neighbouring districts
are of a more arctic type, and may beleng to an earlier part of the
same epoch,

He then gives an account of the principal caves explored about the
Vale of Clwyd, and explains their relation in each case to the drifts of
the district ; inferring that, while some of them may be older than
the marine Clwydian drift, and some may possibly be even preglacial,
yet that none of the bone-deposits so far found in any of them can be
referred to so early a date.

XI.—Svrrrementary Nore on Two Deep Borrnes in Kent. By
W. Wuirarer, B.A., F.G.S., Assoc. Inst.C.E.

HE paper ‘‘On Deep Borings at Chatham,’? communicated in
abstract to the last meeting of the Association, was afterwards
read, with various additions, to the Geological Society. Since then,
however, further information has been got, some of which is of im-
portance, especially in view of the fact that the South Eastern Railway
Company is about to make a deep trial-boring at Dover.

The boring at Chattenden Barracks, near Chatham, has been finished,
being taken to a depth of over 1160 feet, the bottom of the Gault being
reached at 1162 feet, where sand (Lower Greensand) was found and
water got. In my account of the section it was left, in Gault, at 1103
feet, and I ventured to say that ‘‘some 60 feet more would reach the
bottom of that formation’; this happened in 59 feet. I did not
venture, however, to predict the finding of Lower Greensand, as, from
the thinness of that series at Chatham, a little southward, it was quite
possible that it might soon disappear northward.

The almost exact correspondence of the combined thickness of Chalk
and Gault here, 872 feet, with the same total at Chatham (875 and
878 feet in two borings) is noteworthy. Of course there is no Upper
Greensand, which formation is absent at the outcrop on the south.

The Dover boring has been carried a few feet deeper and abandoned.
I have visited the site, and procured a good set of specimens of the
bottom clays, of which we had but a few small pieces before.

These specimens have been carefully examined, and the result of
this examination is, I think, worthy of notice. As regards fossils it is
simply negative, my colleagues, Mr. G. Sharman and Mr. E. T. Newton,
after washing and sifting pieces of many specimens, were unable to
detect any organism, with a solitary exception, and that was a simple
example of a species of otalia, which, struggling into existence
in Silurian times, has managed to survive to the present day! I
have some doubts, too, whether this one fossil may not have fallen

Notices of Memoirs—Deep Borings in Kent. 511

down the bore. Anyway it proves nothing. As regards the character
of the beds, however, I think that a reasonable conclusion may be
inferred from the specimens.

In my published account certain beds are referred, with some doubt,
to the Lower Greensand. The reference is wrong and the doubt right,
for the top five feet, of the 49 credited to Lower Greensand, really
belong to the base of the Gault, and the bottom thirteen feet to the
Wealden, as I believe. The Lower Greensand is left, therefore, with
only 31 feet of clayey sand. It is curious that specimens from
the bottom part (838 to 848 feet) are exactly lke the corresponding
specimens from the bottom part of the Lower Greensand in the
Chatham boring (932 to 948 feet), the two sets having about the same
vertical extent (10 or 11 feet).

These specimens remind one of the division known as the Sandgate
Beds, and I am inclined to think that this division alone occurs at
Dover, the Folkestone Beds above and the Hythe Beds below having
thinned out, although both those divisions are thicker than the
Sandgate Beds at the outcrop.

The clayey beds beneath have been proved to a thickness of some 80
feet, the boring ending at about 930 feet. In my paper I spoke of
chalky matter occurring in them, but in this I was wrong. The white
specks in the small specimens first seen certainly looked calcareous, but
the examination of better specimens has shown that they are anything
but that. Indeed, the prevailing character is the absence of any
effervescence when the clays are treated with hydrochloric acid; in
many cases peculiarly fine-grained whitish beds simply absorb the acid,
without any effervescent action.

On comparing the specimens with other clays, they were found to be
unlike any of the marine Cretaceous and Jurassic clays, and it seemed
to me that their affinities lay rather with the Wealden series, and
probably with the lower, or Hastings division, than with the Weald
Clay.

I have only lately been able to test this by the help of a set of
specimens that Mr. G. Maw has been kind enough to send me. On ex-
amining them I found that three specimens of Weald Clay, from Surrey,
effervesced readily, which is perhaps not surprising as they came in two
cases from close to Horsham stone, and in the other from near a Paludina-
bed. Nine specimens from a more distant district, Dorsetshire, did not
effervesce ; but one can hardly give the exact position of these in the
Wealden Series. ‘Ten specimens from the Ashdown Series, the lowest
division of the Hastings Beds, not only, in some cases, resembled Dover
specimens in character (I speak from memory, not having had the two
sets side by side), but in every case refused to notice the presence of
hydrochloric acid.

Should this classification be right, it serves to strengthen very much
the conclusion, in my paper, that Dover is on all grounds a good site
for a deep trial-boring,' for it looks as if the bottom part of the great
Wealden Series came there within 600 feet of the surface in the low
ground, the boring being described on a site 280 feet above the sea.

1 Quart. Journ. Geol. Soc. 1886, vol. xlii. p. 44,

512 Reviews—Prof. Edward D. Cope—

Gee Ea Ve, 2 GNSS

T.—DepPARTMENT OF THE INTERIOR. ReEpPoRT oF THE UNITED States
GrotocicaL SuRVEY oF THE TrRRITORIES. F. V. Haypen, Unitrep
Srates Gronocist-In-CHarce. VotumE II]. Tue Verreprata
or THE TrRTrARY Formations oF THE West. Boox I. By
Epwarp D. Corz, Member of the National Academy of Sciences.
(Washington, Government Printing Office, 1883.)

(Continued from p. 477.)

HE rocks of Middle Tertiary Age, which are found in the far
west of the United States, are calcareous clays and marls,
alternating with light-coloured sandstone. In Oregon they are often
old trachytic muds, three to four thousand feet thick, and about
2300 feet thick in Nevada. But on the White River in Nebraska the
thickness of these rocks is reduced to 150 feet, and there the strata
are divided by Hayden into eight zones. The Oregon beds are
typically seen on the John Day River, so that the White River and
the John Day beds are regarded as equivalent, and belong to the
Miocene series. ‘These rocks hitherto have yielded no Fishes or
Amphibia, and no traces of Birds; so that the discussion of their
fauna is limited to Reptiles and Mammals.

The striking feature of the reptilian life, as compared with that of
the older Eocene series, is the absence of Crocodiles, the decrease
in number of species of Tortoises, with an increase of Lizards
and Serpents. But none of the Reptiles are remarkable for size,
and are similar in proportions to those now living in the same
region. The author commences with the genus Testudo, which is
represented by five species in the White River beds of Colorado.
They are distinguished by the form of marginal bones, the shape
of gular scutes and other characters. 7: quadratus is the largest,
T. laticuneus the best preserved. Some of the species are only
described from a few bones, because the difficulties of transport com-
pelled the author to select such as were most characteristic, often
leaving the bulk of the specimens behind. The only other Chelonian
is Leidy’s Stylemys nebrascensis.

The Lizards are for the most part founded upon fragmentary
remains. eliosaurus, however, is well preserved. In this genus
the temporal fossa is not roofed over by bone, but is rather small ;
the orbits are large. Two median dermal scutes, which represent
the interparietal and postinterparietal plates, have left impressions
on the parietal bone. The genus is distinguished from Gerrhonotus,
by having had the body covered with bony scutes, which were
rectangular, and arranged in transverse bands, joined at the sides by
minute sutures, and overlapping in an imbricated method. The
hexagonal scutes on the skull are one of its most distinctive charac-
ters; one species is known. Hwxostinus, very imperfectly known,
appears to be related to Peltosaurus, but that genus has the frontal
region much wider, and wants the tubercles along the supra-orbital
border. Aciprion formosum is a Lizard known from a dentary bone,

Tertiary Vertebrata of the West. 513

with closely-packed cylindrical pleurondont teeth, having compressed
crowns with three cusps, the median one large and those at the sides
small. Diacium quinquipedale is founded on a sacral vertebra which
has no trace of a neural spine; and indicates an animal as large as
any of the living Iguanide. The genus Platyrhachis is only known
from vertebra which have the centra much impressed, the neural
spine reduced to a low keel, and the ridge connecting the zygapo-
physes deeply notched, a character which distinguishes these vertebra
from those of Peltosaurus: three species are known. Cremastosaurus
carinicollis is a Lizard known from cervical vertebrae, somewhat like
those of Phrynosoma cornutum, but with relatively small cup and
ball articulations, and a strong rib-like hypapophysis.

There are four genera of Snakes founded on vertebra, which are
the only parts hitherto discovered. Aphelophis is very like the living
genus Charina, though the zygosphene is wider. Ogmophis, known
from two species, is an allied type, distinguished by the ridge which
extends from the parapophysis, and the groove which lies between
that ridge and the middle line of the centrum. Calamagras is a
similar type, but intermediate between the two last named. Neuro-
dromicus has vertebrae which resemble those of one of the Crotalide,
but has no process below the prezygapophysis, and has the hypapo-
physis less robust.

The Mammalia of the White River period are not less numerous
than those of the Bridger and Wasatch rocks, but a great change
has come over the fauna. All the Amblypoda have disappeared,
and there are no representatives of the Tzeniodonta, Tillodonta, or of
the Lophiodonts; while the Creodonta and Mesodonta are rare. No
species of mammal found in these rocks is common to the under-
lying Eocene series. The Miocene species reach a larger average
size, particularly among the Perissodactyla and Carnivora. Life
would appear to have been abundant: for the author states that
many of the species are represented by great droves, and their bones

Peratherium fugax,

form beds of considerable extent. The Marsupialia is represented

by doubtful types, some of which have already been referred to the

Creodonta, and are only placed with the Marsupials provisionally.

Peratherium, though represented by six species, is only known from

the cranium and mandibles. An excellent discussion is given of its

dental characters, with the result that the teeth differ from those of
DECADE III.—VOL. III.—NO. XI 33

514 Reviews—Prof. Edward D. Cope—

Didelphis in the elevation of the median cusps of the superior true
molars into Vs, and in the tubercles of the external series becoming
obsolete. All the species are founded on dental characters.
Mesodectes and Geolabis are referred provisionally to the Creodonta.
The former is intermediate between Leptictis and Ictops, the last
premolar having a single sharp cusp as in the former genus, with an
internal cusp or heel like that of the latter. The cranial characters
are like those of Leptictis, and the molars and some other features
recall the living genus Solenodon. The presternum has a prominent
keel in front, like that of a bird. The cerebral hemispheres and
cerebellum are a little wider than long, and together have a sub-
quadrate outline. The only species known is about the size of the
Hedgehog. Geolabis is only known from crania, from which the
molar teeth are wanting, and the author is uncertain whether it may not
be identical with Domnina. Menotherium lemurinum, though placed
under the Insectivora, is regarded as the first indication of a Lemur
in the Miocene of the United States, and indicates an animal as large
as the domestic Cat. The genus Domnina is referred with some
doubt to the Cheiroptera. It has the posterior external cusp of the
true molar teeth in the form of a crescent, like the anterior cusp,
only rather smaller; both internal cusps are at the summits of strong
ridges : two species are described.

The order Rodentia is represented by no fewer than thirty-one
species and eight genera, of which Sciurus, Hesperomys and Lepus
are found living in the same region, and all the fossil species of Rodents
belong to the three great divisions of the order which now inhabit
North America. The author observes that the feet and teeth in this
order present a succession of changes in structure with time. The
earliest known forms, allies of the Squirrels, belong to the sub-
order Sciuromorpha. In them the trochlear structures of the hume-
rus and tibia are but little developed, they are plantigrade, with five
digits, and the fibula is not co-ossified with the tibia, while their
teeth have nearly always long roots and short crowns, and are rarely
prismatic. An advance on this generalized type is seen in the sub-
order Histricomorpha (which has a single representative in the
Loup Fork beds), in many of its members having a reduced
number of digits and prismatic dentition. In the third suborder,
Myomorpha, the tibia is found co-ossified with the fibula; many
genera have prismatic teeth, some a reduced number of digits, and
a few, comprising the Jerboas, have the metatarsal bones blended
together. Finally, the Rabbits add to these specialized characters
a primitive character in the presence of four superior incisor teeth ;
and the author is disposed to believe that the Rodents are either
direct descendants from the Marsupials, or that the Rabbits may
represent the suborder Tillodonta of the Hocene. The differentiation
of the Rodent suborders, however, must be anterior to the Miocene
period, for the Squirrel tribe has already occurred in the Lower
Eocene. The Myomorpha appear in the John Day beds, but without
prismatic teeth, while the Lagomorpha are typically developed in the
White River beds, and a true Porcupine represents the Hystrico-

Tertiary Vertebrata of the West. 515

morpha in the highest Miocene. There is, moreover, an interesting
affinity between the extinct and living genera, in the circumstance
that all the ancient genera differ from their modern representatives in
the greater constriction of the skull behind the orbits, acecompanied
by an absence of postorbital processes. The genus Sciurus is known
from three species, two of which are about the size of the grey and
red Squirrels of North America. Gymnoptychus appears to be a
Squirrel nearly related to Sciwrus, but differs in having the tubercles
and crests of the molar teeth more complex than in any existing
genus, except Pieromys. There are two species which differ in size
and in proportions of the lower molar teeth.

Meniscomys is another type in which the dentition resembles that
of Pteromys, but differs in the upper molars wanting the re-entering
inflexion of the enamel. Four species are described, which differ in
the length of the roots of the molars, in the character of the dental
crests, and the plications of the inferior molar teeth.

It is observed that there is a suggestive resemblance between
Meniscomys hippodus and Haplodontia rufa, now living in Oregon,
which is indicative of a common origin. This ends the history of
the true Squirrels.

Ischyromys is the type of a distinct family ; for, though it resembles
the Squirrels in dental characters, the infraorbital foramen occupies
the position, at the origin of the zygomatic arch, seen in Porcupines
and Cavies. The superciliary ridge and postorbital process, seen in
most Squirrels, is lost ; and there is a contraction between the orbits,
which approximates towards the Beaver. Beavers are represented by
two species of the genus Castor. C. peninsulatus is about the size of
the large prairie Marmot, and is abundant in the Miocene rocks of
Oregon. C. gradatus is somewhat smaller. Heliscomys vetus is the
smallest Mammal of the White River beds, being about the size of
Mus musculus. Its affinities are open to some doubt; the four
inferior molars have crowns with four cusps in two transverse
pairs and a broad ledge on the external side of the cusps.

The Myomorpha are represented by two families, Muride and
Geomyidee. Humys elegans, of Leidy, is a Rat found in the White
River rocks in Eastern Colorado, previously known from Dakota.
The molar teeth are as large as those of the Norway Rat, but the
muzzle only two-thirds as long, so that the animal was smaller and
more robust. Hesperomys nematodon is a representative of an exist-
ing genus, and indicates a Rat as large as the red Squirrel. The
genus Paciculus, which has three superior molars, differs from Sig-
modon and Neotoma, in having three external inflexions of the enamel,
instead of two, in the upper molars. Entoptychus, known from five
species, is referred to the Geomyide. The molar teeth are four above
and four below, rootless, with prismatic crowns, which differ from
those of Perognathus, in having the enamel loop cut off and isolated.
The skull wants the vacuities and large foramina seen in many
Rodents. 'The bones of the skeleton in general resemble those of the
genus Thomomys. 'The species are defined by the characters of the
superciliary borders, the length of the skull, and width of the pre-

516 Reviews—Prof. Edward D, Cope—

molars. The species are found in the John Day beds of Oregon.
Pleurolicus is another member of the same family. It is represented
by two species, and approximates to the existing genera Heteromys
and Perognathus, from the latter of which the most distinctive ditfer-
ence is the grooving of the upper incisors.

The Lagomorpha is represented by three genera. Palcolagus is a
type which approximates towards Lepus, but it has no postfrontal
process, and the first inferior molar consists of one column, more or less
divided. A cast of the cerebral chamber shows that the olfactory
lobes are large, expanding abruptly from the hemispheres, from
which a constriction separates them. They are wider than long, and
wider than the front of the cerebrum. The brain was smaller than
in the Rabbit, and in the Palgolagus hayden the cerebral hemispheres
are smaller, and the olfactory lobes larger. The number of teeth is
the same as in existing Rabbits, but with age many changes appear,
which at first suggest the characters of different species.

P. haydeni was widely distributed in Dakota, Colorado, and Oregon.
It is thought to have been the progenitor of Lepus sylvatieus, which
now inhabits North America. PP. triplex was rather larger than the
prairie Marmot. Lepus emisianus is the only species of the genus
found in the John Day River beds. It is distinguished by the free
short postorbital processes, which are narrower than in LE. auduboni,
and behind these processes the cranium is narrower. The mandible
has the form of L. sylvaticus, which the animal resembled in size.
The remainder of the volume is devoted to the Carnivora.

From the views already developed by the author, it is interesting
to find the Carnivora distinguished as clawed Mammalia with trans-
verse glenoid cavity of the squamosal bone, confluent scaphoid and
lunar bones of the carpus, and well-developed cerebral hemispheres.
A good deal is made of the cerebral hemispheres, because some
Insectivora possess a united scapholunar bone. Hence the crucial
fissure of the hemispheres, which is present in all Carnivora, except
one or two of the Melinz, becomes as important a characteristic as
the absence of the parieto-occipital, and calcarine fissures. The
author makes two primary divisions of the order: first, Hypomycteri,
in which the external nostril is occupied by the complex maxillo-
turbinal bone, while the ethmo-turbinal bones are confined to the
hinder part of the nasal fossa, and the inferior ethmo-turbinal is of
small size; and, secondly, the Epimycteri, in which the external
nostril is occupied by the inferior ethmo-turbinal and the reduced
maxillo-turbinal. The Hypomycteri stand next to the Pinnipedia,
since the maxillo-turbinal bone has the same anterior development
in that group. The division of the groups into families depends
upon the presence of sectorial teeth, which are defined as having at
least two external tubercles, and by the flattening and emargination
of their continuous edges, the sectorial blade is formed. Other
characters are found in the number and form of the molars, the
presence or absence of an alisphenoid canal, the character of the otic
bulla and the number of toes.

The Canides were abundant in the Miocene of North America, but

Tertiary Vertebrata of the West. 517

in the lower and middle portions of the deposit the genera are allied
to Canis, while in the Upper Miocene or Loup Fork beds the genus
Canis prevails. Hight genera of Dogs are here represented by
twenty-five species. Amphicyon of Lartet is known from three
species. A. cuspigerus is not larger than the Kit Fox; A. harts-
hornianus is about the size of a Coyote, and A. vetus rather larger.
Temnocyon has four species, and is distinguished from Canis by the
presence of a cutting edge on the superior face of the heel of the
inferior sectorial, in place of a double row of tubercles surrounding
a basin. This keel is a repetition upon that tooth of the heel seen in
the posterior premolar teeth of many Carnivora. The genus ap-
proaches most closely to the French form Cynodictis crasstrostris.
On Temnocyon corypheus the author observes that the dimensions
were about those of the Canis latrans, but the face was short. The
brain-case is smaller than in the Coyote. The genus Galecynus
of Owen is well represented by four species, which are characterized
by the relatively small size of their sectorial teeth. The internal

tubercle of the inferior sectorial is more largely developed than in
the later species of Dogs, and thus approaches some of the Viverride.
The genus is separated from Canis by the presence of the epitrochlear
foramen of the humerus, a character shared with Amphicyon and
Temnocyon. G.gregarius is only about half the size of the Red Fox.
G. geysmarianus was about the size of Mustela pennanti : it stood lower
on the legs than a Fox, had a body as slender as the most vermiform
of Weasels, and a tail as long as in the Ichneumons. G. lemur is the
smallest species yet discovered in the Miocene of Oregon. Enhydrocyon
has the canine type of dentition, but in the form of skull resembles
the Polecat and Otter: but one species is known, which was probably
as large as the Coyote.

518 Reviews—Prof. Edward D. Cope—

Oligobunis crassivultus differs from Icticyon venaticus of Brazil, in
the greater development of the inner part of the upper tubercular
molar, while the tubercular molar of the lower jaw is much less
developed. Hycnocyon differs from Oligobunis in wanting the first
premolar and the second molar teeth in both jaws. Bunelurus is
allied to Putorius and perhaps to Gulo, but is distinguished by the
form of its tubercular tooth, which is a cutting tooth without cusps
or tubercles.

In the higher genera of the family Nimravide, the dental characters
are like those of the Felide, but among the lower genera the number
of molar teeth increases anteriorly in the upper jaw, and at both ends
of the series in the lower jaw; though the number of true molars
never exceeds one above and two below. Hight genera are at present
grouped in this tribe; and they show modifications in the reduced
number of molars, the enlarged size of the upper canines, smaller
size of the lower canine, conical form of the crowns of the incisors,
addition of a cutting lobe to the anterior base of the upper sectorial
tooth, the obliteration of the inner tubercle of the lower sectorial in
which the heel is lost, and in the development of cutting lobes on
the hinder borders of the larger premolar teeth.

Nimravus gomphodus.

Some of these genera may belong to the Cryptoproctide ; but
until the number of digits is known in all the forms, this point
cannot be determined. Archelurus debilis was an animal having
much the aspect of existing Cats, but with more slender feet, narrower
head, and greater convexity of the region between and behind the
eyes. The prehensile organs of the feet, and teeth, were less robust.
It was about the size of the American Panther. There is no cutting
edge to the front of the canine tooth, and the posterior edge is not
serrated. The sectorial teeth have a long narrow form, the superior

Tertiary Vertebrata of the West. 519

tooth has no anterior lobe, and the inferior tooth has no internal
tubercle, but the heel is present. Nimravus is known from two
species nearly allied to Archelurus, but distinguished by wanting the
anterior premolars in both jaws, while the large canine in the upper
jaw is denticulated. In dental formula and characters, it resembles
Hoplophoneus, with the addition of a tubercular inferior molar tooth
There is no evidence to show the length of the body. The canine
teeth were probably exposed; and, as penetrating weapons, are un-
rivalled among carnivorous animals. ‘Three species of Dinictis are
described ; it is a primitive sabre-tooth genus, closely connected with
the false sabre-toothed group. The superior canine is long and com-
pressed, and rests against an inferior marginal flange of the mandible,
whose surface is divided from that of the symphysis by a strong
angle. Pogonodon connects Dinictis with the higher sabre-toothed
genera, but wants the tubercular lower molar of Dinictis, while it
possesses the second inferior premolar which is wanting in Hoplo-
phoneus. The species are the largest of the North American sabre-
tooths.

SSS

Pogonodon platycopis.

P. platycopis is equal to the largest Drepanodon, and only inferior
in size to Smilodon. The skull is equal in size to the largest Brazilian
variety of the Jaguar. The molar teeth are rather small, the second
sectorial is primitive, and peculiar in its robust heel. Hoplophoneus
is a genus with the dental formula of Drepanodon and the true Cats,
but which retains the primitive form of the sectorial teeth in the
lower jaw. ‘The type-species was as large as the Canadian Lynx,
with long and slender upper canines. Three species are described.
Here Book i. terminates, leaving the remainder of the John Day
fauna, as well as that of the Pliocene period, for description in the
second book of volume iii. The beautiful plates by which the text
is illustrated reflect credit upon the artists, as well as upon the

520 Reviews—Prof. Cope—Tertiary Vertebrata of the West.

Government Department which issues them, and will always make
this work one of the standard landmarks in the history of Mammalian
life.

As we close the book, it is with an earnest desire that the same
devotion of the Department of the Interior to the interests of Science
which has placed this magnificent contribution before the world,
may at no distant date be able to secure the publication of the
remainder of the author’s contributions to a knowledge of the fossil
Vertebrata of the United States Territories. It is, we believe, known
that the materials for these histories have been in part gathered by
many adventurous explorations, and not inconsiderable expenditure
by the author; and that the United States Government has already
spent large sums of money in preparing plates to accompany the
text, which remains in their hands unused. We venture to believe
that the gratitude which scientific men feel for the work already
published, emphasizes the hope that it may be speedily completed ;
for it is one of the most valuable contributions to knowledge ever
made by an individual, and its publication reflects honour on the
nation.

When we survey the enormous range of Professor Cope’s
work, which has enriched every department of the Vertebrata with
new materials, often interpreted with strikingly original conceptions,
it is impossible not to bear witness to the magnitude of labours
which derive their chief value from the genius which directs them.
Shortcomings are easily detected, but when balanced against valuable
achievements, may well be passed over. Most of the great writers
on similar subjects in the Old World have secured honour by select-
ing for their labours, materials more or less perfect, which left no
doubt on their interpretations. Obscure and difficult specimens have
been laid on one side until later discoveries or maturer powers in the
writer, removed the obscurities. Professor Cope, on the other hand,
has never shrunk from any difficulties which his materials presented.
A tooth, or a fragment of a mandible, or an ankle bone in his hands
has revealed a new type of life. The discoveries which other men
have waited for, for half a lifetime, he has utilized as the fossils
successively came to hand, so that the nomenclature of his species
has changed, and the interpretation of organic structures has
gradually unfolded results of increasing value. There is hardly any
writer whose work, looked back upon after a quarter of a century,
does not show that, here and there, interpretations might be
improved. Such improvements Prof. Cope has been able, in many
cases, to make in a much shorter time by unceasing industry, and
vigilance to seize new truths as they appeared. Work like this,
upon fragmentary fossils, appeals with most powerful interest to
those whose knowledge enables them to appreciate this daring faith
in scientific methods, which is hedged round with reasons for the
results proclaimed. And it is only when these earlier judgments are
in so many cases sustained by later work on better specimens, that
the discriminating insight manifested justifies such methods of work.

The results at which the author has arrived in this first book of

Reviews—Dollo’s Eocene Chelonians. 521

volume iii. are modestly stated by himself under fifteen heads, in-
cluding such matters as the discovery of the Laramie genus Champso-
saurus in Tertiary beds, the discovery of Tertiary allies of Plagiaulax,
the discovery of five families and many genera of Creodonta, the
discovery of the Periptychide, the Meniscotheriide, the Phenaco-
dontidee, the discovery of characters of the suborder Condylarthra,
the characters of the Pantolambdidee, of the suborder Taligrada,
of the Anaptomorphide, the reconstruction of Hyracotherium and
Hyrachus, the discovery of many Marsupials in the Lower Miocene,
and of ancestors of the Cats and Dogs; to which may be added the
description of three hundred and forty-nine species, all discovered by
the author, except thirty-two. But although the present volume may
not claim to have first set forth the greater results to which these are
but some of the stepping-stones, we may point to the method of com-
parison of the fossil types with each other and with living genera as
indications of the sources of knowledge by which the grouping of
families and genera has been produced, which has given rise to new
ordinal and sub-ordinal groups and improved classifications. The
conception of the Bunotheria will always remain one of the most
interesting of these results, because it is the first attempt to apply
the principles of evolution to Mammalian classification in its larger
grouping. The Amblypoda introduces a new hoofed type of life,
which was already elaborated by the descriptions of Coryphodon,
given in Lieutenant Wheeler’s Survey in 1877. These and a
multitude of minor innovations in classification are the fruits of new
knowledge gathered partly from animals still living, partly from
the wonderful organisms discovered in United States rocks. It
is not too much to say that the light thus thrown upon the Mammalia
as a whole, is more instructive as to the laws of life, and the condi-
tions under which the component structures of animals have varied,
and been evolved, than the insight gained during the same time by
the study of Embryology. This harvest of fruit from the past may
justify the confidence that in the history of fossil life, which has yet
to be told by the paleontologist, the significance of the varied
organization of existing animals will be demonstrated.

H. G. SEELEY.

IL—M. L. Dotto on NEW CHELONIANS FROM THE EocENE OF
Bexetum.!

N these two memoirs the learned Assistant Naturalist to the Royal

Belgian Museum of Natural History describes two new genera

of Chelonians which are of very considerable interest, and also pub-

lishes a synopsis of the classification of the order, which is a modifi-
cation of that proposed by Prof. E. D. Cope, of Philadelphia.

1 ¢ Tes Chéloniens du Bruxellien (Eocéne Moyen) de la Belgique,’’ Bull. Mus. R.
Hist. Nat. Belg. vol. iv. 75-86, pls. i. ii. (1884), ‘‘ Les Chéloniens Landeniens
(Eocéne Inférieur) de la Belgique,” Idid. pp. 129-141, woodcuts.

522 Reviews—Dollo’s Eocene Chelonians.

The proposed classification is as follows :

Order CHELONIA.
Suborder 1. PRocurnonta.—Sect. MacELoGNaTHaA.
2. HucHELoNIAW— ,, 1. ATHECH.
» 2. THECOPHORA.
Subsect. 1. PLEvRopIRA.
2, Cryptopira. a. Dactyloplastra,
b. Clidoplastra
c. Lysoplastra.

The first suborder is a purely hypothetical one, and is formed for
the ancestors of the known forms which are presumed to have been
furnished with teeth. Apart from the general question whether
it is advisable to overload scientific nomenclature with terms for
hypothetical groups, it appears to us that in this instance the author
would have exercised greater discretion if he had refrained from
proposing this suborder, since, as Prof. A. Newton has recently ©
shown in the case of the Birds, it does not necessarily follow that the
possession of teeth by the more primitive forms of a group entails
the separation of such forms from the more specialized groups which
have lost these organs.

The Euchelonia comprehends all known members of the order;
the section Athecee being formed for Sphargis and its fossil allies ;
while the section Thecophora includes all other known forms. The
first subsection (Pleurodira) of the latter embraces the existing
family Chelydide and certain Mesozoic forms such as Plesiochelys.
The existing members (e.g. Chelys, Platemys, and Hydraspis) of this
subsection, which is characterized by certain features of the pelvis,
and the presence of an intergular plate, are now entirely confined to
the Southern Hemisphere; and it is interesting to note that while
Platemys is represented in the Lower Kocene of England, a member
(H. Leithi) of the South American genus Hydraspis has been described
by Dr. Gray from the Hocene of Bombay. In the Cryptodira, which
may be now regarded as the Chelonians of the Northern Hemisphere,
are included all the remaining members of the order. In the first
(Dactyloplastra) of the three groups into which this subsection is
divided, M. Dollo recognizes four families,—the Chelonide, Propleur-
ide, Trionychide, and Chelydride. 'The second group (Clidoplastra)
is divided into the Pleurosternide, Baénide, Adocide, Emydide,
Cinosternide, and Testudinide; while the third (Lysosterna) com-
prises only the Cistudinide (e.g. Cistudo, Terrapene, etc.).

We are by no means sure whether such a complicated division of
the Cryptodira is advisable, especially as some English systematists
(e.g. Dr. Sclater’) include the Cistudinide, Cinosternide, Chelydride
(e.g. Chelydra and Macrochelys or Macroclemmys), and apparently
the Baénide (i.e. if Dermatemys be classed in the latter) in the
Emydid@g, and do not consider the characters on which M. Dollo
relies as of more than generic value. This is, however, a matter on
which every scientist who has studied the group is entitled to use
his own opinion.

Turning now to the new forms described by M. Dollo, perhaps

1 See “ List of Animals in Gardens of Zool. Soc.’’ 8th ed. pp. 561-571 (1883).

Correspondence—Dr. H. J. J. Lavis. 523

the most interesting is the one from the Bruxellien, to which he
applies the name Pseudotrionyx, and classes in the Chelydride. This
form is characterized by the absence of horny plates and the presence
of a scute-sculpture, like Trionyx, but was apparently furnished with
a complete series of marginal scutes, while the plastron, although only
imperfectly united to the carapace, is much more complete than
in the latter. This genus evidently forms a connecting link
between the typical Trionychide and those Tortoises in which the
shell is complete; M. Dollo attaches more weight to the apparent
completeness of the marginal scutes than to the sculpture of the
scutes and the absence of horny plates, and therefore separates
the genus, together with Anostira and Apholidemys of Leidy from
the Zrionychide; but we cannot help thinking, from the variations
in the former respect between Trionyx and Hmyda, that the argu-
ments are at least as strong in favour of the opposite view, and for
taking the presence of horny plates as a characteristic of the
Emydida, in the sense in which that term is used by Dr. Sclater.

The second genus, Pachyrhynchus, is from the Lower Eocene, and
is referred to the Chelonide; it is represented not only by the
typical Belgian P. Gosseleti, but probably also by the three forms
from the London Clay described by Professor Sir R. Owen
under the names of Chelone longiceps, C. planimentum, and C.
irigoniceps. The genus is distinguished from Chelone by the great
length of the mandibular symphysis; by the triangular form, thick-
ness, and slight depression of the palate; the depth of the latero-
temporal notches; the separation of the nasals ; and by the posterior
nares being separated from the anterior ones by long narrow
channels, and by opening on the posterior third of the basal aspect
of the cranium. These differences M. Dollo is inclined to regard as
of rather more than generic value.

M. Dollo is to be congratulated on this paper, and especially on
the careful diagnosis of characters distinguishing all his work.

It, Ibe

CORRESPONDENCE.

=

THE VOLCANIC ERUPTION OF NEW ZEALAND.

Srr,—Almost every geologist will have read the deeply interesting
accounts and speculations by Mr. Archibald Geikie and Dr. Hector
in “Nature,” and of Mr. R. Etheridge, jun., in this Macazinn. As
the district affected is one likely to be subjected to a careful inves-
tigation, may I be permitted to draw attention to a few facts of
important bearing on vulcanological science that should be cleared
up. In my paper on the geology of Vesuvius and Monte Somma
and in other communications, it was pointed out that after a long
state of quiescence of a volcano, the subsequent eruption should be
of the explosive or plinian type. That is to say, the stony products
should consist essentially of pumice due to the length of time that

524 Correspondence—Dr. H. J. J. Lavis.

the magma had remained in contact with aquiferous strata, gradually
absorbing water, and consequently the impossibility of the outflow
of lava until all the water-saturated magma has been ejected. In
relation with this the presence of the three divisions of the ejecta-
menta ; the lowest or first being a very vitreous pumice, except for
the presence of pre-eruptive minerals such as the felspars, amphibole,
mica, and magnetite of first consolidation; the second or middle
division being far more microlithic, with the presence of pyroxene or
other eruptive or post-eruptive formed minerals; and the third or
upper division consisting of ash due to the loss of cohesion within
the magma in consequence of the advanced stage of conversion of
the glassy part into “formed ” or individualized matter.

In many tufas, and especially those formed from the third or upper
division of the products of a plinian eruption, or of any pumiceous
ash, there are an abundance of little pisolitic concretions of great
perfection. Scrope has suggested drops of water falling in the dust as
the cause of their production. To me they seem rather a segregation
similar to what occurs in the felspathic and siliceous glazing cream
in pottery manufacture ; but there is still much doubt, and observation
would be of much value if made on the new ash, as we do not know
whether they are formed immediately, or after long exposure and
soaking by moisture. One thing should be remembered, and that
is, that a few small ones may be inclosed in a larger one, which is
not compatible with Scrope’s theory.

The next point is the vesicular structure in ashes, which often so
well mimics that of lava, that in old decomposed rocks much doubt
may exist as to whether a given mass may be a lava or a tuff.
I think the drops of rain, suggested as an explanation of pisolites, is
the real influence at work in producing these vesicular cavities.

Next, it would be interesting to know whether new cones (or more
properly crater-rings) have been formed within the craters of
explosion towards the end of the eruption.

Observations on the proportion of the essential, accessory, and
accidental ejectamenta should be made in each of the subdivisions of
the deposits, and at. different distances from the centres of explosion.

Observations of the green and dry wood buried in the pumice
would clear up the question as to whether the peculiar lignitization
or carbonization to be seen at Pompei, not only in wood, but also in
bread, fruit, cloth, grain, etc., is due to burning, baking, or subse-
quent decomposition. In Pompei neither glass nor lead was fused
where buried by the falling pumice. This I have shown to be due
to the low temperature of the pumice from the loss of heat in
converting liquid or dissolved water into vapour on the relief
of pressure during the eruption.

Lastly, search should be made for fulgurites, which have been met
with at Pompei.

H. J. Jonnston-Lavis.

Correspondence—Ur. E. Wethered—Mr. A. S. Woodward. 525

THE PEA-GRIT OF LECKHAMPTON HILL.

Str,—In the Quarterly Journal of the Geological Society just
issued, there is a paper by my friend, Mr. Witchell, of Stroud, on
“The Basement Beds of the Inferior Oolite of Gloucestershire.” !
The reasons for writing the paper are given under two heads, but
I am only now concerned with the first. Mr. Witchell says: 1.
“ That the beds called ‘Pea-grit’ in the Leckhampton section by Hugh
Strickland, which name was adopted by Dr. Wright and the Geolo-
gical Surveyors, included in that term—erroneously as I think—all
the beds occurring between the Pea-grit proper, and the Cephalopoda
bed of the sands, which beds are shown in some sections to be more
than thirty feet in thickness.”

Further on Mr. Witchell tells us that the “Pea-grit” and Base-
ment Beds at Leckhampton Hill “are described as Pea-grit in the
published works referring to them. Now, if Mr. Witchell will refer
to the late Dr. Wright’s paper,® ‘On the Paleeontological and Strati-
graphical Relations of the so-called Sands of the Inferior Oolite,” he
will find that in the section of Leckhampton Hill the lower beds of
the Inferior Oolite are referred to as Pea-grit and ferruginous oolite.”
That Dr. Wright was fully aware of beds of oolitic structure beneath
the “ Pea-grit,” and which he recognized as distinct from the par-
ticular bed bearing that name, is shown by his section of Cleeve
Hill,* in which he gives the following :—

ft. in.
Rea -oritinamet tcc sen tte Meera 2s 0
Coarse ferruginous oolite 009-606.

Epwarp WETHERED.

NOTIDANUS AMALTHET, OPPEL.

Srr,— During a recent examination of the fossil Vertebrates in the
Whitby Museum, which I have been enabled to make through the
kindness of Mr. Martin Simpson, I have been fortunate enough to
meet with the Liassic tooth mentioned by Tate and Blake as referable
to Notidanus Amalthei. 'This specimen, it will be remembered, was
not forthcoming at the time of publication of my contribution to the
Paleontology of the Notidanidze (antea, p. 208), and it may therefore
be interesting to add a brief note upon the features it presents.

The fossil consists merely of a single laterally-compressed cone,
scarcely two millimetres in height, with a very minute denticulation
at the base of one edge, and fixed upon a fragment of a root. The
cone has an enamelled surface, and the one side is almost plane,
while the other is strongly convex ; and the appearance of the tooth
is certainly suggestive of other cones having been broken away from
the one that remains. There can be scarcely any doubt, indeed, that
the specimen belongs to a Selachian genus, and it bears much

1 QJ.G.S. vol. xli. part 3, No. 167, pp. 264—270. * Ibid. p. 264,

3 Tbid. vol, xil. p. 295, 1856.

4 Proc. Cotteswold Club, 1869, ‘‘ Correlation of the Jurassic Rocks of the Cdte
d’ Or and the Cotteswold Hills.’’

526 Obituary—Dr. Harvey B. Holl.

more resemblance to a dental fragment of Notidanus than the
Swabian fossil described by Oppel, as far as the latter’s figure will
enable one to judge. It does not agree with the teeth of Palzospinau
or any other Liassic Shark I have had the opportunity of studying,
and Tate and Blake’s determination is very possibly correct; but
more satisfactory evidence must still be awaited before there is
absolute certainty of the presence of Notidanus among the early
Jurassic fauna. A. SmitaH Woopwarp.

ENTOMOSTRACA IN THE RHATICS.

Str,—In the Gxronocicat Magazine, May, 1886, p. 203, a slight
error occurs in Mr, J. 8. Gardner’s interesting paper, in stating that
“‘the valves of a species of Cyclas abound in the Rhetics.” This
should have been either Candona or possibly Cypris; the latter may
be after all correct, as it is associated with the freshwater aquatic
Moss, Naiadites. The supposed Cyclas has been determined to be
Estheria, a brackish-water Crustacean, though Sowerby stated it to
be Cyclas, when my work on Fossil Insects was published. In
the Note (2) at the bottom the reference should have been not
to the Hstheria bed in particular, but to the Rhetics in general
(in which the former is included), which may be considered to be
junction or passage beds between the Trias and the Lias.

P. B. Bropte.

OS DA WEASE ae

HARVEY BUCHANAN HOLL, M.D., F.G.S.

Born 28TH Szpremper, 1820; Diep llrn Sepremper, 1886,

Tuts able geologist and paleontologist was son of the late William
Holl, Hsq., formerly of Worcester. After passing through Dr. Walter’s
School at Worcester, he entered the Medical College in Birmingham.

During this period of Harvey Holl’s career, when he was only about
17 years of age, he became acquainted with Sir Henry de la Beche,
and was invited by that distinguished geologist to accompany him in
a geological reconnaissance through Devon and Cornwall. It was
probably owing to this expedition (which extended over some six
months) that young Holl became confirmed in his geological tastes,
and for a time was led entirely to abandon his medical studies.

From the good opinion which Sir Henry de la Beche formed of
Holl’s work in the field, he recommended the youthful geologist to
his friend Professor Rogers, of Philadelphia (who was seeking an
assistant), and Harvey Holl started off to join his new chief and
take a part in the Geological Survey of Pennsylvania. In this
interesting region, Holl remained for about three years, and spent a
year longer in the United States geologising on his own resources.

Upon his return to England, Holl entered as a student at St.
George’s Hospital, and successfully passed the Royal College of
Surgeons in London. Jn 1859 he graduated as M.D. at King’s
College, Aberdeen.

Obituary—Dr. Harvey B. Holl. 527

On the breaking out of the Crimean War, Dr. Holl was appointed
one of the Senior Civil Surgeons to aid the military staff, which was
totally inadequate to the heavy strain laid upon it by the first year’s
severe trials and sufferings. He remained abroad until the end of
the campaign, serving partly in the Crimea, but most of the time in
the hospital at Scutari. On his return after the conclusion of peace
with Russia, he settled for some years as a medical practitioner in St.
George’s Square, Pimlico.

Dr. Holl was remarkable for his extremely reserved and retiring
habits and formed consequently but few friendships. Yet he was
by no means a man of small ability. As a medical practitioner he
might have attained great eminence, but he never was ambitious
of fame.

An earnest student of Cryptogamic Botany, he has left some forty-
seven volumes of carefully collected British Lichens, all arranged
and named by himself. He was also a liberal donor to the Botanical
Department of the British Museum.

As a geologist and paleontologist, he displayed great power,
and his papers always met with high appreciation in the Geological
Society. During his field-excursions he had formed a considerable
collection of British fossils, among which were numerous species
and varieties of the Silurian genera Beyrichia, Primitia, and their
allies, in very perfect preservation. As a good microscopist, clever
draughtsman, and careful observer, he willingly and ably co-operated
with Professor Rupert Jones in the study and description of the older
Ostracoda. Within this year even he warmly assisted in the work,
and notwithstanding his declining health, he supplied new sketches
and notes of his favourite little fossils.

Dr. Holl was well known among the leading members of the
Hereford, Woolhope, Malvern, and Cotteswold Natural History
Field Clubs, and was himself frequently present at their meetings
and excursions.

Although an excellent paleontologist, he will probably be most
widely known and remembered as an able and experienced geologist,
and the papers which will best be recollected are those on the Geolo-
gical Structure of the Malvern Hills, in which area he made great
advances on the work of Prof. Phillips; and his memoir ‘‘On the
Older Rocks of South Devon and Hast Cornwall,” in which he
exemplified the excellence in method of his early teacher in Devonian
geology, Sir Henry de la Bechie.

T’o those who had the pleasure to know him, and were able to
penetrate beneath his ordinary reserve, he will be remembered as
a genial and pleasant comrade, full of scientific information, and
lasting in his attachment to his friends.

Dr. Holl was elected a Fellow of the Geological Society in 1862,
and having about this time relinquished his practice, he removed to
Tower Lodge, The Link, Malvern, where he again took up his
favourite geological studies, and in 1863 communicated a paper to
the British Association “On the Metamorphic Rocks of the Malvern
Hills.” *

1 Brit, Assoc. Report, 1863 (part 2), pp. 70—73.

528 Miscellaneous—Memorial to Dr. Davidson.

Jn the same year he also read a paper before the Geological Society
of London, “On the Correlation of the several Subdivisions of the
Inferior Oolite in the Middle and South of England.” ?}

From Malvern Dr. Holl removed to Elderslie House, London
Road, Worcester, and thence to Little Perdiswell, Worcester, where
he resided until about the end of 1884, when, for the sake of his
health, he removed to Cheltenham, living first at 3, Oriel Villas, and
lastly at 1, Derby Villas where he died after three weeks’ illness,
resulting from heart disease.

Besides those already named, the following additional papers are
credited to Dr. Holl, namely :—

3. On the Geological Structure of the Malvern Hills and adjacent District. Quart.
Journ. Geol. Soc. 1864, vol. xx. p. 413, and vol. xxi. 1865, pp. 72-102. Phil.
Mag. 1864, vol. xxvii. p. 243.

. On the Pre-Cambrian Rocks of Central England. Brit. Assoc. Rep. 1865, vol,

xxxyv. (Sect.), pp. 59-62; Grou. Mac. 1865, Vol. Il. pp. 563-565.

. Goniophyllum pyramidale, Hisinger. Grou. Mac. 1866, Vol. III. pp. 430-431.

On the Geological Position of the Crystalline Rocks of the Malvern Hills,

Woolhope Field Club Trans. 1866, pp. 273-274.

. On the Older Rocks of South Devon and East Cornwall. Quart. Journ. Geol.

Soe. 1868, vol. xxiv. pp. 400-454 ; Phil. Mag. 1868, vol. xxxvi. p. 158.

. Notes on Fossil Sponges. Gurou. Mac. 1872, Vol. IX. pp. 309-315, and 343-352.

. The Epitheca in Fossil Sponges. Monthly Microsc. Journ. 1872, vol. viii. pp.

141-142.

He was also joint-author with Prof. T. Rupert Jones, F.R.S., of
the following papers, viz. :—

1. Notes on the Paleozoic Bivalved Entomostraca. No. VI. Some Silurian Species
(Primitia). Ann. and Mag. Nat. Hist. 1865, vol. xvi. pp. 414-425.

9. Notes on the Paleozoic Bivalved Entomostraca. No. VIII. Some Lower
Silurian Species from the Chair of Kildare. . Op. cit. 1868, pp. 54-62.

3. Notes on the Paleozoic Bivalved Entomostraca. No. IX. Some Silurian Species,
Op. cit. 1869, pp. 211-229.

4, Notes on the Paleozoic Bivalyed Entomostraca. No. XX. On the Genus
Beyrichia and some New Species. Op. cit. 1886, pp. 337-363.

5. Notes on the Paleozoic Bivalved Entomostraca. No. XXI. On some Silurian
Genera and Species. Op. cit. pp. 403-414.

OOH I an

MIiSCHUiGMAN HOUS.

Memor1at to Dr. Tomas Davipson, LL.D., F.R.S.—Thursday
was the first anniversary of the death of Dr. Thomas Davidson.
The proposed memorial to his memory in the Brighton Museum will
take the form of a life-sized medallion in marble, framed in alabaster.
The work has been undertaken by Mr. T. Brock, A.R.A., through
the kind offices of Mr. Edward Armitage, R.A., an old friend and
former fellow Art student of Dr. Davidson’s in the ateliers of Paul
de la Roche. Mr. Armitage has contributed £20 to the “ Davidson
Memorial Fund,” and his advice and assistance have been of great
service to the Committee and Hon. Secretaries.—Brighton Herald,
Oct. 16, 1886.

1 Quart. Journ. Geol, Soc. vol. xix. (1863), pp. 70—73.

Grou. Mac., 1886. Dsewvoys; MUNG e Wendy IOUS JRL. SANG

Fig 1. X 12 Diam. Ge, 2B, S< 22 IDEN.

Is, 3 >< 28 IDyievone Wigs Als Sk Ba) ID iano.

Wile Go be we IDyiaven. Io, (= SK We IDiaan.

STRUCTURE AND ORGANISMS IN CARBONIFEROUS SHALES AND
LIMESTONES,
FOREST OF DEAN.

Photo-Zinco. Waterflow and Sons Limited,

ian
eae
; oe

Grou. Mac., 1886. DECADE ITS Wor hier Ove

Fig. 7. 22 Diam. Pigs, Bs 3< 2p IDiayrn

Fig. 10. X 22 Diam.

. Fig. 11. X 24 Diam. Pigs 125 ><) 22) iam

STRUCTURE AND ORGANISMS IN CARBONIFEROUS SHALES AND
LIMESTONES,
FOREST OF DEAN.

Photo-Zinco + Wratovlian And Sane limited eee

THE

GEOLOGICAL MAGAZINE.

NEW SERIES?! “DECADE Ny VOLES “tlk
No. XII—DECEMBER, 1886.

(@ nS 0 KS oe aN ye Bey ee = op el ee =
a
I.—On THE STRUCTURE AND ORGANISMS OF THE Lower Limn-
STONE SHALES, CARBONIFEROUS LimESTONE AND Uppsr Lims-
STONES OF THE Forest or Dean.

By Epwarp WeETHERED, F.G.S., F.C.S., F.R.M.S.
(PLATES XIV. & XV.)

{IR ANDREW RAMSAY has described! the Coal-fields of the
Forest of Dean, Somersetshire, and Bristol as outliers of the
great Coal-fields of South Wales; there is, however, a marked thinning
out in the thickness of the Carboniferous rock in the Forest of Dean
as compared with the development of those rocks in South Wales
and Bristol. At Clifton, near Bristol, the total thickness of the
Carboniferous Limestone is about 2900 feet. at the northern end ot
the Forest of Dean Coal-field it is about 600 feet.

Professor Edward Hull has given® a comprehensive idea of the
several divisions of the Carboniferous series as represented by typical
developments in England. He has divided the series into three
divisions, which he has again subdivided into stages marked by
letters. The following is Professor Hull’s classification, but I have
omitted details which do not concern this paper.

Tue Brirish CARBONIFEROUS SERIES. BrEps In DESCENDING ORDER.

Essentially Fresh- ( Stage G. Upper Coal-Measures.
water and
Estuarine Beds. Stage F. Middle Coal-Measures.
(Stage E. Gannister Beds (Phillips), or Lower Coal-measures.
Essentially | Stage D. Millstone-grit Series. Coarse grits, flagstones, and
Marine. < shales, with a few thin coal-seams.
| Stage C. Yoredale Series. Shales and grits, passing down-
wards into dark shales and earthy limestones.
Stage B. Carboniferous Limestone. Massive Limstone, pass-
ing northwards into several beds, with intervening

Essentially Marine, ¢ shales and grits.
except Stage A | Stage A. Lower Limestone Shales and Calciferous Sandstone.
in Scotland. (Ul Dark shales in some places; grits, conglomerates,
and red sandstones and shales in the northern
district.
Bycehater Beda: { Base. Upper Old Red Sandstone. Yellow sandstones and
conglomerates.

In the Forest of Dean stage A is represented resting on a succes-
sion of many-coloured calciferous sandy beds and shales, very much

" Physical Geology and Geography of Great Britain, fifth edition, pp. 34, 35.
Also, Mem. Geol. Survey, vol. i. p. 303. :
* Quart. Journ. Geol. Soc. vol. xxxiii. p, 615, 1877.

DECADE III.—VOL. III.—NO. XII, 34

530 FE. Wethered—Organisms in Carboniferous Limestone.

like what Prof. Hull describes as occurring in “northern districts.”
They were first described by Mr. W. C ©. Lucy, F.G.S8.,/ and later on
by myself.? Stage B is represented by the Carboniferous Limestone,
or middle series, Dut appears to be quite void of fossil remains, which
fact I shall refer to later on. Above stage B, Professor Hull gives,
as stage OC, the Yoredale Series, and he describes them as ‘‘shales and
grits, passing downwards into dark shales and earthy limestones.”
In the Forest of Dean we have beds very similar in a lithological
point of view to those which Prof. Hull described; but in my pre-
vious paper, just referred to, objection was taken to my classing
these upper limestones as the representatives of the Yoredale Series.
I shall not in this paper discuss that question, but I shall show that
these upper limestones are different from the Carboniferous Lime-
stone, and are quite as much entitled to be grouped separately as the
Lower Limestone Shales. To condense what I have said, the Car-
boniferous Limestone series in the Forest of Dean consists of the
following divisions :—

Approximate thickness in feet.

Upper Limestones (occupying position of Yoredale Series

of the North of England.) Stage C. 000 p06 116 3
Carboniferous Limestone proper. Stage B. 305 250 360
Lower Limestone Shales. Stage A. ee a0 ad 130

Lower Limestone SHALES.

The calciferous sandy beds, which succeed Old Red Conglomerate,
gradually become more calciferous in ascending order, till at last
a series of quarries are found opened out in a succession of limestones
and shales. Some of the latter are bituminous, a feature to which -
I have called attention in a paper communicated to the Cotteswold
Club. The lowest of these beds are exposed in two quarries on
either side of the deep cutting near Drybrook, from which the
following specimens were selected (see Plates XIV. and XV.).

No. 1 (Plate XIV. Fig. 1).—A crinoidal limestone which gave the
following result on chemical analysis :—

- _., ( Insoluble residue (oan) ae a0 304 20 3°68
Lasdlleble oa gal \ Organic matter... a3 50 ona Bee 3°30
Carbonate of Lime.. oo so ase ... 90°40

goss ho Carbonate of Magnesia be sia 500 ie 2°38

Sole ble tn au Carbonate of Iron... 300 308 aon aa “42,
Alkalies 2008 500 ae at 200 trace

100°18

The sand is little else than grains of quartz as large as -01 of an
inch in diameter, but average about ‘0038. The larger ones are
rounded, the smaller ones angular. The absence of alumina in the
analysis is a feature to be noticed, as in the analysis of a crinoidal

1 Proc. Cotteswold Club, 1866.

2 Quart. Journ. Geol. Soc. vol. xxxix. p. 212, 1883.

3 I put the Upper Limestone at 116 feet, but it is impossible to measure the thick-
ness accurately at present. The Wilderness Portland Cement Company, however, is
making a cutting, near Mitcheldean, with the object of ascertaining the thickness, as
the limestone produces a good cement.

4 << On the Occurrence of Spores of Plants in the Lower Limestone Shales of the
Forest of Dean,’ Proc. Cotteswold Club, 1883—1884, pp. 168—173.

E. Wethered—Organisms in Carboniferous Limestone. 531

limestone from the Lower Limestone Shales from Clifton the late
Mr. Stoddart also called attention to the absence of alumina: he
remarks,! “The absence of alumina in these beds is very remarkable,
because the Lower Limestone Shales are very argillaceous.” The
organic remains preserved in this bed are chiefly those of Crinoids,
associated with Polyzoa, the spines of Spirifera and Productus ;
in some layers the two latter are very numerous.

No. 2.—A light blue hard compact limestone, almost entirely made
up of the valves of Ostracoda, but there are also present a few
Polyzoa, the spines of Brachiopoda, and Spirorbis carbonarius. In
the majority of cases the valves of the Ostracods are broken into
fragments, but where preserved the largest measure :035 of an inch
in diameter. The remains are cemented together by crystalline
calcite, and the empty valves are also filled with the same mineral.

No. 3.—A slightly ferruginous limestone. The organic remains
are not well preserved; those which can be determined consist of
joints of Crinoids, remains of Polyzoa, valves of Ostracods and ob-
scure calcareous fragments.

No. 4.—A dark argillaceous bed containing 17:15 per cent. of
organic matter, 6-89 of which was volatile. On washing a sample
with distilled water, a large quantity of mud is got rid of, and the
residue consists of quartz-grains, fragments of shells, plant-remains,
and the jaws of Annelides.

No. 5.—A concretionary limestone slightly oolitic, the nuclei of the
granules are grains of quartz. There are also present the valves of
Ostracods, joints of Crinoids, and the remains of a small Coral.

The next specimens were selected from a quarry a little beyond
the last in the direction of Mitcheldean, in which beds were exposed
occupying a higher horizon than those in the previous quarry.

No. 6.—From a thickness of about 10 feet of thin strata, slightly
ferruginous; on exposure to the air, the carbonate of iron (in which
state the iron exists) undergoes decomposition, ferric oxide is formed
which imparts a yellow tinge to the rock. The structure exhibited is
chiefly that of calcareous sand, among the grains of which are frag-
ments of shells. The spaces between the sand are filled in with calcite.

No.7 (Pl. XIV. Fig. 3).—A bed of argillaceous limestone 34 inches
thick, and contains 11:15 of sand. It is made up of the valves of
Ostracods, occasionally Polyzoa, scanty fragments of Crinoids, and
oolitic granules. As in the previous examples, the limestone is con-
solidated by an infilling of calcite.

No. 8.—A dark argillaceous limestone 84 inches thick, and con-
taining 16-4 per cent. of sand. The calcareous constituents comprise
the spines of Spirifera, broken valves of Ostracods, and other remains
which are too obscure to be determined; some were probably de-
composed and altered shell fragments.

No. 9.—Light brown arenaceous limestone, 6 inches thick, con-
taining 387-2 per cent. of sand in quartz grains, measuring ‘004 of an
inch in diameter. Microscopic sections show the valves of Ostracods,

1 Ann. Mag. Nat. Hist. vol. viii, 3rd series, p. 487.

532 EE. Wethered—Organisms in Carboniferous Limestone.

numerous spines of Spirifera, fragments of shells, etc. The vacant
spaces are filled in with calcite.

No. 10.—A bed of blue argillaceous limestone 6 inches thick ;
contains 16°75 per cent. of sand, the grains of which are rounded
and measure about ‘004 of an inch in diameter. The rock is chiefly
made up of the spines and other remains of Brachiopoda and numerous
valves of Ostracods.

No. 11.—A black argillaceous bed 53 inches thick with calcareous
arenaceous layers. In the argillaceous material the joints of Crinoids,
remains of a small variety of Rhynchonella pleurodon and Ostracods
were discovered. Sections of the thin calcareous layers showed them
to be largely made up of the spines of Spirifera, a few joints of
Crinoids, and calcareous fragments.

No. 12.—An earthy limestone 5 inches thick; contains 12 per
cent. of sand, the grains of variable size, the largest measuring ‘008
and the smallest -002 of an inch in diameter. The limestone is
largely made up of an organism to which I shall provisionally give
the name of Mitcheldeania (Pl. XIV. Fig. 6), and which I shall
describe further on. The rock also contains some Ostracoda.

No. 18 (Pl. XIV. Fig. 4).—A light limestone 8 inches thick, con-
taining 3:2 per cent. of sand, the grains measuring -003 of an inch
in diameter. Flakes of mica and fragments of other minerals are
also present. ‘The bed contains the remains of Mitcheldeania, a few
Polyzoa, a large proportion of Ostracoda, and a shell which Mr.
Etheridge, F.R.S., tells me is allied to Murchisonia angulata.

Pl. XIV. Fig. 4 represents a portion of the rock in which the
valves of Ostracods are the chief feature. The clear calcite is well
shown filling up the empty valves and spaces between them.

No. 14.—Similar to the last, with the exception that Mitcheldeania
is less numerous. Thickness 1 foot 6 inches.

No. 15 (Pl. XIV. Fig. 5).—Made up of various small concretions,
of various shapes; calcareous fragments and occasional spines of
Spirifera. ‘Thickness 24 inches.

No. 16.—A limestone 1 foot 3 inches thick. Chiefly concretionary,
with the spines of Productus, Crinoidal remains, and other calcareous
fragments.

No. 17.—A black argillaceous bed 4 inches thick, containing 5:13
per cent. of sand, the quartz grains measuring ‘004 of an inch in
diameter. Flakes of mica and fragments of other minerals also present.

No 18.—A light argillaceous limestone 7 inches thick, containing
16:5 per cent. of sand, the quartz-grains varying between -009 and
-OO1 of an inch in diameter. The organic remains are chiefly those of
Ostracods, well preserved and capable of being extracted from the
matrix.

No. 19.—A shelly limestone 15 feet thick, and containing 39-2 per
cent. of sand. The chief calcareous constituents are the remains of
shells, and those in a very fragmentary condition.

GENERAL Review oF THE LowrR Limestone SHALES.

The samples examined are sufficient to give a correct idea of the

E. Wethered—Organisms in Carboniferous Limestone. 5338

structure of the rock generally. In the lowest beds of the series
Ostracods have contributed very largely, in some cases little else
than the valves of these small Crustaceans make up the limestone.
In the upper beds, with the exception of No. 16, they become less
numerous, and in some cases are altogether absent.

Much the same may be said of the Crinoids. Though their re-
mains occur throughout the series, they are most numerous in the
lowest beds, and in one they are the chief factor, as in Fig. 1. The
Polyzoa are most numerous in the Crinoidal bed, but are to be found
throughout the Lower Limestone Shales. They are not, however,
an important feature in the structure of the rocks with the exception
stated. The shells of Rkynchonella pleurodon are very numerous in some
beds of black shale, and on weathering taking place, they may be
collected in hundreds. The Lower Limestone shales, as with lime-
stones generally, represent the floor of a sea in which the organisms
lived which we now find in a fossil state. By their death the
limestone was formed from the calcareous portions of their structure.
The deposition of the strata doubtless extended over a long period
of time, during which the conditions were varied, and thus the life
varied according as the conditions suited. For this reason we get
limestones of different structure and quality, which, of course, was
regulated by the organisms which contributed to their formation.
The limestone-forming process was at times stayed, during which
intervals clays and shales were deposited. The water was probably
not deep. This is shown by the amount of sand in the limestone,
and also by the great profusion of Ostracods, which class of Crustacea
are not abundant in extreme depths of water.!

OrGanisms oF THE Lower Limestone SHALES.

Ostracoda.—My specimens have been referred to Professor Rupert
Jones, F.R.S., and Mr. J. W. Kirkby, to whom I am indebted for
their careful examination. The following is a list of the genera
and species which these gentlemen have been able to determine.
Probably others exist, but the difficulty of separating them from the
matrix, and thus obtaining reliable specimens, prevents a more
definite statement being made.

Kirkbya variabilis, J. & K.
», plicata, J. & K.
Cytherella extuberata, J. & K.
The above list is especially interesting and important in connection
with the Ostracoda recently described? by Prof. Jones and Mr.
Kirkby from the Gayton boring, Northamptonshire. The material
examined yielded six recognizable forms, as follows :—

Kirkbya variabilis, J. & K.

Bythocypris sublunata, J. & K.
Darwinala Berniciana (?), Jones.
Leperditia Okeni, Munster.

Macrocypris Jonesiana (?), K.

» plicata, J. & K. Cytherella extuberata, J. & K.
Bythoeypris sublunata, J. & K. - attenuata, J. & K.
Comparing the above list with mine, from the Forest of Dean, we

find that from the Gayton boring six genera and species were deter-
mined, one of which was doubtful. In my list six genera and species

1 Challenger Report, Zoology, on the Ostracoda, p. 1.
* Guou. Mag. 1886, Dec. III. Vol. III. pp. 248—263.

534 E. Wethered—Organisms in Carboniferous Limestone.

are also given, one of which, too, is doubtful. In each case we
get five undoubted genera and species, and of these four appear
in both lists. Mr. Kirkby writing to me remarks: “It is surprising
how similar the groups of species are to those we have just described
from the Gayton boring.”

Professor Jones, after an examination of different samples from
the same locality, makes similar remarks. Of the forms described
from the Gayton boring three have not been known to occur above
the Calciferous series of Scotland, which horizon is immediately
above the Old Red Sandstone (Devonian). The forms referred to
are B. sublunata, C. extuberata, and CO. attenuata. Of these two
appear in my list.

CrinorpEA.—The Crinoidal remains in the Lower Limestone Shales
appear to be those of two genera. One of these is Poteriocrinus crassus,
Miller, and the other probably Miller’s genus Rhodocrinus. In some
of my slides apparent pentagonal joints are seen (Pl. XIV. Fig 2),
which I was at first puzzled to account for. On reference to Miller’s
“ Crinoidea,” I found that he had figured! joints resembling mine,
which were also collected in the Forest of Dean, and that he referred
them to Rhodocrinus verus. Miller in his ‘ Description” ex-
presses some doubt as to whether all the forms referred by him
to this genus are really the same species; he remarks: “In the
columns (pl. ii. fig. 1, t. 22) which I consider as belonging to the
animal of this genus, I have noticed two different modes of organiza-
tion, which inclines me to suspect that although I am only able to
treat of one species as decidedly ascertained, yet two distinct species
may really exist. Thus in regard to the surface of adhesion, some
columnar joints display numerous radiating striz proceeding imme-
diately from the alimentary canal to the circumference (figs. 6 to 10);
other joints (figs. 1 to 5) have only a narrow striated rim with a
smooth central area; and again some columns (figs. 11 to 15) are
formed of joints of uniform thickness, from some of which, occa-
sionally, several side-arms proceed; whilst other columns, particularly
those from Mitcheldean, are formed of joints alternately thicker and
thinner, smaller and larger, much contracted at their margin of mutual
adhesion. In these every second or fourth joint is considerably
thicker, showing at its circumference five or six tubercles, which
render it angular and its surface waved, to which the joints above
and below conform.” It is therefore clear that Miller detected some
points of difference in the specimens from the Forest of Dean compared
with those from other localities. With regard to the striz, I think
he attaches too much importance to them; they are simply striations
on the articular faces of the stem-joints, and the features pointed out
by Miller are due to the particular portion preserved or examined.
With regard to the joints themselves, these are features which are of
importance, and though Miller only considered them of sufficient
note to possibly justify a different species, it is probable that further
investigation may prove that the fossil is wrongly referred to the
genus Lhodocrinus. Having doubts regarding the specimens which
I had collected, I sent them to Dr. P. Herbert Carpenter, F.R.S., and

1 «« Miller’s Crinoidea,’’ 1821, Rhodocrinites, plate 2, figs. 17, 18, 19, p. 107.

E. Wethered—Organisms in Carboniferous Limestone. 539

asked his opinion onthem. He kindly wrote meas follows: “I think
your pentagonal stem-joints may not improbably be identical with those
figured by Miller on plate 2 of Rhodocrinus, figs. 17-22, but I have
great doubts whether they can be properly referred to Rhodocrinus.”

The microscopic section shown in Fig. 1 appears to throw some
light upon the apparent pentagonal joints. The central object re-
presents one of them surrounded by a circular margin. It is there-
fore possible that some of these Crinoids have a pentagonal centre,
and that it is this central portion which is represented on Pl. XV.
Fig. 12. I have shown my specimens to Mr. R. Etheridge, jun., who
informs me that he has observed the same thing in some Crinoids
which have come under his notice.

Potyzoa.—The specimens of Polyzoa were sent to Mr. John
Young, Curator of the Hunterian Museum, Glasgow, who kindly
examined them for me. Though the Polyzoa occur in such large
numbers in the crinoidal bed, Mr. Young has only been able to detect
two genera and species, namely, Rhabdomeson (Millepora) gracile
(Phill.), and Fenestella tuberculocarinata (Etheridge, jun.).

MircueipEanta NicHo.soni, gen. et. sp. nov. (Plate XIV. Fig. 6).
—TI have referred the specimens of this organism to Mr. John Young,
Dr. Hinde, Professor Nicholson of Aberdeen, and to Mr. Robert
Etheridge, jun., all of whom have kindly examined them, but are
unable to recognize them as identical with any known form. I have,
therefore, determined to describe and figure it as a new provisional
genus under the name of Mitcheldeania, after the locality (Mitcheldean)
near which I found it. To Professor Nicholson I am especially
indebted for assistance in examining the fossil, but he is in no way
committed to any of my remarks in reference to it. As a slight
acknowledgment of Professor Nicholson’s assistance and appreciation
of his work generally, I propose to name the first species of the
genus Nicholsoni. In working out this organism I have been placed
at a disadvantage in not being able to separate reliable specimens
from the matrix, on account of the nature of the rock in which the
fossil occurs ; the determination, therefore, has been chiefly arrived
at from microscopic slides.

The organism, Fig. 6, consists of a series of concentrically arranged
layers, or laminz, penetrated by systems of tubuli which become
more minute and numerous in the central series of lamine. The
tubuli are separated by the skeleton fibre, which is itself penetrated
by a minute canal system. There are also other tubuli of larger
size than are seen in the inner lamine, which appear first in the third
series, and become more numerous outwards. The skeleton fibre
is also penetrated, in places, by centres of growth made up of
concentrically arranged minute tubuli, resembling the series which
constitute the nucleus of the entire organism. At the base there
is a peduncle which probably served for attachment.

Conciusions.— Mitcheldeania Nicholsoni, then, was an organism the
structure of which consisted of a series of concentrically arranged layers
penetrated by two systems of tubuli, the larger measuring ‘003 and
the smaller ‘001 of an inch in diameter. The latter were probably
filled with living matter, and the larger I regard as zodidal tubes. I

536 E. Wethered—Organisms in Carboniferous Limestone.

would refer this organism to the Hydractinide, and as allied to the
Stromatoporoids. Professor Nicholson is himself struck with the
similarity of the structure to certain Stromatoporoids, but remarks that
he is not aware of any which have so minute a canal system of precisely
the same nature; and that if it be referable to the Stromatoporoids, it
would probably require to be placed in a new genus. Of course I
am aware that Stromatoporoids have not before been noticed in
Carboniferous rocks, but that is no reason why they should not occur.

In referring Mitcheldeania Nicholsoni to the Stromatoporoids, I do
not wish to ignore certain features which this fossil possesses in com-
mon with some other Hydrozoa. Professor Nicholson called my at-
tention to Parkeria, Carp., which no doubt shows structure which is
also seen in M. Nicholsoni, but in the former there is a nucleus con-
stituted of chambers which are laid end to end in a reticulate direc-
tion, and separated by septa. I have not detected a nucleus of this
nature in M. Nicholsoni.

Another organism which especially struck Dr. Hinde as similar to
my new genus is Girvanella problematica, Nich. and Ether., jun.
Professor Nicholson has kindly sent me rock specimens containing
that fossil, from which I have been enabled to get some good sec-
tions. As regards mode of occurrence, there is a great resemblance,
and also in the concentric lamination, but the minute structure is
quite different. g

Tue Carsonirerous Limestone—or Stage B of Prof. Hull—con-
stitutes the middle division of the limestone series in the Forest of
Dean. Commencing with the lowest beds, I have worked upwards,
and in all that I have examined, the slides exhibit the same structure,
namely, a rock made up apparently of very small calcareous granules
(Pl. XV. Fig. 7). It is not, however, so formed; the key to the
problem is Pl. XV. Fig. 8, in which we see the outlines of a previous
structure, the whole having undergone complete change and been
replaced by crystalline material. The granular appearance is due
to the small crystals and possibly large ones which have cracked or
split up into fragments. As to what the replacing mineral is, the
following chemical analysis will enable us to judge. The sample
was taken from the centre of the formation, and though one analysis
cannot be said to prove the composition of the whole 360 feet of
strata, yet I believe it to be typical of at least a large portion.

In making the analysis I was assisted by Mr. W. H. Wiltshire,
F.C.S. As it is important, I will state it in two forms:

II, II.

Moisture Sd ete Aes -02 | Moisture... ai ott fe “02
Organic matter... 904 20 6°17 | Organic matter ... eae Boe el
Carbonic acid ... aBe ... 44:01 | Insoluble Residue end LOG
Insoluble Residue a. aie 1:06 | Carbonate of Iron wie LOL
Soluble Silica ... an An ‘10 | Soluble Silica ... ans dats 10
Ferrous Oxide ... due 8 ‘63 | Carbonate of Lime Ce ... 54:00
Time ieee 506 sae ... 80°24 | Carbonate of Magnesia... .. 30°19
Magnesia sie ane ... 17°50 | Carbonate of Soda with trace of

SOGE, © aan mae es suis 25 chlorine BoE ai Ba 43

99°98 99-98

E. Wethered—Organisms in Carboniferous Limestone. 537

The foregoing analysis shows the limestone to be dolomitized, the
carbonate of magnesia being as high as 37 per cent. Of this I shall
treat further under the head of chemistry.

Tur Upper Limestone Serins.

This series consists of two varieties of limestone locally termed
the “‘ Crease” and ‘‘ Whitehead.” The former occupies the lower
horizon of the two.

The Crease (Pl. XV. Fig. 9).—The samples which I have examined
show an unusually coarse structure due to the size of the calcareous
fragments of which the limestone is made up. ‘The origin of these
calcareous fragments is somewhat obscure, but I have detected among
them undoubted remains of Crinoids. The grains are closely com-
pressed, reminding one of the structure of arenaceous grits; the
rock is, indeed, a calcareous grit.

The ‘“ Whitehead” Limestone.—The ‘‘ Whitehead” follows the
“Crease,” and is represented by an interesting series of beds from
which I have selected the following as typical.

No. 1 (Pl. XV. Fig. 11).—Oolitic limestone, from a thickness of
about forty feet. The granules measuring from ‘007 to 018 of an inch
in diameter. The nuclei are generally destroyed, leaving an open
space. The spaces between the granules are often wide and are
filled with calcite.

No. 2.—A concretionary limestone from a bed three feet thick.
Contains the valves of Ostracoda, spines of Productus and angular
grains of quartz. There are also present circular rings as large as
005 of an inch in diameter, and are a conspicuous feature in the
rock.

No. 38.—From a bed made up of concretionary nodules, as large as
an inch in diameter, and calcareous sand. Microscopic sections of
the nodules reveal the remains of a variety of organisms, but all
badly preserved.

No. 4.—This is a very interesting bed, and makes a beautiful object
under the microscope (PI. XV. Fig.12). The rock is made up of the
remains of a spiral shell, of Foraminifera, Ostracoda, Polyzoa, and
obscure calcareous fragments, the whole being cemented together by
clear calcite.

No. 5 (PI. XV. Fig. 10).—A peculiarly white limestone, which
gave the following analysis :—

Insoluble residue (sand) ont 600 soe soon) eSB
Organic matter 506 50 ae oe ee O94
Water oeG Pep 906 506 “100 ede Sh CAO
Carbonate of Lime ... 300 500 he ... 85°56
Carbonate of Iron... ae 500 ss 506 “46
Soluble Silica 000 Doe si06 500 200 “01
Carbonate of Magnesia 0K wae is 0 "84
Alkalies wen sie 20 dae eae esr sO,
Phosphate and Sulphate of Lime, and loss ... Soe “78

100°00

Sections of the limestone show it to be largely made up of the

5388 FE. Wethered—Organisms in Carboniferous Limestone.

remains of Ostracoda, among which Professor Jones has distinguished
Leperditia and Cytherella, but as we have not been able to separate
any from the matrix, the species have not been determined. In
addition to Ostracoda, the rock contains remains of Foraminifera
badly preserved, also occasional Polyzoa, and the spines (and possible
shell fragments) of Productus.

GENERAL VIEW oF THE Upprr LimMESsTONES.

The beds of the Upper Limestones indicate a return of conditions
not unlike those which existed at the time of the deposition of the
Lower Limestone Shales. At the period of the latter, the Carbon-
iferous Limestone was about to commence; at the period of the
former, it was near to its close, and the great Coal epoch was
soon to dawn. From what I have said respecting the changes which
the beds of stage B, or the Carboniferous Limestone proper, have
undergone, it is difficult to say what fossils they contained or what
organisms contributed to the formation of the limestone; but in the
Upper Limestones we get a return of life similar to that which con-
tributed so largely to the Lower Limestones. I therefore contend
that I am justified in forming a separate division of the Upper Lime-
stones. If I am not, then there is no justification for making a
separate division of the Lower Limestone Shales.

CHEMISTRY.

As in the case of limestones generally, the Lower and Upper series
have been consolidated by the deposition of calcite in the vacant
spaces between the organisms and other calcareous fragments. With
regard to the Carboniferous Limestone, that, too, undoubtedly
originated from calcareous organisms, but a subsequent change
occurred which replaced the original structure with magnesia and
possibly some calcite. I am not aware that dolomitization in the
Carboniferous rocks of the Forest of Dean has before been noticed,
but it has in other localities. Mr. Sorby, F.R.S., states! that “in
Derbyshire and elsewhere some of the beds are almost pure dolomite.
As far as can be judged from their structure, they may have been
normal limestones completely changed after deposition, and cer-
tainly do enclose dolomitized shells, Corals, and Encrinites.” The
late Professor Harkness called attention to the same thing in a
paper? “On the Jointing in the Carboniferous and Devonian Rocks
in the district around Cork and on the Dolomite of the same district.”
The limestone referred to by Professor Harkness has undergone
considerable jointing, which he considered to be a factor in the pro-
cess by which those particular beds became dolomitized. He says :*
“The whole aspect of the Carboniferous dolomites of Cork and
Kilkenny leads to the inference that certain changes have been
effected on previously existing masses of carbonate of lime; and
the general parallelism which occurs between these dolomites and

Quart. Journ. Geol. Soc. Proc, 1879, vol. xxv. p. 87.
2 Quart, Journ, Geol. Soc. vol. xv. p. 86.
§ Quart, Journ, Geol. Soc, vol. xv. p. 103.

E. Wethered—Organisms in Carboniferous Limestone. 939

the main joints, and also the intimate connexion which exists between
them, supports the conclusion that the change was produced after
the operation of those forces which gave rise to the phenomena of
joints.” Professor Harkness attributes the dolomitization to the sea-
water finding its way into the joints and fissures of the limestone
when submerged. In the case of the Forest of Dean, however, the
amount of jointing would not be sufficient to produce such effects,
in the presence of sea-water, as Professor Harkness speaks of in the
district of Cork. That sea-water was the agent which supplied
the magnesia I do not agree. Professor J. D. Dana states” that
«analyses of the Coral Limestone of the elevated coral island Matea,
by Professor B. Silliman, jun., have determined the singular fact that,
although the Corals themselves contain very little carbonate of mag-
nesia, magnesia is largely present in some specimens of the rock.
It affords on analysis, 88-07 per cent. of carbonate of magnesia, and
hence only 61:98 of carbonate of lime. ... This introduction of
magnesia into the consolidating submerged coral-sand or mud, has
apparently taken place (1) in sea-water at the ordinary temperature ;
and (2) without the agency of any mineral waters except the ocean.
But the sand or mud may have been that of a contracting and
evaporating lagoon, in which the magnesia and other salts of the
ocean were in a concentrated state.” Looking at the fact that the
Carboniferous Limestone in the Forest of Dean was undoubtedly
originally formed by accumulations of the remains of organisms,
seems to me to be against the lagoon theory. Had the strata been
deposited under conditions of concentrating waters, I fail to see
how the organisms could have lived in so briny a solution. In
endeavouring to arrive at a solution of the problem, there are two
details which must be considered. (1) The beds of the Carbon-
iferous Limestone are not mixed with argillaceous strata; those
of the Lower and Upper Limestone series are. (2) The proportion
of insoluble residue (sand) in the Carboniferous Limestone is small.
These two facts seem to indicate that either there was deep
water at a distance from land, too far for much sediment to be
carried, or else a lagoon existed. My objection to the lagoon
theory has already been stated, and I think the evidence is in
favour of deep water some distance from land. But in what way
would this solve the problem of the formation of dolomite in the
Carboniferous Limestone? We must consider the fact that in the
Lower and Upper Limestones there are argillaceous beds; these
latter are less numerous in the former than in the latter, and I am
informed by Colchester Wemyss, Esq., J.P., that some of the beds
contain a considerable proportion of magnesia. The effect of these
argillaceous beds, it seems to me, would be to cover the limestone
beneath with a water-tight stratum. This, however, was not so in
the Carboniferous Limestone, and consequently the sea-water would
have free course through the at first loosely accumulated calcareous
remains. That dolomite might, under such circumstances, result
from the decomposition of magnesium chloride, and possibly

1 Corals and Coral Islands, 1872, pp. 356—367.

540 Aubrey Strahan—Rocks beneath the Coal-measures

magnesium sulphate, we can readily understand. That dolomite
can be produced by the decomposition of magnesian chloride in the
presence of Iceland spar has been proved by Mr. Sorby, F.R.S.*

EXPLANATION OF PLATE XIV.

Fig. 1. Crinoidal Limestone, Lower Limestone Shales.
», 2. Apparent pentagonal stem joint of a Crinoid, from the same bed as Fig. 1.
», 98. Lower Limestone Shales, contains remains of Ostracoda, occasional Polyzoa, &c.
», 4. Lower Limestone Shales, chiefly made up of the remains of Ostracoda.

The infilling calcite in the spaces between the organisms is well illustrated
in this specimen.

», 9. Lower Limestone Shales, chiefly made up of minute calcareous fragments
and concretions.

», 6. Mitcheldeania Nicholsent.

PLATE XY.

Fic. 7. Dolomitized Carboniferous Limestone.

», 8. Dolomitized Carboniferous Limestone, the outlines of previous structure
remaining.

», 9. ** Crease Limestone,’’ base of Upper Limestone Series.

», 10. ‘‘ Whitehead Limestone,” Upper Limestone Series, showing remains of
Ostracoda and Polyzoa.

», Ll. Oolitic Limestone, Upper Limestone Series.

», 12. Whitehead Limestone, another bed, showing remains of Ostracoda, spines of
Productus, ete.

Ii.—On tHE Rocks suRRoUNDING THE WARWICKSHIRE COAL-FIELD,
AND ON THE Bask OF THE COAL-MEASURES.”

By Ausrey Srrawan, M.A., F.G.S.,
H.M. Geological Survey.
With Appendix I. on the Igneous Rocks of the Neighbourhood, by Frank Rutley,

F.G.S. Appendix II. on the New Species Olenus Nuneatonensis and Oboledla
granulata, by G. Sharman.

(Communicated by permission of the Director-General.)

N a paper read before the Birmingham Philosophical Society in
1882, it was announced by Professor Lapworth that the dis-
covery of fossils in some shales underlying the productive Coal-
measures of Warwickshire, and coloured on the Geological Survey
Map as Coal-measures, proved that these shales must be of Cambrian
age (Lower Silurian of the Geological Survey). As the true age
of these shales had for many years been a debateable question,
Professor Lapworth’s discovery was of considerable interest, and
has led to an important alteration being made in the map, the sup-
posed Lower Coal-measures and Millstone Grit having both been
now relegated to the Lower Silurian (Lingula Flags). It may
be of interest, before entering on the description of these beds, to
trace shortly the history of the error in their classification.
The first notice referring to the older rocks of Warwickshire that

1 Quart. Journ, Geol. Soc. Proc. 1879, vol. xxxv. p. 73.

2 Read before Section C. (Geology), British Association, Birmingham, Sept. 2, 1886.

3 The nomenclature of the Geological Survey, according to which the Lingula
Flags are included in the Lower Silurian, will be used throughout this paper.

and around the Warwickshire Coal-field. 541

appeared in the publications of the Geological Society is a paper on
the occurrence of manganese near Hartshill.! The ore is described
as occurring in detached pieces weighing from one to sixty pounds
each, and distributed through a red clay, which chiefly forms the
soil of the neighbourhood.

In 1822 the rocks in which the ore occurred were referred to as
Coal-shale and Millstone Grit by Conybeare and Phillips.2 In 1829
the Rev. James Yates® pointed out the resemblance of the Hartshill
quartzite to that of Bromsgrove Lickey, and gave a most accurate
account of the overlying shales and the intrusive character of the
voleanic rocks, concluding that the quartzite and shales must be
considered of Silurian age. In 1855 the Geological Survey Map
(63 8.W.) was published, and was followed in 1859 by the Memoir on
the Geology of the Warwickshire Coal-field, Sir R. Murchison being
Director-General. In these publications the quartzite was referred
to the Millstone Grit, and the overlying shales to a lower or unpro-
ductive subdivision of the Coal-measures. The reasons for which
this classification was adopted are given on p. 8 of the Memoir. The
quartzite “ has an average dip to the south-west at an angle of from
30° to 40°, passing under the ordinary Coal-measures which lie con-
formably upon it. No fossils have ever been found in it, and from
the strong resemblance it bears to the quartz-rock of Bromsgrove
Lickey, it was formerly classed as part of the Silurian series; but
from the fact of the complete conformity of the Coal-measures upon
it, and the occasional streaks of Coal-measure-looking shale with
which it is banded, the evidence is more in favour of its belonging
to the Carboniferous formation.” This conclusion was not arrived
at without anxious deliberation. The late Prof. Jukes and Mr.
Howell were in favour of retaining the beds in the Silurian series,
while Sir A. Ramsay (at that time Local Director), in consideration
of the perfect conformity between the quartzite and overlying shales,
and of the apparent conformity between the shales and the productive
Coal-measures, was of opinion that they must be included in the
Carboniferous series. The views of Prof. Jukes are given in the
Memoir on the South Staffordshire Coal-field (Memoirs of the Geolo-
gical Survey), 2nd edition, 1859, p. 134. After speaking of the
gentle westerly dip which the Silurian strata of the South Stafford-
shire Coal-field had assumed before the deposition of the Coal-
measures, he continues: “That this gradual rise to the east was
continued yet further in that direction beyond the bounds of our
district is rendered probable by the fact of rocks still older than the
Upper Silurian (perhaps older than any Silurian) appearing in the
Warwickshire and Leicestershire coal-fields, with the Coal-measures
resting directly upon them.” Previously (pp. 80, 81, fig. 11), he

1 Notice on the Black Oxide of Manganese of Warwickshire, by S. Parkes,
Trans. Geol. Soc. series 2, vol. i. p. 168, 1824 (read 1821).

Outlines of the Geology of England and Wales, by the Rev. W. D. Conybeare
and W. Phillips, book iii. chap. iii. p. 406, and chap. v. p. 456.

3 On the Structure of the Border Country of Salop and North Wales, etc., Trans,
Geol. Soc. series 2, vol. ii. p. 287, 1829 (read in 1824).

542 Aubrey Strahan—Rocks beneath the Coal-measures

had figured and described a section near Dudley, in which the Coal-
measures were seen resting on Silurian shale, both being nearly
horizontal, but the unconformity being shown by the fact of the
Coal-measures abutting against a small cliff of Silurian shale at one
part of the section. “ From this very instructive instance we learn
generally how, with perfect apparent local conformability, there may
be still on the large scale a very great amount of unconformability
between two formations.” From these statements it is quite clear
that Prof. Jukes had fully grasped the true relation borne by the
Warwickshire quartzite and shales to the overlying Coal-measures.

In 1879, the results of a microscopic examination of the intrusive
Diorites were described by Mr. Allport,’ who accepted the conclusion
of the Carboniferous age of the rocks, and it was not until the year
1882 that the discovery of fossils in the shales by Prof. Lapworth ?
finally disposed of the possibility of the beds being of Carboniferous
age, and established the correctness of the earlier view that the
quartzites with the overlying shales were of Silurian age. This
being the case, it was evident that the base of the Coal-measures
had yet to be found, and traced upon the map, and for the purpose
of doing this I received instructions to proceed to the district in the
spring of this year.

This task was rendered far easier than it would otherwise have
been by Professor Lapworth’s kindness in placing freely before me
the results of his own observations on the Silurian rocks, and on
their relations to a still older volcanic series beneath, one of the
most valuable of these results being his discovery of fossils at
different horizons, ranging from near the top to near the bottom of
the shales. For the resemblance of the Silurian shales, and espe-
cially of some soft nearly black bands, to Coal-measures is so
striking, that in the absence of such fossil evidence the difficulty of
separating them would have been greatly increased. Not only are
the Silurian shales entirely uncleaved, and, except in the immediate
neighbourhood of the intrusive igneous rocks, very little altered,
but their dip agrees very closely both in amount and direction with
that of the Coal-measures, especially in the southern part of the
district. The clue once provided, however, it became easy to see
(1) that the conformability of the shales with the Coal-measures is
apparent only, there being in reality such evidences of discordance
as might be expected between rocks so very different in age;
(2) that the Coal-measures are based by an impersistent bed of
sandstone containing pebbles of quartzite and of the local rocks,
bearing evidence (as in South Staffordshire) of having been deposited
in the hollows of a floor of gently inclined Silurian strata; while
(3) it became clear that the intrusive igneous rocks are entirely of

1 On the Diorites of the Warwickshire Coal-field, Quart. Journ. Geol. Soc. vol.
xxxv. p. 637, 1879.

2 On the Discovery of Cambrian Rocks in the Neighbourhood of Birmingham,
Grou. Mae. New Series, Dec. IJ. Vol. IX. p. 563, 1882 (reprinted from the
Proc. Birmingham Phil. Soc. vol. iii. p. 284). See also Grou. Mac. New Series,
Dec. III. Vol. III. p. 319, 1886.

and around the Warwickshire Coal-field. 543

pre-Carboniferous age, and do not affect the Coal-measures in any
way whatever.

The total thickness of the Coal-measures, as now shown, amounts
to between 600 and 700 feet, in place of about 8000, as previously.

It will be convenient in describing these rocks to take them in
order of age, beginning with the southern end of the range of each
formation.

The Caldecote Series.

The oldest rocks are found near Caldecote, rising from beneath the
quartzite on the north-east side of the range of low hills, which this
rock forms between Nuneaton and Hartshill. They are referred to
by Professor Lapworth as the Caldecote Volcanic Series, and consist,
as he pointed out to me, of a finely-laminated rock, probably a tuff,
with intrusions of diabase and quartz-porphyry.’ There are very
few exposures of these beds. About a quarter of a mile east of
Caldecote Windmill, there is an abandoned quarry known as the
‘Blue Hole,’ from which paving cubes were formerly obtained.
The rock in request was the diabase, but the workings on the north
side intersected quartz-porphyry, which had been intruded into, and
contained fragments of, a highly altered fine-grained ash. The
diabase with a sharply-defined line of separation is found in the side
of the quarry above the quartz-porphyry. Its intrusion is con-
sidered by Professor Lapworth to have taken place subsequently to
that of the quartz-porphyry.2 The tuff has been found again by
Professor Lapworth in the entrance to an old tunnel 100 yards west
of Caldecote Hill, where the presumed bedding-planes have a dip
25° to 30° in the same direction as the quartzite, that is, about
south-west. The further extension of these beds is inferred from
the occurrence of fragments in the soil, and from the position of the
overlying conglomerate, which will now be described.

The Harishill Quarizite.

The Hartshill quartzite extends from the Midland Station at Nun-
eaton to half a mile north of Hartshill, with a steady dip to the
south-west of from 25° to 45°. The whole series can be seen in the
series of immense quarries in which it is worked for road-metal.
The base of the quartzite is a coarse stratified conglomerate or breccia,
containing fragments of the underlying Caldecote series, some of the
fragments ranging up to the size of half a brick, as was pointed out
to me by Prof. Lapworth. The base is seen in the cutting by which
Boon’s Quarry is entered, about one-third of a mile south-east of
Caldecote Windmill. The quartzite becomes coarse in grain towards
the base and passes into a grit made up of small rounded grains of

1 These rocks were referred to by Sir Andrew Ramsay in his evidence given
before the Coal Commissioners as being of doubtful origin (Report of Coal
Commission, vol. ii. p. 470). Hventually from the limited nature of the exposures,
and the small advance that petrography had made at the time of the publication of
the map, they were included in the index with the intrusive diorites under the
general name of greenstone.

* Gzou, Maa, for 1886, p. 320.

544 Aubrey Strahan—Rocks beneath the Coal-measures

quartz and other rocks. This grit rests on the greenish and purplish
coarse conglomerate or breccia mentioned above. A better exposure
of the lower beds is found in the entrance to a quarry half a mile
south-east of Hartshill. There there occur in the quartzite thin
bands of intrusive igneous rocks much decomposed. The lower beds
of the quartzite consist of bands of conglomeratic grit, well bedded
and split up with shaly partings, and strongly impregnated with
manganese. The conglomerate is seen for a thickness of more than
eight feet, but the actual base is not exposed. There are also a few
conglomeratic bands higher up in the quartzite, with pebbles ranging
up to half an inch in diameter.

I may remark here that the Blue Hole and both the sections in
which the basement conglomerate is exposed have been opened since
the original survey of this district was made, and that it was there-
fore almost impossible at that time to determine the nature of the
rock beneath the quartzite, and its relation to this formation. The
true nature of the Caldecote Series and of the basement conglomerate
of the quartzite was first detected by Prof. Lapworth.

The great mass of quartzite overlying this basement conglome-
rate is an intensely hard fine-grained siliceous rock, in which the
original sand-grains are so closely cemented together by silica as to
have almost lost individuality. The rock, however, is well bedded,
and contains thin bands of green or purplish shales. It is used most
extensively for road-metal, and nearly the whole series of beds is
exposed in one or other of the great quarries. The quartzite is also
traversed by sheets of intrusive igneous rocks, ranging from 8 to
over 100 feet in thickness, and following the bedding with remark-
able regularity. The igneous rocks are usually quite decomposed to a
depth of from 380 to 40 feet from the surface, especially when in thin
beds. They are locally known among the quarrymen as “Dun Dick,”
and when sufficiently fresh are “cut” (broken to size) into paving
cubes. The price of the quartzite road-metal is 3s. a ton when
broken to size. Iwas informed that a prepared cubic inch of quart-
zite crushed at a pressure of 24,000 lbs. to the square inch, the
igneous rocks yielding at between 11,000 and 12,000 lbs. to the
square inch.

A good exposure of one of these intrusive sheets is found in the
Midland Company’s Quarry at Nuneaton Midland Station. The
quarry is principally in this thick sheet, the eastern part only being
in quartzite. The jointing of the igneous rock, which at a distance
resembles bedding, is nearly at right angles to the bedding of the
quartzite, that is, perpendicular to the plane along which the melted
rock has been injected. In this quarry the basement-bed of the New
Red Sandstone may be seen lying across the edges of the quartzite
and igneous rock, as will be described subsequently. Another great
sheet is seen in the cutting by which a quarry on the east side
of the high road, one-third of a mile south of Caldecote Windmill,
is eutered, and again close to the windmill. This sheet forms the
boundary up to which the old quarries along the road were worked.
Most of the quarries now worked are in beds below this sheet.

and around the Warwickshire Coal-field. 545

The Stockingford Shales.

The shales which overlie the quartzite occupy a considerably larger
area. They extend from a little south of Bedworth to Waste Hill,
one mile and a half north-west of Atherstone, a total distance of nine
miles and a half. They are divisible into two perfectly conformable
subdivisions, the lower, which rests quite conformably on the
quartzite, being distinguished by a bright red tinge and by the pre-
sence of minute Brachiopods of the genera Lingulella and Obolella,
the upper consisting of olive-coloured, grey, and thin black shales,
with Agnostus and Olenus.! The shales are fine-grained and laminated
and contain only a few harder and more sandy micaceous bands.
They are altogether uncleaved, and present so close a resemblance
to Coal-measures, as to have led (in the absence of fossil evidence
and in view of their apparent conformity with the productive
measures) to their having been originally classed as Lower Coal-
measures.

They are traversed by very numerous sheets of intrusive diorite,
etc. ‘These igneous rocks are frequently found to follow a bedding-
plane for many yards, and on a general view indicate the strike of
the shale very accurately. On a close examination it becomes
evident that the shale overlying each sheet of igneous rock is as
highly altered as that below, and that frequently the igneous rocks
break obliquely across the beds, or even swell out into bosses,
forcibly contorting and thrusting aside the surrounding shales.
These facts, indicating the intrusive character of the rock, were
clearly recognized by the Rev. J. Yates in the year 1824.

The southern termination of this range of Lower Silurian shales
is concealed by Drift. But the beds seem to have been found ina
colliery shaft at Hawkesbury Basin, one mile south of Bedworth,
where the following section was proved :°—

ft. in.
Bind, rock, and fire-clay with coal andironstone 182 11
Coal-measures. { Black shale-rock ..............0.csscescecseceecscess 6
Wihitemock- binds” s...cs-+ ss aoaeecoeececteee eeace 16
Alternations of hard black bat and granite-
inicemrocisine boulders... .eecetseesctenos eneee cece 25 3
357 = 8

Mr. Howell remarks that the “granite-like rock” was not a granite,
but that, not having seen it in situ, he is unable to say whether it is
_ trap or an altered sedimentary rock. It seems extremely probable,
however, that the reck described as hard black bat was the altered
Lower Silurian shale, and the granite-like rock some of the dioritic
intrusions which are so numerous in this part of the shale, as seen
at Chilvers Coton.

The most southerly exposure is at Marston Jabet in the old quarry
in diorite figured in the Memoir on p. 89, but the first surface

1 This subdivision consists of two zones according to Prof. Lapworth, an upper
zone characterized by Spherophthalmus aiatus, Beck., and a lower zone with
Aynostus sociale, Tullberg, Grou. Mac, for 1886, p. 321.

* The Geology of the Warwickshire Coal-field (Geol. Survey Memoir), p. 20.

DECADE III.—YOL. III.—NO. XII. 30

846 = Aubrey Strahan—Rocks beneath the Coal-measures

evidence we get of the boundary between the Coal-measures and the
Silurian shales occurs in the railway south-west of Griff Hollow.
The bottom of the railway cutting is in white fireclay with nodules
of clay-ironstone, while the wood on the east side is planted over
old excavations in flaggy Silurian shales, lying on the top of the
thick mass of diorite which is seen at the point where the road
crosses the Griff Canal." The boundary of the Coal-measures is
marked by a shallow “strike-valley,” due to the comparative soft-
ness of the beds.

In the Chilvers Coton Railway-cutting we get a clear view of the
Silurian shales, several intrusions of diorite, etc., and of the base of
the Coal-measures. In walking from the station southwards we
find first grey shales with a thin bed of diorite near the bridge. A
few yards south of the bridge these shales pass under a thick mass
of diorite, which extends to a distance of 150 yards south of the
bridge; there its base is fully exposed. It rests upon shale dipping
normally about west-south-west, but thrown into contortions imme-
diately under the diorite. The base of the diorite is very straight
and forms an angle of 25° with the horizontal. At first sight it
resembles a fault of very low-hade, but it seems on the whole more
probable that its appearance is due to the diorite having broken
through and across the shales at the time of its intrusion. Faults
are rare in this neighbourhood, but evidences of the intrusive charac-
ter of the diorite are abundant. The contortions of the shale more-
over do not point to motion in any definite direction along the line
of junction, but rather resemble the foldings produced in the leaves
of a book by pressure straight upon their edges.

The shales which lie on the south side of this diorite have a steady
dip to W. 10° S. of about 20°—80°. At 90 yards distance from their
junction with the diorite just described, they are found to be split
up by numerous strings and sheets of diorite and andesite, ranging
from three inches to as many yards in thickness. These intrusive rocks,
as is often the case, follow the bedding-planes very closely, so as to
imitate contemporaneous lava-flows. But the alteration of the
shale above, as well as below, the igneous rock is sufficiently marked
to have determined the intrusive character of the diorite, without
the conclusive evidence obtainable in other sections. The same
shales occupy the cutting for a few yards further, until we are sud-
denly made aware of the fact that we have passed the boundary
of the Coal-measures by the exposure of a seam of coal on the west
side of the railway, as subsequently described.

The Coal-measures occupy the cutting to a distance of 130 yards
south of the Accommodation Bridge, where the Silurian shales are
brought to the surface again by a small fault. These shales dip to the
north-east, and are highly altered by the influence of a sheet of
diorite, which is seen in the cutting to rise from beneath them at
45 yards distance from the fault. The same sheet is well seen in a
quarry behind Griff Hollow Farm, and in the high road close by.
The diorites in this neighbourhood are much decomposed, and show
spheroidal weathering even in the thinnest bands.

and around the Warwickshire Coal-field. 547

Another very admirable section has been opened in these rocks,
in the Midland Railway hetween Nuneaton and Stockingford. The
eastern end of the cutting is in red and grey or green shales, the red
tinge being, as before mentioned, the predominating colour in the
lower part of the Lower Silurian shales. The first sheet of diorite
is met with a few yards east of the Accommodation Bridge. It is
about 50 feet thick and contains a band of shale, 6 inches thick, about
3 feet from the top. This shale is of course highly altered, but the
shale above and below the diorite has also been baked hard for a
distance of about 6 or 8 feet. The top of the diorite is seen on the
south side of the cutting and to the east of the bridge. On the west
side of the bridge the overlying beds are seen to be pale grey shales
with bands of black shale, the whole presenting an appearance very
like that of Coal-measures. Further to the west the shales are seen
to be traversed by numerous bands of diorite, etc., ranging from
1 to 8 feet in thickness, and in most cases following the bedding ;
but it may be noticed that some of the thicker beds thin out and
reappear very suddenly, while on the south side of the cutting near
the bridge, a sheet of diorite cuts across the beds of shale at an
oblique angle. The western end of the cutting runs through pale
fine shales with an occasional black band, or more sandy micaceous
rocky bed. The dip increases westwards till the beds become nearly
vertical.

The outcrop of the Lower Silurian shales throughout the northern
part of the district ranges from one-half to one mile in width, and from
the abundance of intrusive sheets and masses of diorite and other
rocks, forms a prettily undulating country. The red beds which lie
next above the quartzite can be well seen in Atherstone Outwoods; in
a lane forming the south-east side of Purley Park; on the north side
of Hartshill Heys; and near Hartshill. They are interstratified
with pale grey or olive shales. The upper part of the shales are
grey and contain dark, almost black, bands, and are well exposed at
Oldbury Reservoir, in Monks Park, and in the Atherstone and
Birmingham high road. The best section of the diorite is afforded
by the great quarry at Oldbury Reservoir, where the whole thick-
ness of a great sheet, with its junction with the shales above and
below, is clearly seen. The description of this and of the other
igneous rocks that have been referred to has been written by Mr.
Rutley, and will be found at the end of this paper.

The following is a list of the fossils which were collected by Mr.
Rhodes, fossil collector to the Survey, during the examination of this
tract. Many of the best localities were pointed out to me by Professor
Lapworth. The specimens have been identified by my colleague,
Mr. G. Sharman.

Sponge spicules, Protospongia fene- { Lane on S, side of Purley Park, 30 yards down.
strata ?, Salt. Grey shale. 1 specimen.
spat Lane on 8. side of Purley Park, near top.
LIONEL { Grey shale. 2 specimens. ;

é : oi. ( Lane on S. side of Purley Park, near top.
Rod-like bodies, Annelids or Plants ? i Grey shale. 1 specimen,

548 Aubrey Strahan—Rocks beneath the Coal-measures

Half a mile N.W. of Hartshill Castle. Red
shale. 2 specimens.

Atherstone Outwoods, 250 yards W.N.W. of
Rawn Hill. Redshale. 15 specimens.

Griff Hollow Farm House. Grey shale. 1
specimen.

200 yards 8.W. of Merevale Church. Grey
shale. 3 specimens.

200 yards 8.W. of Merevale Church. Grey
shale. 11 specimens.

200 yards S.W. of Merevale Church. Grey
shale. 38 specimens.

200 yards W. of The Mawbournes. Grey
shale. 3 specimens.

Road-cutting, + mile S. of Chilvers Coton.
Grey shale. 3 specimens.

{ Junction Ot Griff and Coventry Canals. Grey
shale. 2 specimens.

W. end of Midland Railway cutting. Grey
shale. 32 specimens.

W. side of Railway cutting, 300 yards 8. of
Chilvers Coton Station, "Grey shale. Isp.

; W. end of Midland Railway cutting. Grey

_ Shale. 2 specimens.

Marston Jabet. Red shale. 7 specimens.

200 yards W. of The Mawbournes. Grey
shale. 2 specimens.

Lane on S. side of Purley Park, 30 yards down.
Black shale. 47 specimens.

Lane on 8. side of Heel Park, 50 yards down.
Red shale. 1 specimen,

Atherstone Outwoods, + mile S.W. of Rawn
Hill. Red shale. 8 specimens.

Lane on 8S. side of Purley Park, near foot of
hill. Red shale. 2 specimens.

| Lane on S. side of Purley Park, near top.
Grey shale. 3 specimens.

200 yards S.W. of Merevale Church. Grey
shale. 2 specimens.

Rod-like bodies, Annelids or Plants? {
99 bP) 99

Annelid markings,

32 ”

|
», burrows and castings. {
Dictyonema sociale, Salt. {
Trilobites, fragments of. {
Agnostus, sp. {
sf cyclopyge ?, Tullberg.
Olenus Nuneatonensis, Shar.
SSDs
5, NSalteri?, Call.

Lingula lepis ?, Salt.
Lingulella Nicholsoni, Call.

Obolelia granulata, Shar.

~
’
~
~

OS OS se sees ee SSS

» Sabrine?

Theca, sp.

~—

This list may be supplemented from the following specimens
which have been collected from the Stockingford Shales by Professor
Lapworth, and identified by himself.

1. PURPLE AND GREEN SHALES. Agnostus pisiformis, var.sociale, Tullberg.
Obolella sagittalis, Salt. Beyrichia Angelini, Barr.
ie Salteri, Holl. Leperditia sociale, Brogger.
Orthis lenticularis, Wahl. Lingulella Nicholsoni, Call,
2 Lingulella pygmea, Salt. (6) Upper zones.
Protospongia fenestrata, Hicks. 8
wae : pherophthalmus alatus, Boeck (8.
Serpulites fistula, Holl. eee Phill.). :
2, BLACK AND GREY SHALES. “A ' Agee, , Angelin.
nostus cyclopyge ullberg.
(a) Lower zones. 2 ye oes U8
Agnostus pisiformis (princeps, Salt.). 2 Hymenocaris.

Nearly all these fossils occur in some part or other of the Lingula
Flags. Protospongia fenestrata, Salt., occurs in the Harlech Beds, ‘and

1 This list was furnished to me in MS, by the kindness of Prof. Lapworth. He
remarks that Obolella sagittalis, Lingulella pygmea, and L. Nicholsoni, may be all of
them varieties of L. lepis.

and around the Warwickshire Coal-field. 549

in the Menevian of South Wales (Mem. Geol. Surv. vol. iii. p. 472).
Dictyonema sociale, Salt., is found in the uppermost Lingula Flags in
North Wales (7b. p. 536), in the Shineton Shales (Tremadoc) in
Shropshire, and at Malvern (Quart. Journ. Geol. Soc. vol. xxxiii.).
Agnostus princeps, Salt., occurs in the Upper Lingula Flags, and
Tremadoc Slate of North Wales, and in the Lingula Flags of South
Wales (Mem. Geol. Surv. vol. iii. p. 489), and Olenus Salteri, Call., is
common in the Shineton Shales of South Shropshire (Quart. Journ.
Geol. Soc. vol. xxxiii. p. 666). Lingula lepis, Salt., ranges from the
Lower Lingula Flags to the Arenig (Mem. Geol. Surv. vol. 111. p. 538),
but is commonest in the Tremadoc. Lingulella Nicholsoni, Call., and
Obollela Sabrina, Call., are common in the Shineton Shales (Quart.
Journ. Geol. Soc. vol. xxxiii.).

In Professor Lapworth’s list we find the following additional
forms: Obolella sagittalis, Salt., which occurs in the Menevian of
North and South Wales; QO. Salteri, Holl, known in the Upper
Lingula Beds of Malvern; Orthis lenticularis, Wahl., which occurs
in the Upper Lingula Flags (Dolgelly group of Belt); Lingulella
pygmea, Salt., of the Upper Lingula Flags; Serpulites fistula, Holl, from
the same beds near Malvern; Spherophthalmus ( Olenus) alatus, Boeck,
of the Upper Lingula Flags, and the black shales of Malvern; S.
flagellifer, Angelin, which occurs in the Lingula Flags, and is
believed to range up into the Tremadoc.

It may be concluded that the Stockingford Shales belong to a late
Lingula Flag age, including possibly a portion of the Lower Tremadoc
series.

The base of the Coal-measures.

The most southerly point at which the position of the base of the
Coal-measures has been definitely fixed is the colliery at Hawkesbury
Basin, previously alluded to. There the Silurian rocks (presumably)
were entered at a depth of 115 feet 5 inches below the Bench Coal, the
lowest seam worked in this coal-field. We next find evidence of its
position in the railway-cutting near Griff Hollow, as has been described.
But in the cutting at Chilvers Coton the junction is fully exposed to
view. A coal-seam is seen on the west side of the cutting 116 yards
north of the Accommodation Bridge (the second bridge south of
Chilvers Coton). This seam is underlain by three feet of white
fireclay, which rests upon about eight inches of sandstone. On
clearing the soil from the base of this sandstone, it may be seen that
it rests upon soft blue laminated shale, weathering yellow, and
obviously forming part of the same set of shales in which the
intruded diorites described above occur. The dip of the Coal-
measures is nearly in the same direction as that of the shales, but
is less rapid, so that by clearing a sufficient length of junction it
may be seen that there is an actual unconformity. The Coal-
measures occupy the cutting to a distance of 1380 yards south of the
Accommodation Bridge, where the Lower Silurian shales are brought
up again by a small fault running about 8. 35° H., the evidence for
the fault being the fact that the dip of the Coal-measures continues

550 Aubrey Strahan—Rocks beneath the Coal-measures

to be southerly, that is, towards the Silurian shales, close up to the
point where these shales reappear. This point is marked by slips
in both sides of the cutting, necessitating the covering up of the
side-drains.

From Chilvers Coton northwards there is no section showing the
base of the Coal-measures for nearly four miles, but its position is
indicated by the rise of the ground, where the harder Silurian shales
with the intruded diorites rise to the surface. There can be little
doubt that the Coal-measures rest almost directly upon the highest
beds seen in the Midland Railway cutting near Stockingford, for it is
known that the workable coal-seams crop out in the depression which
lies at the west end of the cutting. They are not exposed, but two
or three hundred yards south of the Accommodation Bridge there is
an old pit, now ploughed over, in which fragments of soft Carbon-
iferous sandstone occur, and which probably marks the position of
the boundary of these beds. On following the boundary northwards,
we find it marked by the outcrop of a seam of coal in the bed of
the stream west of Camp Hill, the hill itself consisting of the shale
with diorites, etc., seen in the western part of the railway cutting.
The coal-seams, which have been for the last two miles resting close
upon the Silurian shales, now begin to be separated from them by
beds which thicken steadily northwards. The nature of these beds
is first seen near Oldbury Hall. A pebbly sandstone dipping gently
to the west, and resting with a marked unconformity on the Silurian
shales, may be traced continuously from here to the Atherstone and
Birmingham high road. The rock is seen in the sides of a pond at
Oldbury (Farm) ; in the foundations of the farm west of Hopwood
Coal Wood ; in a sandpit near The Mawbournes; and in some old
quarries 200 or 300 yards further west in the edge of the wood.
The rock is buff-coloured or white, and so soft as to be readily
broken down into sand by the use of a pick. It is associated with
some mottled red and white clays, which are exposed in the brook
near the south-west corner of Hopwood Coal Wood, and were found
in laying the pipes of the Atherstone Waterworks along the lane
which passes the sand-pit. The red tinge, however, is not confined
to the lowest beds of the Coal-measures, but may be seen in many
of the fireclays associated with the workable coal-seams. The sand-
stone is seen again in the north part of Monks Wood in an old pit
close to a small quarry in diorite and Silurian shale, and again in the
side of the bridle-path leading into the high road, but from this point
northwards the beds which underlie the coal-seams rapidly disappear,
until the seams come down, as at Stockingford, close on top of the
Silurian shales.

The unconformity between the Coal-measures and the Lower
Silurian shales, which is generally masked on this side of the Coal-
field from the accidental parallelism between the bedding of the two
formations, is here very marked. The dip of the Coal-measures is
slight, ranging from 6° to 8°, while that of the Silurian shales ranges
from 20° to 40°. As a consequence of this the Coal-measures, where
they extend eastwards, at Mawbournes, overlap a great thickness of

and around the Warwickshire Coal-field. 551

the shales, including two sheets of igneous rock. The Pre-Carbon-
iferous age of the igneous intrusions, which might have been inferred
from their absence in the Carboniferous rocks and abundance in the
‘Lower Silurian shales, is thus placed beyond doubt.

On passing Merevale the lower beds of the Coal-measures again
thicken out rapidly, with the development of a pebbly sandstone at
the base as before. The best section of this basement bed is found
in the Baddesley Mineral Railway, but it may be traced from Mere-
vale Brook to a little north of Waste Hill.

Dosthall.

While Professor Lapworth was investigating the neighbourhood
of Nuneaton and Atherstone, the igneous rocks of Dosthill, on the
opposite side of the Coal-field, were visited by Mr. W. J. Harrison,
F.G.S., with the result of finding that shales similar to those of
Atherstone occurred here also.1. ‘The shales are first seen where the
footpath to Dosthill intersects the road to the Ford. They are
immediately overlain by a pebbly sandstone which forms the base
of the Coal-measures, and which may be traced southwards along the
west side of the lane, through the churchyard and neighbouring farm-
buildings. Immediately to the south of the village this sandstone
thins rapidly out, and the coal-seams come nearly, if not quite, into
contact with the diorite. But after passing the most southerly of
the igneous rocks, this sandstone reappears. There is no good
section in it, but its course can be followed without difficulty across
the ploughed land.

The shales are seen in the side of the high road a quarter of a
mile south of Dosthill; in a small pit near Stockall Barn ; in the
side of the high road again near the word ‘mill’; and lastly in the
brook which comes down from the Brick Works.” The dip is in all
cases towards the south-west, at angles varying from 20° to 40°, and
therefore in nearly the same direction as on the east side of the
Coal-field. The dip of the Coal-measures, on the other hand, is
towards the east, and generally at a high angle (from 50° to 80°),
so that the unconformity is most conspicuous. The shales are highly
altered grey and olive-coloured sandstones. No red beds are seen,
and at present no fossils except worm-tracks* have been found.
There is a strong resemblance, however, in these shales to the
Nuneaton and Atherstone beds, and there can be little doubt that
they also are of Lower Silurian age.

The Base of the Coal-measures continued.

The nature of the evidence, on which the base of the Coal-
measures has been drawn upon the map (now for the first time), has
been given:above. It has been shown that the actual base is formed
in some cases of a conglomeratic sandstone, with a considerable

1 Gron. Mac. 1882, New Series, Dec. II. Vol. IX. p. 565.

2 The position of the boundary fault of the New Red Marl is marked in this brook
by a rubble of diorite resting against red and white clay. Lumps of a white siliceous
yein-stuff containing specks of galena may be picked out of the white clay.

3 Harrison, Midland Naturalist, vol. viii. 1589.

002 Aubrey Strahan—Rocks beneath the Coal-measures

thickness of strata intervening between the coal-seams and the
Silurian platform, while in others the coal-seams appear to rest
almost directly upon this platform. The impersistency of these
lower beds led Professor Lapworth to conclude that the Stockingford
shales were brought “in a long-curved strike fault against the Coal-
bearing beds of the Upper Carboniferous.”! The same view was
taken by Mr. Harrison also, who writes that the line of fault between
the Coal-measures and the Stockingford Shales is “marked by a line
of brick-pits in which the rubbed-up material or ‘fault-stuff’ is
worked,” and again, in reference to Dosthill, that “on the west of
the hill . . . . a line of fault runs, by which the Triassic strata are
placed on a level with the Cambrian shales, while on the eastern
side a parallel fault of less ‘throw’ places the Coal-measures in a
similar position.” ?

The mapping of the boundary, however, about Oldbury, placed it
beyond doubt that in this neighbourhood it was not a fault, but an
unconformable superposition of the one series upon the other, while
the section at Chilvers Coton proves that the absence of the con-
glomeratic sandstone is due to attenuation and does not imply a fault.
Nor in the intermediate ground is there any reason to attribute the
varying distance of the seams from the top of the Silurian rocks to
a fault rather than to the known variability of the lower beds of the
Coal-measures, the material ‘referred to by Mr. Harrison as ‘ fault-
stuff’ being merely such fireclays and shales as are commonly found
in connection with seams of coal in the Coal-measures. The relations
of the Coal-measures to the Silurian platform appear to be exactly
paralleled by those of the Coal-measures of South Staffordshire to the
platform of the Upper Silurian rocks, on which they rest in that
county. Professor Jukes writes*® that “the Silurian rocks were
greatly denuded and worn away, and cliffs and hollows formed in
them, on, against, and over which the Coal-measures were deposited,
both lying in a nearly horizontal position” (p. 81) ; and again, “ We
have already, in examining the base of the Coal-measures, seen the
way in which at particular spots the lower beds of that formation
filled up hollows in the Silurian rocks and obliterated their little
pre-existing cliffs, and thus formed a smooth floor for the deposition
of the chief mass of the Coal-measure beds ” (p. 185).

These words describe exactly the manner in which the earlier
beds of the Coal-measures appear to have been laid down in
Warwickshire. We have here a platform of rocks varying in
hardness, and forming in consequence such peculiarly undulating
ground as is found near Merevale. At the commencement of the
Carboniferous period they must have presented just such a surface
for the reception of the first deposited sediments, the igneous rocks
standing up, as now, in small hills above the general level of the
shales, and it seems to have resulted from this that a thick mass of

1 Gzon. Mac. Dec. II. Vol. IX. p. 565.

2 Midland Naturalist, vol. viii. p. 72, 1885.

* The South Staffordshire Coal-field (Memoirs of the Geological Survey), second
edition, 1859. :

and around the Warwickshire Coal-field. 503

sandstones and clays was deposited at Oldbury and Waste Hill,
while the bosses of diorite, etc., about Merevale remained still
uncovered. Similarly, at Dosthill the diorite seems to have formed
a small elevated area, bare of sediment, while conglomeratic sand-
stone was being deposited on its flanks.

The Base of the New Red Sandstone.

From the south end of the Warwickshire Coal-field northwards
to Nuneaton, the New Red Sandstone (Waterstones) rests uncon-
formably, first on Coal-measures, then on the Silurian shales and
diorites, the junction being exposed in an old quarry at Marston
Jabet,! and in Wash Lane, Nuneaton. In both cases soft red and
white sandstone, based by an inch or two of breccia, is seen resting
on diorite and shale. The same boundary-line is seen again in the
Midland Co.’s Quarry near Nuneaton Station (Midland Railway).
The beds, which are flaggy and resemble parts of the New Red
Marl (into which the Waterstones shade insensibly), are seen resting
on a very uneven floor composed in part of a sheet of igneous rock,
and in part of quartzite. The hollows in this floor are filled with
a breccia of large fragments of quartzite, sometimes a foot across,
while three or four feet from the bottom of the red beds there is seen
a conglomeratic band containing well-rounded pebbles of quartzite,
from 4 to 1 inch in diameter.

From this point northwards, however, the boundary of the Trias
is shown as a fault. The evidence of this is given by Mr. Howell
as follows.2_ The coals were wrought in the old workings near Poles-
worth Station up to a “Red Rock Fault” and there entirely cut off.
Near Dordon the coals were found to be so much faulted that the
workings were not proceeded with. Lastly, a fault falling into the
same line is seen in a quarry in Merevale Park (p.50). The absence
of the Lower Keuper Sandstone (Waterstones) between Atherstone
and Nuneaton is also taken as evidence of a fault, and it may be
added that the nearly straight course taken by the boundary is in a
general way suggestive of a fault rather than of a natural super-
position. The existence of such a fault, however, has been questioned
by Mr. W. Andrews,’ and borings made since the date of the original
survey of the ground have proved that the fault, if it exists, has not
the importance which might have been attributed toit. For it might
have been supposed that the Coal-measures would occur beneath the
Red Marl on the east side of the fault, having been thrown down

e Rees, of the Warwickshire Coal-field (Memoirs of the Geological Survey),

. 39, fic. 4.

Py Geology of the Warwickshire Coal-field.

3 In a paper read at the Annual Meeting of the Warwickshire Naturalists’ and
Archeologists’ Field Club, 1884. A different view was taken by Prof. J. Phillips,
who refers to the ‘‘ curious circumstance, that the Nuneaton coal-field terminates on
the north-eastern [side] by a magnificent line of fault. It is one of the grandest
lines of fault which can be seen anywhere, and along that line of fault there are the
effects of metamorphosis; there are considerable bursts of trap-rock’’ (Coal Com-
mission Report, 1871, vol. ii. p. 494). ‘The trap-rock referred to appears to be the

Caldecote Volcanic Series, which is of course of vastly greater antiquity than the
fault.

504 Aubrey Strahan—Rocks beneath the Ooal-measures

with this rock against the older Paleozoic strata. The absence of
Waterstones, moreover, does not necessarily imply the presence of a
fault, for these beds constitute merely the earlier and more sandy
sediments of the New Red Marl, and are known to be quite un-
represented in some other localities where the Red Marl mantles
round bosses of old rock, as at Croft, Sapcote, etc.

That there is a fault, however, along the northern part of the
coal-field appears to have been proved, and that it extends south-
wards as far as shown, though perhaps with no great throw, seems
probable. Near Hartshill Wharf is a quarry in quartzite in which
the base of the Trias is seen, the lower beds consisting of about
three feet of sandstone, overlain by about three feet of marl, and
lying upon the quartzite. The beds undulate and when last seen are
dipping steeply, as though near a fault. If there is a fault here,
the Triassic beds seen must be on the west or upthrow side. The
section proves therefore that the Trias rests upon the quartzite here,
without any of the Coal-measures intervening.

At the brick-pit near the canal by Nuneaton Midland Station, the
Red Marls are seen with a dip ranging up to 85°. The quartzite
rises to the surface close by, but the junction is not exposed. The
steepness of the dip of the Marl, however, points to the boundary
being probably a fault.

We have, then, four instances in which the Trias is seen resting
directly upon the Silurian rocks, namely, Marston Jabet, Wash Lane,
the Midland Co.’s quarry, and Hartshill Wharf. This evidence
alone would have been sufficient to indicate that the Trias of the
great plain on the north-east of the Warwickshire Coal-field would
probably be found to rest in great part on the older Paleozoic rocks,
and not on Coal-measures, especially when it is remembered that the
nearest exposure of Paleeozoic rock to the east (namely, at Sapcote)
shows syenite rising through the Marl. But this conclusion has
been placed beyond doubt by the results of borings, some of which
have reached the base of the Triassic rocks, and proved the depth to
the Paleozoic floor. The following is a list of those which bear
upon the district under consideration.

Hawkerspury Pumpine Srarron; about five miles south of Nuneaton. 252 feet

above Ordnance Datum.1
DUE Cee cach ee Pee ee oe RAN 99 lo an eco eld Oa eae 30 feet.

120 ,,
Tue Wurre Stonz, about 2% miles south-east of Nuneaton, A well to a depth of
80 feet, a borehole to a further depth of 50 feet. Height above Ordnance
Datum about 250 feet.?
White sandstone and red shale [Waterstones] ............ 60 feet.
Hard mottled blue and purple shales .......cs00seseeeeees ALOT IRS

130 ,,

1 Report of the British Association for 1875 (Report of the Committee on the
Circulation of Underground Waters), pp. 185, 136. For the Nuneaton boring see
also Report for 1878, Report on the Circulation of Underground Waters, p. 7.

* The details of this section were given me by Mr. W. Andrews. The Water-
stones are well exposed in a quarry by the side of the L. and N. W. Railway, near
Attleborough.

and around the Warwickshire Coal-field. 505

At the time of my visit, April, 1886, the débris from the pit was
in a fresh condition. The character of the shales left no doubt that
they were of Silurian age, and probably of the same age as those
that crop out at Marston Jabet. Some of the fragments were inter-
sected by veins of gypsum, doubtless derived by infiltration from
the Trias above. No fossils have been found.

Nuneaton: centre of the town. 210 feet above Ordnance Datum.!

Wriko (Sand, oravely andsclay)eu-.cececesceecaeoscaccoceee see 18 feet.
Red Marl sac we reece eecetrecrec sas sesceness eo nsevanescenesecvecces 12 9
Lower Keuper Sandstone [Waterstones] ..........20.s006+ SOlmes:

Hard slaty white rock [probably Hartshill Quartzite]... 2

Tear

Linptry Hatt Estate; boring near the Fenn Lanes. About three miles north
of Nuneaton.

Soil} red clay, ete:5 (Drift) oes. cc sccnccnseccecesseseosaece 6 feet.
Red marl with red and blue rock and gypsum ..........4 456 ,,
Blue, red, and brown rock with marl, probably Water-
BUDE agg g000caCCOOOCOOOODHOD, HOCOSODNCOOCOUSOOODEONEOCO00000 IG v
643 ,,

Hincktey Wuarr, about three miles east-north-east of Nuneaton, 313 feet above
Ordnance Datum.!

Glacial Drith -....2- Sands and Boulder-clay) <2 scccsccsc--ace-nesseceecccsecssese 88 feet.
ed) Maris’ ....-.-..--. Red gypseous marls with bands of grey sandstone ... 408
Waterstones .........Red, grey, and brown sandstones with bands of marl 209

705 ,,

This boring is nearly midway between the exposures of Paleozoic
rocks at Nuneaton and Sapcote, and is probably near the deepest part
of the trough of Triassic rocks separating these localities. It shows
that the lower sandy beds of the Red Marls, which are distinguished
by the name of the Waterstones, increase rapidly in thickness on
receding from the old land-barriers or islands, formed by the harder
parts of the Silurian and pre-Silurian series. In this they may be
compared to the impersistent sandy and conglomeratic beds which
form the base of the Coal-measures, as previously described.

Hincxzy; at the Holy Well, 330 feet above Ordnance Datum [should be 421].?

Drift (pebbly clay, sand, and gravel)........sssesssseseeeor 150 feet.
HRedsim arly oj aesoaeneemeencwecies asiom ates ebeee aoe aeaeslnesaee sien 20) 55
Lower Keuper Sandstone (viz. thin beds of clay and

gypsum alternating with thick beds of red, grey,

and white sandstone) [Waterstones] .....0.seseeseseee SOs

540 ,,

1 Report of the British Association for 1882. Report on the Circulation of Under-
ground Waters, pp. 14, 15, where the section is given in full.

2 Report of the British Association for 1875 (Report of the Committee on the
Circulation of Underground Waters), pp. 136,137. Fora further account of the
Hinckley Boring see Report for 1879, p. 160.

556 A, Strahan—The Warwickshire Ooal-field.

EtmestHorPe Borine, at Sapcote Freeholt, two miles east of Hinckley and two
miles west of the syenite boss of Sapcote. 300 feet above Ordnance Datum.!

UTE sae seks taatar senec secre senacanse seetacerensareesestenetace: 10 feet,
Rede Mar eee. uy a atk Renee odec gel ee, stay Rae i20ieee
Lower Keuper Sandstone [Waterstones] .......se.eeseeees 330 ,,
Slaty rocks with a dip of 70°, Lower Silurian? ,........ 980 ,,
1440

This boring appears to have subsequently reached a depth of 1655
feet from the surface without meeting any change of ground.

Liyprivcr Coriiery Company (Landridge ?), one mile north of Desford. 400 feet
above Ordnance Datum.?

Drittj Fs sinuaht hacnten oanotnstramenate ace neces venaean cea acaan aes 2 feet.
Upper Keuper Sandstone................ bhonoeobonnceacoa9Nc04e 20 5
Red Marl (marl with thin bands of gypsum) ..........+ 44 ,,
Lower Keuper Sandstone. Waterstones .......sssccseeees 204 ,,
BHO 55

Newton Unruanx, near Desford Station. One mile and a quarter E.S.E. of the
Lindridge section, 320 feet above Ordnance Datum.

DD PUTh ses eat re heen AL eee TORE, HEOELEO ET Lee 6 feet.
Upper Keuper Sandstone and Marls ..........c0cecsseseraee 56 ,,
Red Marls with sandstone ...........cecoscsccececasecsacce see 80 ,,
Wialerstonest st. ketre oct tice a Net drctMe a cena cena oe enue 120 5;
Coal-megsuresplitl|iasvsoccsnestessscrscerserseeeer ens raceer tenes 353 4,
615 ,,

There have been also borings, of which details are not forthcoming,
at the undermentioned localities :—

Near Kingshill Spinney, one mile and a half south-west of Market Bosworth,
ending at a depth of about 672 feet, probably in Waterstones.

At Bosworth Wharf, one mile west of Market Bosworth.

At Cowpasture, three-quarters of a mile north-east of Market Bosworth, said to
have entered Cambrian or Lower Silurian rocks at 400 feet.

Near Gabriel Pool, # of a mile N.N.W. of Newbold Vernon, to a depth of 266 feet.

Newbold Heath, half a mile W.8.W. of the Landridge boring mentioned above, in
which Coal-measures were said to have been proved at a depth of 400 feet.

There can be little doubt therefore that, as pointed out by Mr.
Harrison,‘ the Trias rests directly upon rocks older than the Coal-
measures over a large part of the area. Whether or no the Coal-
measures were ever deposited continuously over the area remains
an open question. It is certain that the Silurian rocks had suffered

* The lower part of this subdivision was attributed to the Permian by Sir Andrew
Ramsay, who gave the following details (Report of the Coal Commission, 1871, vol.
il. p. 184) :—

(Tooseysandstone:snecy.cs-nnsesuccseeesccecsesn ences 64 feet.
j’ Hardisamdstoney..sc.8).ceessevesceereneerere eee IY 5.
Permian ......¢ Light and dark sandstone........ccccsssseeesees 43 5,
Pebbles, hard conglomerate ........s.cessceseees Di iis
Pink and purple marls .............. “nonsoned eon 15 ,,

Coal-measures [now known to be Silurian or of earlier age]..—
1

* Report of the British Association for 1875 (Report of the Committee on the
Circulation of Underground Waters), p. 137.

3 Report of the British Association for 1878 (Report on the Circulation of Under-
ground Waters), pp. 6, 7.

* Midland Naturalist, vol. viii, (1885),

F.. Rutley—Igneous Rocks of the Warwickshire Coal-field. 557

enormous denudation in pre-Carboniferous times, so great indeed as
to remove the whole of the series, consisting in the aggregate of
several thousand feet of rock, from parts of Leicestershire. And it
is probable that in the period of submergence that succeeded this
continental epoch most of even the higher parts of the old land-
surface in this neighbourhood were overspread by the latest Coal-
measure sediments. But, however this may have been, the Carboni-
ferous rocks were swept bodily off large areas in the Midland Counties
in the long period of denudation which preceded the Trias. There
are therefore two questions to be taken into consideration, in specu-
lating on the possible presence of Coal-measures under the Trias at
any point in the Midland Counties: firstly, whether the Coal-measures
ever existed at that point; secondly, whether, having existed, they
were subsequently removed by pre-Triassic denudation. Itis scarcely
possible to attach too much importance to the study of the great
unconformity at the base of the Trias. In the present instance
it seems certain, that though the Coal-measures may have been
deposited in a continuous sheet between the Leicester and Warwick
Coal-fields, they were certainly swept clean off, as far north as
Market Bosworth and perhaps further, before the Waterstones and
Marls were deposited.

AppENpDIx I.

Iil.—Tue Igneous Rocks, erc., or THE NEIGHBOURHOOD OF THE
WARWICKSHIRE COAL-FIELD.

By Frank Ruttey, F.G.S., ete.

HESE rocks may be classed into five or six more or less
distinct groups.
1. Syenitic Rocks (Croft Series).

1. Andesite and Andesitic Tuffs (Caldecote Series).

wi. Hartshill Quartzite with Breccia at its base.

tv. Diorites.

v. Andesites or Diorites containing Augite.

vi. Basalts or Diorites containing Olivine.

The three last groups appear to graduate into one another, and
seem to correspond with similar rocks described by Mr. Allport.’
Many of the specimens examined are in a more or less advanced
stage of decomposition, calcite, serpentine, pyrites, etc., being very
commonly present.

The best example of diorite in the series is that from the Oldbury
Reservoir. ‘These rocks are of special petrographical interest since
so few diorites have been found in England. The mineral constitu-
tion of some of these rocks is such that they are also interesting from
the transitional characters which they present between diorite, basalt
and andesite or diabase. The pseudomorphs after olivine met with
in the sections of rock here described might rather, as a rule, be
called metasomata, since well-developed forms of the original crystals

1 On the Diorites of the Warwickshire Coal-field, Q.J.G.S. vol. xxxy. p. 637.

558 F. Rutley—Igneous Rocks of the Warwickshire Coal-field.

are often wanting, and it is seldom that any unaltered olivine is
present. The replacing substance is frequently calcite. Accepting,
therefore, the conclusions of Allport, who was fortunate in finding
good crystals of unaltered olivine in some of the dioritic rocks of
this district, and coupling them with such evidence of the former
presence of this mineral as the sections, here described, afford, there
seems little doubt that we have, in some cases, rocks which may
often, with equal justice, be termed either olivine-bearing diorites or
hornblendic basalts. On the other hand, the association of augite
with hornblende in some of these rocks, also described by Allport,
gives rise to a like ambiguity, since in these we may have either
hornblendic diabases or andesites, or augitic diorites.

The term augite-diorite has already been employed by Zirkel,! and
its use advocated afresh by Grenville A. J. Cole.2 The sanction of
such a term, although its meaning is evident and not opposed to the
observed mineral constitution of these rocks, may however, lead to
some present confusion in petrological nomenclature, since the cur-
rently accepted definition of a diorite indicates that the constituent
minerals are essentially triclinic felspar (labradorite or oligoclase)
and hornblende. The important point in naming rocks of this mixed
character is to indicate their relationship on either hand to sharply
and of course arbitrarily defined rock types when their position is so
evenly balanced between two types that the rock cannot be referred
to the one type more than to the other, and, to indicate this, I would
suggest that the names of the two nearest types should be combined,
a preponderating affinity towards the one type or the other being
denoted by underlining the name of the dominant type. Thus in the
case of those olivine-bearing rocks which approximate on the one
hand to diorites and on the other to basalt, we should have

Diorite. Diorite-Basalt. Diorite Basalt. Diorite-Basalt. Basalt.

A nomenclature based upon mineralogical terms only is never likely
to be adopted, since it is far too cumbrous. Rock-names taken singly
fail to indicate transitions in mineral constitution, while a mixture of
mineralogical and petrological names at once impairs the needfully,
but unnaturally sharp definition of a type. It therefore seems better
to employ already well-known words and preserve, so far as possible,
the landmarks of classification, than to destroy the meaning of a
term by a mineralogical prefix or affix which in conveying a small
truth may breed a great misconception. If, for instance, augite or
olivine were assumed to be anything more than occasional and
subordinate constituents of a diorite, the commonly accepted definition
of that rock would become worthless, since the term diorite would
then embrace a number of rocks of far greater importance and wider
distribution, which have hitherto been distinguished by other names.
That a relationship exists between such rocks, and that they
graduate one into another, is too well known to need any comment,
1 “«« Lehrbuch der Petrographie,”’ vol. ii. p. 7, Bonn, 1866.

2 «<The Igneous Rocks of Stanner,’ Guot, Mac. Decade ITI. Vol. III. p. 225
(May, 1886),

F, Rutley—Igneous Rocks of the Warwickshire Coal-field. 559

but, to have classification, more or less clear definitions must be
employed; without these the whole series of basalts, andesites and
diorites may as well be called Greenstones.

1. Syenitic Rocks.
Croft.’

Pinkish-grey crystalline rock, resembling a fine-grained granite
and apparently composed of pinkish or flesh-coloured felspar, a very
little dark mica, quartz, and some dark specks of hornblende and
magnetite. Under the microscope the rock is seen to have a holo-
crystalline granitic structure, and to consist chiefly of orthoclase
and triclinic felspars, quartz, hornblende and magnetite, with pos-
sibly a little magnesian mica. The amount of triclinic felspar
present renders it necessary to distinguish this rock from an ordinary
quartz-syenite. It is an orthoclase-plagioclase syenite, in other
words it occupies a position between quartz-syenite and quartz-diorite.

Croft.

A pinkish-brown crystalline rock with numerous white, porphyri-
tic crystals seldom over one-eighth of an inch in diameter, and small
dark greenish-black and black specks. The specimen has a weathered
appearance.

Under the microscope it is seen to consist of orthoclase, a triclinic
felspar, which from some of the extinction angles seems to be albite,
hornblende in small irregularly developed crystals which are some-
times represented by serpentinous pseudomorphs and crystals and
irregular grains of magnetite. Quartz occurs plentifully. The rock
is essentially a quartz-syenite. It is a more coarsely crystalline
rock than the preceding.

Croft.

A purplish or reddish-grey, fine-grained crystalline rock, with
dark brown spots ranging up to an eighth of an inch in diameter.

Under the microscope the chief constituents are seen to be
felspars, all of which are greatly altered, so that their optical charac-
ters afford no clue to the species, quartz, serpentine, apparently
pseudomorphous after hornblende, and ilmenite partly converted into
leucoxene.

The rock seems to be a decomposed, fine-grained, quartz-syenite.

1. Andesite and Andesitic Tuffs, Caldecote Series.
Old tunnel, near Caldecote Hill.? Caldecote Series.

A finely-laminated greenish-brown rock, resembling a fine-grained
sandy-mudstone or slate. Thespecimen is bounded by parallel joint-
planes. Under the microscope, with a power of about 75 linear, a
considerable proportion of the rock appears between crossed Nicols
to consist of isotropic matter finely stippled with very minute doubly
refracting granules and traversed by irregular wavy films of a ser-
pentinous or sericitic substance, which commonly runs in sinuous

1 See also ‘On the Pre-Carboniferous Roeks of Charnwood Forest,” by the Rey.

T. G. Bonney and Rey. E. Hill, Q.J.G.S. vol. xxxiv. pp. 119-289, 1878.
2 See also T. H. Waller, Gzox, Maa. 1886, p. 323.

560 F Rutley—Igneous Rocks of the Warwickshire Coal-field.

streaks approximately parallel to the lamination of the rock. The
entire section is profusely spotted with small crystals and fragments
of crystals of felspar and augite, the latter mineral being usually
represented by pseudomorphs of limonite. Some of the sections of
augite crystals undergo maximum extinction at an angle of about
39° from the vertical axis, while other sections transverse to the
vertical axis show approximately right angles formed by the adjacent
faces of the oblique rhombic prism. The felspars are generally
labradorite. Taking into consideration all the characters presented
by this rock, it seems highly probable that it is an altered andesitic
tuff.

“Blue Hole,” east of Caldecote Windmill. Caldecote Series.
(The Quartz- Porphyry.)

Rock composed of pink and greyish-white crystals of triclinic
felspar with grains of quartz, in a dark bluish- or brownish-grey
matrix, the latter constituting the smaller proportion of the rock.

Under the microscope the general appearance is that of a tuff,
composed of crystals or fragments of crystals of triclinic felspar and
quartz more or less corroded, together with fragments of eruptive
rock of an andesitic type, containing serpentinous pseudomorphs
after pyroxene. The porphyritic felspar crystals, all of which have
their angles rounded, are often corroded superficially and their angles
of extinction indicate, as a rule, that they are labradorite. The
quartz crystals are also rounded, and frequently show inlets of corro-
sion, which are much more strongly marked than in the felspars.
The material in which these crystals and fragments are embedded is
felsitic in character, and as it seems to be continuous with the felsitic
matter which fills the corrosion-creeks in the quartz-crystals, it
appears probable that it may be a product of devitrification, and that
the rock is a tuff resulting from fragments taken up in a magma
which, on solidification, assumed a vitreous condition. The general
appearance of this rock under the microscope is rather lke that of
certain porphyritic pitchstones occurring in Saxony, except that in
the latter the porphyritic crystals or fragments are usually less
numerous and the ground-mass retains its glassy character. It seems
probable that this rock from Caldecote is part of a lava-flow or dyke
which has taken up fragments of other rocks in such quantity that
it simulates an ordinary volcanic tuff.

“Blue Hole,’ east of Caldecote Windmill. Caldecote Series.
(Junction of Quartz-Porphyry and Andesite).

Compact bluish-grey to brownish-grey rock with splintery fracture.
The small specimen contains in one part greyish-white to pinkish-
white specks of felspar, the largest being about +s inch in diameter.
Minute grains of quartz are also visible with a lens.

Under the microscope, between crossed Nicols, the section seems
to consist chiefly of a crypto-crystalline to micro-crystalline ad-
mixture of felspar and quartz, with some irregularly-shaped and
usually rounded grains which, by ordinary transmitted light, appear
of a brownish-green colour, and which are probably altered fragments

1 See also T. H. Waller, Grou. Maa. 1886, p. 3238.

F. Rutley—Igneous Rocks of the Warwickshire Coal-field. 561

of crystals of pyroxene or amphibole. A similar green or brownish-
green substance (chlorite ?), accompanied by minute specks of opaque-
white matter (kaolin), constitutes irregular stringy markings and
sinuous bands, which traverse the section, in some cases simulating
fluxion structure, the material between such bands sometimes differ-
ing in texture from that on either side. This seems to be due to the
presence of fragments of rock, whose margins are ill-defined, except
through the contact of the chloritic films and strings. Small angular
and rounded fragments of felspar crystals are plentifully distributed
throughout the section, and here and there opaque grains of ilmenite,
partly converted into leucoxene, are visible.

The porphyritic crystals and fragments of crystals of felspar
mostly give extinction angles approximating to 40°, and may therefore
be regarded as anorthite. In a few cases, however, labradorite
occurs.

Judging from the section, it seems probable that this rock is a
tuff composed of lapilli of some rocks allied to andesite or porphyrite
in which the ground-mass was once vitreous or partly so.

“Blue Hole,” east of Caldecote Windmill.1 Caldecote Series.
(Andesite. )

Compact purplish-grey rock, in which a few minute felspar crystals
may be detected with a lens.

Under the microscope the section is seen to consist of crystals of
triclinic felspars and magnetite in a felsitic or aphanitic ground-
mass. in which numerous very minute crystals occur, which are
apparently hornblende, since in some cases they give an extinction
angle of 19°.

If these small crystals be hornblende, the rock is probably a horn-
blende andesite. It is somewhat decomposed, the specimen effer-
vescing slightly when treated with acid. Isotropic matter seems to
be present and it is quite possible that the rock may have originally
possessed a more or less glassy ground-mass, some of the unaltered
vitreous matter being apparently still present.

11. Hartshill Quartzite with Breccia at its base.
Base of Hartshill quartzite, half a mile S.E. of Hartshill.

A coarse breccia consisting of angular fragments. embedded in a
bluish-grey to purplish matrix. On a cut surface of the specimen
some of the fragments are of a dark slate-colour or purple, while
others are of a rather pale greenish-grey. The fragments do not
seem to exceed half an inch in diameter, and most of them are of
much smaller dimensions.

Under the microscope the fragments are seen to be of a mixed
character. A few consist of eruptive rock, one or two showing distinct
felspar crystals (labradorite), while one fragment contains small
vesicles filled with a pale green substance (chlorite?). Quartz
prains constitute a large proportion of the rock, and most of the
other fragments and grains consist either of greatly decomposed

1 See also T. H. Waller, Grou. Mac. 1886, p. 824. The Dark Basic Rock.
DECADE III.—VOL. III —NO. XII. 36

562 F. Rutley—Igneous Rocks of the Warwickshire Coal-field.

felspar, converted into felsitic matter, or fragments of quartzite, and
fragments of slate, together with grains of magnetite. The fragments
of volcanic rock appear to be of an andesitic type. The slate frag-
ments are the largest and the most numerous.

Hartshill Quartzite.
A very fine-grained pinkish-grey rock resembling quartzite.

Under the microscope the rock appears to consist chiefly of
irrecular crystalline grains of quartz containing numerous minute
fluid lacunz, with a few grains of felspar, which from the extinctions
are seen in some cases to be microcline, in others anorthite. Grains
of a clear, colourless, isotropic mineral are also present, which are
probably garnet. Here and there but quite rarely a little micro-
crystalline siliceous matter may be seen lying in thin films or occupy-
ing small spaces between the quartz grains. The rock is essentially
a quartzite.

rv., v. and vr. Diorites; Andesites, or Diorites containing Augite ;

Basalt, or Diorites containing Olivine.’
The specimens are taken in geographical order.
Marston Jabet. Intrusive in Lower Silurian Shales.

A rather coarsely crystalline greenish-grey rock, consisting of
greyish crystals of felspar, a dark green mineral, calcite and specks
of pyrites.

Under the microscope the section shows, triclinic felspar crystals
(labradorite), serpentinous matter pseudomorphous after hornblende,
the crystals being frequently about =; inch in diameter and giving
in sections transverse to the vertical axis the usual prismatic angle
for hornblende. These pseudomorphs are mostly flecked with an
opaque yellowish-white substance probably leucoxene. Well-defined
pseudomorphs of leucoxene after ilmenite are also present, the altera-
tion being so complete that scarcely a trace of the original mineral
remains. Spots of pyrites and large patches of calcite occur, and
serpentine, frequently fibrous and in spherical groups of divergent
fibres, often fills the spaces between the larger crystals. Apatite is
also plentiful in well-formed crystals. The rock is a diorite, as
pointed out by Mr. Allport in the paper already cited, where descrip-
tions of the microscopic characters of this rock in its fresh condition
and in various stages of alteration are very clearly given.

Griff Farm (South of). Intrusive in Lower Silurian Shales.

A bluish- to brownish-grey crystalline rock containing specks of
pyrites.

Under the microscope this is seen to be composed of crystals of
labradorite and hornblende with a considerable amount of serpentine
ora pale greenish substance which appears to be serpentine, and
which occasionally occurs in small spherical or fan-like fibrous

1 See also T. H. Waller, Grou. Mac. 1866, p. 235. The Quartzite.
2 See also J. J. H. Teall, Hornblende-Bearmg Rocks, Grou, Mac. 1886, p. 3dl.

F. Rutley—Igneous Rocks of the Warwickshire Coal-field. 563

aggregates. There is also some calcite present, the rock effervescing
briskly when touched with acid. It is a diorite.

Chilvers Coton Railway-Cutting. A sheet three inches thick in
Lower Silurian Shales.

A greenish-grey or greyish-green rock of very fine texture, pro-
fusely speckled with dark-green crystals and containing much
pyrites, crystallized in cubes.

Under the microscope this rock appears to consist of pale green
serpentinous matter with interlacing sheaf-like aggregates of small
slender acicular crystals, having frequently rather ragged boundaries.
These crystals often undergo extinction at an angle of 19° from their
longest diameter, and it may be assumed from this and from their
pleochroism that they are hornblende. There appears to be very
little felspathic matter in this rock. There are, however, a few im-
perfectly formed crystals of labradorite present. The serpentine
may possibly be pseudomorphous after olivine, but the sections are
very irregular in form, and there is no positive evidence upon this
point. A few grains of augite are visible in this section, as well as
irregularly-shaped patches of pyrites.

Chilvers Coton Railway-Cutting. Intrusive in Lower Silurian
Shales.

A medium-grained crystalline rock of a pinkish-grey, closely
speckled with dull green crystals and containing minute specks of
pyrites.

Under the microscope it is seen to consist of triclinic felspar,
hornblende, rather sparsely distributed grains of magnetite and
pyrites, a very few minute crystals of apatite and some isotropic or
nearly isotropic matter, which may represent an interstitial glass.
The felspar appears as a rule to be labradorite. The rock is essen-
tially a diorite.

Chilvers Coton Railway-Cutting. Intrusive in Lower Silurian
Shales. Three feet from top of dyke.

A greenish-grey crystalline rock of fine texture, containing
numerous minute specks of pyrites.

The constituents of this rock appear under the microscope to be
triclinic felspar (labradorite), serpentine, apatite pyrites, and a little
unaltered augite. The serpentine, which is very plentiful in the
section, may be an alteration product after augite or after some other
mineral, but upon this point the section affords no trustworthy
evidence. The rock is probably some kind of andesite.

Midland Quarry, Nuneaton Station. Intrusive in Hartshill Quartzite.

A very fine-grained purplish-grey rock showing under a pocket-
lens a small quantity of a light-green mineral resembling epidote
and minute octahedra of magnetite. The specimen attracts the
magnetic needle.

Under the microscope the constituents are seen to be triclinic
felspar, augite, olivine, magnetite, and serpentine, the latter sub-

564 FF. Rutley—Igneous Rocks of the Warwickshire Coal-field.

stance being probably pseudomorphous after olivine. A few fan-
like or divergent groups of capillary crystals occur here and there in
the section. They undergo extinction approximately parallel to the
longest axes of the minute rods, and are probably epidote. The
magnetite occurs in irregularly-shaped grains and in well-developed
octahedra. A little hornblende may be present, but the evidence for
this is not satisfactory. The rock is a diabase.

Stockingford Cutting, Midland Railway (EK. of bridge). Intrusive
in Lower Silurian Shales.

A very fine-grained, greenish-grey crystalline rock, containing
small spots and very numerous minute specks of pyrites. The rock
effervesces freely when touched with acid.

Under the microscope it is seen to consist of triclinic felspar
(labradorite), serpentine often in pseudomorphs after olivine, horn-
blende, pyrites, calcite, and specks of a yellowish white substance,
either kaolin or leucoxene, but probably the former. It is difficult
to say whether this rock is to be regarded as a basalt or a diorite.
The occurrence of olivine in dioritic rocks from this neighbourhood
has already been noticed by Mr. 8. Allport.’

Midland Railway, Stockingford Cutting, Nuneaton. Upper surface
of dyke intrusive in Lower Silurian Shales.

A very fine-grained greenish-grey or drab-coloured crystalline
rock, showing numerous minute specks of pyrites.

Under the microscope the constituents appear to be chiefly triclinic
felspar, serpentine pseudomorphous after hornblende, a very little
unaltered hornblende and a considerable quantity of pyrites, some
ot which occurs in triangular sections which give angles of approxi-
mately 110° (the angle formed by the edges of an octahedron). It
therefore seems probable that the pyrites in this case is pseudo-
morphous after magnetite, and this appears the more likely since no
magnetite is visible in the section, although the rock is one in which
this mineral is generally present. So far as I am aware, pseudo-
morphs of pyrites after magnetite are of very unusual occurrence,
but instances are quoted by Delesse.? The rock is a diorite.

Oldbury Reservoir. Very thick sheet intrusive in Lower Silurian
Shales.

A greenish-grey crystalline rock, spotted with numerous dark-
green or blackish crystals of hornblende. It also shows many
specks of pyrites and the joint planes are coated with calc-spar.

Under the microscope the rock is seen to be composed of triclinic
felspar, crystals of hornblende, larger than those seen in the rocks ~
already described, and exhibiting the interrupted crystallization,
sometimes termed ophitic, a considerable quantity of kaolin, specks
of pyrites and also a little calcite. The rock is a diorite.

1 Quart. Journ. Geol, Soc. vol. xxxv. p. 639.

2 Récherches sur les Pseudomorphoses, Tableau II. p. 52, Annales des Mines,
t. xvi. 1889.

G. Sharman—New Species of Olenus and Obolella. 565

Dosthill (intrusive in Lower Silurian Shales).

A fine-grained greenish- to greyish-brown crystalline rock.

Under the microscope it is seen to consist of more or less imper-
fectly developed lath-shaped crystals of triclinic felspar, which, from
the extinction angles of some of them, appear to be labradorite,
octahedra and irregularly-shaped grains of magnetite, apatite and
pseudomorphs of serpentine, apparently after hornblende, since the
angles of some of these pseudomorphs correspond with the angle of
the oblique rhombic prism in hornblende.

The rock may be regarded as an altered diorite.

AppPenpix II.

TV.—On tut New Sprzcres Ozewus Nuwearovewsis aND OBOLELLA
GRANULATA, FROM THE Lower SinuRIAN (‘Camprian, Lap-
WORTH), NEAR NUNEATON.

By Gzoree SHarman, Esq.
Olenus Nuneatonensis, 8., sp. nov.

Locality.— West end of the Midland Railway cutting, between
Nuneaton and Stockingford.

Several fragmentary specimens of this Trilobite, differing in size,
yet exhibiting similar characters, have been collected from this locality.
The most perfect, although one of the smallest, is best fitted for
description.

The length of this specimen is three-eighths of an inch, and the
head, or cephalic-shield, is rather more than one-third of the entire
length. The glabella is very convex, slightly narrowing in front,
but inflated and bending over the frontal margin. The neck-furrow
is distinct, the basal groove runs across the glabella, and there appear
to be two short indistinct furrows on each side. There are eleven to
thirteen body-rings, the pleurz of the 5th, 6th, and ‘th bearing
short spines, and the 8th possessing a produced spine half as long
as the specimen itself, and projecting beyond the end of the tail. The
four terminal segments of the body also have spines, lessening in
length towards the tail. The tail is short, the axis showing it to be
composed of three, or perhaps more segments ; it narrows posteriorly,
and is subtruncate, being indented as in O. micrurus.

This species is distinguished from O. micrurus by the more
lengthened spines from the posterior angles of the cheeks, and the
possession of those attached to the pleure of the lower segments of
the body, the nearer approach and bending over of the glabella
towards the anterior margin, the continuance of the basal groove
across the glabella, and in the anterior portion of the body being
more parallel-sided. The character of the tail appears in all respects
to agree with that of O. micrurus.

It is distinguished from O. bisulcatus, Phil., by the absence of the
mesial spine on the cephalic-shield.

The marked difference in the size of these Trilobites (as before
mentioned) would undoubtedly suggest the probable presence of two

566 Dr. H. Hicks—The Ffynnon Beuno and Cae Gwyn Caves.

species, yet after a careful examination of the larger specimens,
which are unfortunately only fragments, the characters appear to be
the same as those of the smaller ones just described, and therefore, until
better specimens can be found, they are regarded as the same species.

Obolella granulata, S., sp. nov.

Locality.—Lane on the south side of Purley Park, near Atherstone.

Only two specimens have been collected by the Survey, and
although somewhat imperfect, yet they exhibit characters separating
them from previously described species.

On first viewing the specimens, the form and general appearance
of Siphonotreta is strongly suggested, but the structure and orna-
mentation is found on closer examination to differ considerably from
it; radiating ribs apparently underneath the general surface of the
shell are clearly seen extending from the beak towards the margin,
and these commencing and terminating irregularly, none however
quite reaching from the beak to the margin of the shell.

The surface of the whole shell is minutely granulated, giving an
appearance of very fine concentric wavy lines. The umbonal region
not being quite perfect prevents any definite determination of the
genus, but provisionally it is placed with Obolella.

V.—On tHE Frynnon Bruno anp Caz Gwyn Caves.
By Henry Hicxs, M.D., F.R.S., F.G.S8.

HE best reply that I can make to Prof. Hughes’ remarks, in the
GxrotoctcaL Magazine for November, on the Ffynnon Beuno
Caves, is to publish the substance of the report presented to the
British Association, especially as an opportunity will be given to
those interested in the inquiry to examine the section during the
further explorations to be carried on, probably in the month of June
next year. Some of his statements—especially as regards the position
of the fence, which is entirely at the opposite end of the cavern to
that at which the flint flake was found, also as to the position of the
flake, and the nature of the deposits overlying it—are so entirely
misleading, that I can only account for such statements being made
by the fact that Prof. Hughes did not visit the section, though
strongly urged by me to do so, until it had been almost entirely
covered over, and work for the time suspended, and by his hasty
survey of the surrounding conditions.’ That such experienced
1 Tt is surprising that Prof. Hughes did not recognize that the accumulation against
the upper side of the old fence, ‘‘ until there is now a drop of eight feet to the level of
the ground on the lower side of the fence,’’ mentioned by him as of such great im-
portance, is merely material conveyed there during the explorations. Before work
was commenced, the space between the old fence and the entrance was almost bare
rock, and there was nothing resting against the fence. No wonder then that he should
have come to the conclusion that this was remanié drift, and that he thought he recog-
nized on some of the stones “ traces of agricultural implements as well as true Glacial
strie.”” The remarkable thing is that he should not have recognized the difference
between this very recently mixed material near the old entrance and the stratified
deposits in the shaft at the other end of the cavern. The term ‘‘ Clwydian,”’ if it is
at all advisable to give local names to drift, is a most unsuitable name for the wndis-
turbed glacial deposits on the higher levels, and should be confined to those at and
about St. Asaph, which are at a low level near the centre of the Vale of Clwyd, and

Dr. H. Hicks—The Ffynnon Beuno and Cae Gwyn Caves. 567

geologists as Prof. Boyd Dawkins, Mr. Morton, Mr. De Rance, Mr.
Strahan, Mr. Shone, and Dr. Stolterfoth, should, after careful
examination, have been perfectly satisfied that the Glacial deposits
overlying the flake and Mammalian remains were in an entirely un-
disturbed condition, and that they agreed with the views of the
members of the Committee (Mr. Luxmoore, Mr. P. P. Pennant, Mr.
E. Morgan, and myself), who were almost daily present at the
explorations, is, 1 think, ample proof that Prof. Hughes’ deductions
are entirely at variance with the facts.

Report of the Committee, consisting of Professor T. McK. Hughes, M.A., F.G.S.,
H. Hicks, M.D., F.R.S., H. Woodward, LL.D., F.R.S., E. B. Luxmoore, M.A.,
P. P. Pennant, M.A., and Edwin Morgan, appointed for the purpose of explor-
ing the Caves of North Wales.—Drawn up by Dr. H. Hicks, Secretary.

The explorations conducted by the Committee have been confined
to the caverns of Ffynnon Beuno and Cae Gwyn, in the Vale of
Clwyd. These caverns had been explored in preceding years by
Dr. H. Hicks and Mr. E. B. Luxmoore, some of the results being
given in a paper communicated to the Geological Section of the
Association in 1885, but more fully in a paper in the Quart. Journ.
Geol. Soc. February, 1886.

between the important rivers Elwy and Clwyd. This is in the main part remanié,
and as such ,the term ‘‘ Clwydian’’ might be applied to it. ‘lhe undisturbed glacial
deposits, stratified marine sands, and the overlying clay, containing large boulders of
local rocks and northern erratics, found at Cae Gwyn and at so many other points in
the neighbourhood at a high level far away from, and beyond the influence of any
important river, ought not, on any account, to be termed ‘‘ Clwydian.”’ The true
glacial deposits which overlaid the Mammalian remains and flint flake at the entrance
to Cae Gwyn Cave belong to a much earlier phase than the Clwydian drift about St.
Asaph and at other low levels in the valley, bordering the great rivers. The Cefn and
Plas Heaton Caves, mentioned by Prof. Hughes, are also at a very much lower level
than the Ffynnon Beuno Caves, and are so near to the rivers that I do not think
the evidence furnished by them can be quoted as of much value either way, though it
is well known that many have contended that the evidence in the Cefn Cave was
distinctly in favour of its having been occupied by the animals before the great sub-
mergence in the Glacial period. The evidence cited by Mr. Strahan, in his recent
excellent Memoir, as having been obtained in sinking shafts at the Talargoch mines,
conclusively proves that Mammalian remains occur there in the very lowest glacial
deposits. It is the great height at which the Ffynnon Beuno Caves occur, the im-
possibility of their having been disturbed by fresh water, the evidence of their having
been occupied as dens before the great submergence, of the stalagmite floor having
been broken up by marine action, of the bones having been cased in marine sand,
and of the caverns having afterwards been completely buried under marine sand and
an overlying undoubted boulder clay, containing many large ice-scratched boulders,
that make the evidence found in them and in their immediate neighbourhood of such
great value. The facts in my opinion are conclusive, and they cannot be altered by
any amount of special pleading. Prof. Hughes’ argument about the absence of
flint and other foreign rocks in what he calls the oldest deposit, is founded on nega-
tive evidence derived from a limited examination. Mr. Strahan, the latest authority
on the drift of this area, says (Geol. Survey Mem. 1885), ‘‘' The passage from the one
Boulder clay into the other is gradual, nor can it be said that one under or overlies
the other. They were no doubt formed contemporaneously, differing only in the
source of supply of material.’’ Sir C. Lyell in speaking of the Moel Tryfaen beds
says (‘‘ Student’s Elements,’’ 1871), ‘‘In the lowest beds of the drift were large
heavy boulders of far-transported rocks, glacially polished and scratched on more than
one side.”’ Prof. Hughes’ palxontological argument is found on examination to be
almost equally inapplicable, as a very large proportion of the animals occur in the
Norfolk forest-bed, which is acknowledged by all to be of pre-Glacial age. The fact
that some others have not been found in the caverns probably indicates that they did
not migrate into this area,

568 Dr. H. Hicks—The Ffynnon Beuno and Cae Gwyn Caves.

Among the remains discovered in these two caverns up to the
commencement of the work this year there were over eighty jaws
belonging to various animals, and more than 1300 loose teeth, in-
cluding about 400 Rhinoceros, 15 Mammoth, 180 Hyena, and 500
Horse teeth. Other bones and fragments of bones occurred also in
very great abundance. Several flint implements, including flakes,
scrapers, and lance-heads, were found in association with the bones.
The most important evidence, however, obtained in previous re-
searches was that bearing on the physical changes to which the area
must have been subjected since the caverns were occupied by the
animals. During the excavations it became clear that the bones had
been greatly disturbed by water action, that the stalagmite floor, in
parts more than a foot in thickness, and massive stalactites had also
been broken and thrown about in all positions, and that these had
been covered afterwards by clays and sand containing foreign peb-
bles. This seemed to prove that the caverns, now 400 feet above
Ordnance datum, must have been submerged subsequently to their
occupation by the animals and by Man. One of the principal objects,
therefore, which the Committee had in view this year was to critically
examine those portions of the caverns not previously explored, so as
to endeavour to arrive at the true cause of the peculiar conditions
observed. Work was commenced at the end of May, and carried on
during the whole of June and parts of July and August.

Car Gwyn Cave.

When the explorations were suspended last year, it was supposed
that we had just reached a chamber of considerable size, but after a
few days’ work this year it was found that what appeared to be
a chamber was a gradual widening of the cavern towards a covered
entrance. The position of this entrance greatly surprised us, as
hitherto we had believed that we were gradually getting further into
the limestone hill. The rise in the field at this point, however,
proved to be composed of a considerable thickness of glacial deposits
heaped up against a limestone cliff. As the materials covering the
bone-earth within and at the entrance were chiefly sands and gravels,
it was found necessary to suspend operations in that direction and to
ask the landlord (EH. Morgan, Esq.) for permission to open a shaft
directly over this entrance from the field above. As this necessi-
tated the removal of a considerable surface of land, and caused some
damage to the field, the Committee feel that their special thanks are
due to Mr. Morgan for his kindness in so readily acceding to their
application. This shaft, as at first opened, was about nine feet
across at the surface and over five feet at the bottom. It was sub-
sequently widened at the bottom in consequence of some falls and
the lower part, excepting at one point, had to be carefully faced with
timber. The upper part is now much widened and sloped. The
shaft was about twenty feet in depth, and the deposits as shown in
Fig. 1 were made out in it. These were carefully measured by Mr.
C. E. de Rance, F.G.S., Mr. Luxmoore, and the writer during the
prosecution of the work. Below the soil, for about eight feet, a

Dr. H. Hicks—The Ffynnon Beuno and Cae Gwyn Caves. 569

tolerably stiff boulder clay, containing many ice-scratched boulders
and narrow bands and pockets of sand, was found. Below this
there were about seven feet of gravel and sand, with here and there
bands of red clay, having also many ice-scratched boulders. The
next deposit met with was a laminated brown clay, and under this
was found the bone-earth, a brown, sandy clay with small pebbles
and with angular fragments of limestone, stalagmite, and stalactites.

—~goil, 1ft. 6in.

"~~ Brown clay with boulders,
2 ft. 9in.

__ Yellow loamy clay, 7 in.
~ Gritty boulder clay, 9in.

SPSS Stiff reddish clay with
boulders, 2ft. 3in.

Fie eR ee Sand, 2in.

Si a ae Purple clay. in.

7in.

——— ———— Gravelly sand with boul-
5 ders and bands of pur-
So ple clay, 2ft. 2in.
——=————— ——- Sandy gravel, 2 ft.

SS eee Kine banded) sand, Jit:
5 in.

‘—— — — —— — —- Red laminated clay and
bone-earth, with angu-
lar fragments of lime-
stone and a few boul-
ders. Contained also a
flint flake, from 2to5 ft.

A. Carboniferous Limestone. 4 Position of the flint flake.

Fig. 1. Section at New Entrance to Cae Gwyn Cave.
On June 28, in the presence of Mr. G. H. Morton, F.G.S., of Liver-
pool, and the writer, a small but well-worked flint flake was dug up
from the bone-earth on the south side of the entrance. Its position
was about eighteen inches below the lowest bed of sand. Several
teeth of Hyzna and Reindeer, as well as fragments of bone, were
also found at the same place, and at other points in the shaft teeth
of Rhinoceros and a fragment of a Mammoth’s tooth. One Rhinoceros
tooth was found at the extreme point examined, about six feet beyond
and directly in front of the entrance. It seems clear that the con-
tents of the cavern must have been washed out by marine action
during the great submergence in mid-Glacial time, and that they
were afterwards covered by marine sands and by an upper-boulder
clay, identical in character with that found at many points in the
Vale of Clwyd and in other places on the North Wales coast. Figs.
2 and 3 explain the order of the deposits as found within the cavern.

570 Dr. H. Hicks—The Ffynnon Beuno and Cae Guyn Caves.

Fig. 3 was taken at a distance of about sixteen feet from the entrance
at the shaft, and Fig. 2 just within that entrance. The order in that
portion of the cavern examined this year accorded in the main with
that found during the previous researches, but within the entrance
there was a greater thickness of sand, less of the laminated clay,
and more bone-earth than in the other parts of the cavern. The
bone-earth seems to diminish in thickness rather rapidly outwards
under the glacial deposits, but it was found as far out as the excava-
tions have been made. Here the bone-earth rests directly on the
limestone floor, with no local gravel between, as in the cavern.

Sand
Laminated clay | ss. sees
Bone earth . . his

(Sandy clay with pebbles, ete.)

Giravelingiin idee een ieee
(Mainly local materials.)

Sandygclayinle aii ile sek iiKe) ies

Maminatedtclaye waist aie t= ta me

iBoneearthignge es pieelne mer wae
(Sandy clay with pebbles, etc.)

Grivel. se ese
(Mainly local materials.)

Fig. 8, Section in Cae Gwyn Cave, about 16 feet from the New Entrance.

It would be interesting to know how far the cave earth extends
under the glacial deposits, but this could only be ascertained by
making a deep cutting through the terrace of glacial deposits, which
extends for a considerable distance in a westerly direction. The
glacial deposits here are undoubtedly in an entirely undisturbed con-
dition, and are full of smooth and well-scratched boulders, many of
them being of considerable size. Among the boulders found are
granites, gneiss, quartzites, flint, felsites, diorites, volcanic ash,

Dr. H. Hicks—The Ffynnon Beuno and Cae Gwyn Caves. 571

Silurian rocks, and limestone. Silurian rocks are most abundant.
It is clear that we have here rocks from northern sources, along with
those from the Welsh hills, and the manner in which the limestone
at the entrance to the cavern in the shaft is smoothed from the north
would indicate that to be the main direction of the flow. The marine
sands and gravels which rest immediately on the bone-earth are pro-
bably of the age of the Moel Tryfaen and other high-level sands, and
the overlying clay with large boulders and intercalated sands may
be considered of the age of the so-called upper-boulder clay of the
area. The latter must evidently have been deposited by coast-ice.
Whether the caverns were occupied in pre- or only in inter-glacial
times it is difficult to decide, but it is certain that they were fre-
quented by Pleistocene animals and by Man before the character-
istic glacial deposits of this area were accumulated. The local gravel
found in the caverns, underlying the bone-earth, must have been
washed in by streams at an earlier period, probably before the exca-
vation of the rocky floor of the valley to its present depth. From
the glacial period up to the present time excavation has taken place
only in the glacial deposits, which must have filled the valley up
to a level considerably above the entrances to the caverns. The
characteristic red boulder clay with erratic blocks from northern
sources is found in this area to a height of about 500 feet, and sands
and gravels in the mountains to the 8.H. to an elevation of about
1400 feet. The natural conclusion therefore is that the caverns
were occupied by an early Pleistocene fauna and by Man anterior to
the great submergence indicated by the high-level marine sands, and
therefore also before the deposition of the so-called great upper-
boulder clay of this area. As there is no evidence against such a
view, it may even be legitimately assumed that the ossiferous remains
and the flint implements are of an earlier date than any glacial
deposits found in this area.

Frynnon Beuno Cave.

This cavern, which yielded the greatest number of bones in the
previous researches, has now been cleared out in all those parts
where the deposits appeared to have been undisturbed by Man. A
considerable addition to the number of bones and teeth has been
made this year, but no new forms have to be added to those already
mentioned.

The animal remains found in the caves, as defined by Mr. W.
Davies, F.G.S., of the British Museum, comprise teeth and bones of
eleven genera and sixteen species, as shown by the annexed list :—

Lion (Felis leo, var. spelea). Boyine (Bos ? Bison 2).
Wild Cat (Ff. catus ferus). Great Irish Deer (Cervus giganteus).
Spotted Hyena (H. crocuta, var. Red Deer (Cervus elaphus).
spelea). Roebuck (C. capreolus).
Wolf (Canis lupus). Reindeer (C. tarandus).
Fox (C. vulpes). Horse (Zquus caballus).
Bear (Ursus, sp.). Woolly Rhinoceros (R. tichorhinus).
Badger (Meles taxus). Mammoth (Hephas primigenius).

Wild Boar ( Sus scrofa).

572 Reports and Proceedings—Geological Society of London.

REPORTS AND PROCHHDIN GS.

——_+-_>—_

I.—November 8, 1886.—Prof. J. W. Judd, F.R.S., President,
in the Chair.

The President noticed the presentation, on the part of Dr. Hector,
of a preliminary report of the late eruptions in New Zealand, and
stated that Dr. Hector hoped shortly to communicate a paper to the
Society on the subject; papers had also been sent or promised on the
same subject by other New Zealand geologists, and it was hoped that
before long the Society would be in possession of very full accounts of
these remarkable volcanic outbursts.

The following communications were read :—

1. “On the Skull and Dentition of a Triassic Saurian, Galesaurus
planiceps, Ow.” By Sir Richard Owen, K.C.B., F.R.S., F.G.S., ete.

The author referred to a fossil skull from the Triassic sandstone of
South Africa, which combined dental characters resembling those of
a carnivorous Mammal with the cranial structure of a Saurian. The
structure was described and figured in Owen’s ‘ Catalogue of the Fossil
Reptilia of South Africa,’ under the generic title of Galesaurus, as
belonging to a distinct suborder of Reprim1a, termed Theriodontva.

The characters of the skull and teeth of the original specimen of
Galesaurus have been brought to light by further development.

In both the type specimen and that lately received the reptilian
nature of the fossil is indicated by the single occipital condyle and
other features. The chief difference from a mature male of a placental
or marsupial carnivore is the evidence of a primordial ‘“ gullet-tract.”
Further details as to the structure of the skull were given, more
especially with reference to the orbits and nasals. The palatal region
repeats the same general characters as in previously described Therio-
donts. The angle of the jaw is not produced, as in the Crocodile,
beyond the articular element. In general shape and bony strength the
mandible of Galesaurus resembles that of a mammal.

The dentition is so much better preserved in the new specimen than
in the type Galesaur as to call for description;and illustration. In
four of the upper molars the entire crown is preserved; it shows less
length and greater breadth than appears in the previous restoration, is
moderately curved externally, and triangular; the base is flanked by a
short cusp before and behind, and the corresponding margins are finely
crenulate, as in the molars of Cynodracon. The incisors are eight in
number in both upper and lower jaws, four in each premaxillary,
opposed or partially interlocking with the same number in each mandi-
bular ramus; they have longish, slender, simple-pointed crowns. ‘The
canines, one on each side of both upper and lower jaws, have the same
laniariform shape and size of crown as in the original fossil. In the
right maxillary bone the long deeply planted root is exposed; the cor-
responding part of the lower canine is similarly exposed in the left
mandibular ramus. No trace of successional teeth, as in ordinary
Saurians, has been found.

Both Crocodiles and Alligators have two or more teeth of canine pro-
portions ; but the author shows how they differ from those of mammalian

Reports and Proceedings—Geological Society of London. 573

carnivores and Galesaurus. A similar character and disposition of
destructive canines is shown by the fossil jaws of the Oolitic great
extinct carnivorous Saurians, e.g. J/egalosaurus. In the Triassic
Labyrinthodonts the destructive and prehensile laniaries would by
position rank as incisors rather than canines. In existing Lizards the
dental series has more uniformity, and the cement-clad roots contract
bony union with the jaw-bone. In Galesaurus the teeth, besides being
distinguished, as in Mammals, by their differential characters, are
implanted freely in sockets, the cold-blooded character being chiefly
manifested in the greater number of teeth following the canines, and in
their want of distinction.

Lastly, the author remarked on the earlier reptilian character shown
by the Oolitic Mammal Amphitherium, and also by the existing Australian
Myrmecobius. He speculates on the degree of resemblance manifested
by the teeth of the old Triassic Reptile of South Africa with the excep-
tional characters of some of the low Australian forms of Mammals.

2. ‘The Cetacea of the Suffolk Crag.” By R. Lydekker, Esq.,
BoA, EEG: S., etc:

This paper commenced with notices of previous contributions to
the subject by Sir R. Owen, Prof. Ray Lankester, Prof. Huxley, and
Prof. Flower. In the preparation of a catalogue of the specimens
in the British Museum, the author had had occasion to examine the
collection of Cetacea from the Crag, not only in that Museum, but
also in the Museum of Practical Geology, that of the Royal College
of Surgeons, and in the Ipswich Museum, besides visiting the collec-
tions at Brussels. In consequence several additions to the fauna and
also numerous emendations of specific names were noticed in the paper
now laid before the Society. Prof. Ray Lankester’s views as to the
Diestian affinities of the English-Crag Cetacea were confirmed by this
comparison.

Detailed notes on the specimens examined and the species identified
were given. The following list of the species believed to be repre-
sented in the various collections mentioned was given at the conclusion
of the paper :—

BaL=NIDm.
Balena affinis, Owen. Balenoptera borealina, van Beneden.
> primigenia, van Beneden. » emarginata (Owen).
» insignis (van Beneden). Cetotherium Brialmonti (van
», balenopsis (van Beneden). Beneden).

Megaptera afinis, van Beneden. 50 dubiwm (van Beneden).
99 similis (van Beneden). 9p Hupschi (van Beneden).
ay minutus (van Beneden), brevifrons (van Beneden).

Balenoptera definita (Owen). Herpetocetus scaldiensis (van

99 Goropi, van Beneden. Beneden).
PHYSETERID &.

Eucetus amblyodon, du Bus. Choneziphius planus (Owen).
Homocetus Villersi, du Bus. a Packardi, Lankester.
Balenodon physaloides, Owen. Mesoplodon longirostris (Cuvier).
Physodon grandis (du Bus). 5 tenutrostris (Owen).

» fusiformis 2 (du Bus). 3p gibbus (Owen).
Hoplocetus crassidens, Gervais. 55 angustus (Owen).

ars borgehoutensis, Gervais. Jn angulatus (Owen).

%p crassidens ? Gervais. compressus (Huxley).
Hyperoodon, sp. Flowers 7, Canham MS,

Choneziphius planirostris (Cuyier).

O74 Correspondence—Dr. W. T. Blanford.

SQUALODONTID &.
Squalodon antverpiensis, van Beneden.
DELPHINIDE.
Orca citoniensis, Capellini. Delphinoid genus, non det.

Globicephalus uncidens (Lankester).

3. “On a Jaw of Hyotherium from the Pliocene of India.” By R.
Lydekker, Esq., B.A., F.G.S., etc.

Colonel Watson, the Political Resident in Kattiawar, had recently
sent to the author a fragment of a left maxilla with the three true
molars from Perim Island, in the Gulf of Cambay. The specimen
belonged to Hyotherium, and apparently to an undescribed species,
the differences between which and the several forms previously known
from various European and Asiatic beds, were pointed out. The
author also called attention to the peculiar association of types found
in the beds of Perim Island, and to the affinities of the genus
Hyotherium with the recent Sus and Dicotyles on the one hand, and
with the Upper Eocene Cheropotamus on the other,

CO S42 @sN DE aC zeae

eee tae,
THE FACETTED BLOCKS FROM THE PUNJAB SALT RANGE.

Str,—Had I been aware that the abstract of my remarks ‘‘On a
Smoothed and Striated Boulder from a Pretertiary Deposit in the
Punjab Salt Range”? would appear in the Gxrozoercan Magazine,
together with Mr. Wynne’s notes on another facetted fragment from
the same bed, I would have asked permission to add a few observations.

The great difficulty in accounting for the origin of these facetted
blocks is that whilst the smoothed surfaces are in every respect similar
to those on stones worn by glacial action, no fragments from moraines,
from boulder-clay, or from other glacial deposits are known to exhibit
the peculiar facetting characteristic of the present specimens. I have
heard of something similar, but have not seen an example. Other
geologists who have a wide experience of smoothed and striated
boulders are equally puzzled.

At the British Association meeting two suggestions were offered as
to the cause of the markings—the first was soil cap action; this,
however, could. not have produced the facets, nor, unless it acted in
two or more directions at the same time, could it have caused the
striation. The other suggestion was wind and sand action, by which
similarly facetted blocks are said to have been produced in Australia.
My objections to this view are that wind and sand action never, so far
as I have seen, produce plane surfaces, that the striation (or rather
grooving) on wind-worn surfaces is of a different character, and that
the wind-worn fragments sent from New Zealand by Mr. Enys, and
figured in the Quart. Journ. Geol. Soc. for 1878 (xxxiv. p. 86), as well
as some described in the American Naturalist (occurring, I think, in
Maine), have no resemblance to the Punjab specimens. Further and very
cogent arguments are supplied by Mr. Oldham in a paper which I trust
will shortly be published in this Macaztnn.

Before concluding, may I point out that felspar-porphyry on p. 494
is a misprint for felsite-porphyry.

Nov. 8th, 1886. W. T. Buanrorp,

Correspondence—Prof. T. G. Bonney. D709

THE FOLIATION OF THE LIZARD GABBRO.

Srr,—Students of petrology will, I am sure, feel indebted to my
friend Mr. Teall, no less for his valuable paper on the Lizard Gabbro
than for the admirable Plate with which it is illustrated. He has
stated very clearly the reasons in favour of ascribing the peculiar
rock-structure, there described and depicted, directly or indirectly to
mechanical influences. In this it is quite possible he may be right.
But, inasmuch as there seems to me some danger at the present
time of overestimating the part played by mechanical agencies in
producing the crystalline schists—a part which hitherto undoubtedly
has been much underestimated—a danger in short of supposing that
a truth is “the truth, the whole truth, and nothing but the truth,”
I venture to put a few words on record, not so much by way of
protest or criticism, as for the purpose of showing that in Mr. Teall’s
proposed solution of this puzzle there are difficulties on which he
does not dwell, so that it ought at present to be regarded as an
hypothesis on its probation, and should not be quoted (as I feel sure
it would otherwise be) as an undoubted fact. My remarks, be it
understood, must be regarded as directed, not against the general
principle, of which this Lizard gabbro would be a particular case,
but against the application of the principle to this case.

The difficulties which I feel may be thus stated. If the foliation
of the Lizard gabbro is the result of earth-movements acting on the
rock after it became solid, these movements, having resulted in
effects of an exceptional character, should have been of exceptional
importance—that is to say, the whole district should bear the impress
of the same earth-movement that has foliated the gabbro. Mr. Teall
states indeed: “that the Lizard district has been profoundly
affected by earth movements is apparent on every hand.” Speaking
for myself, I should prefer to read ‘considerably’ for ‘ profoundly,’
so far as regards the earth-movements to which we could ascribe the
foliation of the gabbro. I am well acquainted with three large
separate areas of country which have been ‘ profoundly affected by
earth-movements’ since their rocks became solid, and I do not find
a parallel to them in the Lizard, except perhaps at the extreme south
and near the great boundary fault on the north. There are un-
doubtedly numerous dislocations (as I have pointed out in one of my
papers on the district) ; there are endless wrenches, slips and nips;
but there are few signs of a great compression such as may often be
traced through whole regions of crystalline rock almost as surely
(when the key to it is once found) as a slaty cleavage in one of sedi-
mentary rock. This foliation of the Lizzard Gabbro, as Mr. Teall
truly says, comes in and disappears, even in the thin veins, in appa-
rently the most arbitrary manner. This of course is perplexing in
any theory of its origin. I only quote it to show that our difficulties
are so far not diminished by the new one. Again, the foliation often
occurs where the neighbouring rocks show little or no signs of
material disturbance. I do not say that the contrary is not some-
times the case, but near the Balk (or Pen Voose), and to the north

076 Correspondence—Prof. T. G. Bonney.

of Karakclews, and at Coverack this is the case. Serpentine is a
decidedly brittle rock. Any one who knows the Alps is familiar with
its pressure-modifications. Yet the serpentine at all these three
places, as a rule, is singularly perfect in its structure, free from
all indications of serious mechanical disturbance. There are, I am
well aware, serpentines at the Lizard which might be quoted as
evidencing ‘pressure-structure,’ but, as it happens, these do not
occur at any one of the three localities where the foliated gabbros
exist. At all three the serpentines are perfectly normal in their
characters. But it might be asserted that, at the epoch of the pressure,
the serpentine existed as a peridotite, and this very possibly would
be true; still I think I know what is the effect of pressure on a
peridotite, and could conjecture what the results would be when
it was converted into a serpentine, and of these also I find no signs
at the above-named places.

But it may be argued that this foliation in the gabbro is the
result not so much of a general compression of the district, as of
local strains, thrusting, and shearing in the gabbro-mass itself, due
to local disturbances; that it is a structure resulting from faulting
rather than from jfolding—from dislocation-strains rather than com-
pression-thrusts. So far as the minor cases at the Balk and Coverack
are concerned, this explanation would seem feasible, but it is difficult
to apply it to such an enormous mass as that of Karakclews,
where the differentiation and parallel ordering of the minerals have an
extraordinary development. Moreover, as Mr. Teall justly says,
this mass sends out veins into the neighbouring serpentine, and that
rock to the north has been repeatedly pierced by small gabbro veins,
so that we cannot suppose the main mass to have been thrust far
away from its original position.

There are then, as it seems to me, some serious difficulties in
applying the theory of pressure-foliation to the Lizard gabbros, if
it be assumed that the structure was produced in a solid rock. Mr.
Teall’s solution of the difficulty may be the right one, but it is always
well to look at all sides of a question. A new answer to one of
Nature’s greater riddles is often rather a first approximation to the
truth, than the actual truth, and stands in need of subsequent
modification. As at present advised, I am disposed to think this the
case in regard to the Lizard gabbro, though further study may
remove my difficulties. Still I think we shall do well to proceed
cautiously in regard to this new hypothesis of pressure-metamorphism.
It has come to many, like myself, almost as a revelation, pouring
a flood of light upon a number of dark enigmas; but for all that we
must not allow it to dazzle our eyes. In this, as in so many other
things, reason should go hand in hand with faith, T. G. Bonney.

Necrotocy.—We have to record with deep regret the recent losses by death of
Dr. H. Abich, F.M.G.S. (Vienna); Mr. George Busk, F.R.S., F.G.S.; Rev. W.
Downes, B.A., F.G.S.; the Earl of Enniskillen, D.C.L., F.R.S., F.G.S.; Mr.
Caleb Evans, F.G.S.; and Prof. F. Guthrie, F.R.S., F.G.S.

Erratum.—Gxrox. Mac. November Number, p. 492, line 10, delete ‘ difficult.”

INDEX.

ADA

DAMS, F. D., The Anorthosite
Rocks of Canada, 506.
Adamson, §. A., Fossil Tree near Brad-
ford, 406.
Address, Reading Literary and Scientific
Society, 37.
Afghanistan, Geological Formations in,

Age of the Tuffeau de Ciply, 10.

“« Alaska Glacier,’’ 140.

Alteration of coarsely spherulitic Rocks,
187.

American Paleontology, Contributions
to, 374.

Ammonites, Lobe-line of Lias, 442.

Ancient Glaciers of Isar and Linth, 259.

Andree, Dr. A., Geology of Alsace and
Lorraine, 78.

Angiosperms, Mesozoic, 193, 342.

Animals, Tracks of, 409.

Annual Meeting of the Geological
Society, 180.

Anthracite Coal-fields of the Rocky
Mountains, 379.

Application of the Term Neocomian, 311.

Arabia Petreea, Notes on Rocks from,267.

Arenig Series of North Wales, 509.

Archean Rocks from Shropshire, 376.

Arctic and Atlantic Basins, Relations of
‘the Geology of the, 504.

Assouan, Rocks of, 103.

Atlas of China, 34.

Atmospheric Dust, 122.

Australia, Ichthyodorulite from, 1.

Axosmilia elongata, Duncan, 340.

ACKHOUSEH, J., on a Lower Jaw
of Macherodus, 234.

Bagshot Beds of the London Basin,
300.

Base of a Fossil Tree at Clayton, 406.

Becher, H. M., on some Cupriferous
Shales, 379.

Beesley, T., on the Lias of Fenny Comp-
ton, 168.

Belemnitella plena, Zone of, 136.

Belfast Natural History Society, 134.

Bell, A., Succession of the Later Ter-
tiaries, 67.

Bell and Kendall, Pliocene beds of St.
Erth, 186.

Beyrichia Bradyana, J. & K., 488.

—§§\ cratigera, G. 8. B., 489.

Beyrichiella cristata, J. & K., 488.

DECADE III.—VOL. III.—NO. XII.

CAM

Beyrichiopsis cornuta, J. & K., 436.

—— fortis, J. & K., 435.

——— jimbriata, J. & K., 434.
simplex, J. & K., 437.
subdentata, J. & K., 487.

Birmingham. Deep-Boring near, 453.

Black Rock of Kiltearn, 29.

Black, W. J., Alaska Glacier, 140.

Blake, J. H., on the Coal-fields of Great
Britain, 37.

Blanford, W. T., Glacial Conditions in
the Paleozoic Era, 494; Facetted
blocks from the Punjab Salt Range,
574; Striated Boulder from the Salt
Range, 494.

Bois de Fontaine Meteorite, 357.

Bonney, T. G., Foliation of the Lizard
Gabbro, 575; Microscopic Structure
of Rocks of Assouan, 103 ; The Pale-
ontographical Society, 237; on Rock
Specimens from Pembrokeshire, 331.

Bone Caves in North Wales, 39.

Borings in Kent, 41.

Brachiopoda, Notes on Jurassic, 217.

Brighton Waterworks, 32, 159.

British Association, 477.

British Museum Publications, 175, 177,
419, 425, 428.

British Stromatoporoids, Monograph of,
123.

Brodie, P. B., Remarkable Section in
Derbyshire, 482; Rheetic Sections,
185; Fossil Fish from the Keuper,
507; Range of Rhetic Fossils, 508.

Brookwood Deep Well Section, 456.

Brown, J. A., Thames Valley Surface-
deposits, 135.

Brown, H. Y. L. and Woodward, H. P.,
Geological Report on Barossa Gold-
field, etc., 278.

Buckman, 8. S., on Jurassic Brachio-
poda, 217; on the Lobe-line of Am-
monites, 442.

Bulletins of the United States Geological
Survey, 172.

Bythocypris sublunata, J. & K., 250.

AITHNESS, Rocks of, 31.

Callaway, C., on Archean Rocks of
Shropshire, 376; on the Crystalline
Schists of Ireland, 507.

Cambrian Rocks at Nuneaton, 319, 540.
Cameron, A. G., on Water-bearing
Nodules, 319.

37

578

CAN

Canada, Anorthosite Rocks of, 506.

Canadian Examples of Fossil Algz, 508.

Canadian Paleontology, 129.

Cape-Breton Island, Geology of, 878.

Carboniferous Limestone of England and
Belgium, 463.

Paleoniscide, 440.

Carinthia, Eocene Strata in, 120.

Carpenter and Etheridge, Catalogue of
Blastoidea, 419.

Carter, J., Decapod Crustaceans of the
Oxford Clay, 378.

Catalogue of the Blastoidea, 419.

——— Fossil Mammalia, 175.

Paleozoic Plants, 177.

—— Silurian Crustacea of Got-
land, 33.

Caves of Ffynon Beuno and Cae Gwyn,
489, 566.

Cetacea of the Norfolk “ Forest-bed,”’
234.

Cetacea of the Suffolk Crag, 573.

Chester Society of Natural Science, 89.

Clayton, Fossil Tree at, 406.

Coal-measures of Warwickshire, 540.

Cole, G. A. J., Igneous Rocks of Stanner,
219; on “ Spherulitic Rocks,” 187.

Collins, J. H., on Cornish Serpentinous
Rocks, 359.

Colorado, Fossil Ostracoda from, 146.

‘*‘Coming-of-Age”’ of the GroLocicaL
MaGazine, 46.

‘¢ Cone-in-Cone,’”’ 139.

Cope, E. D., On Edestus and Pelecopte-
rus, 141; Note on Hrisichthe, 239;
New Perissodactyle Ungulate, 49;
Vertebrata of the Tertiary Formations
of the West, 410, 465, 512.

Cornet, M. L. F., Phosphatic Beds near
Mons, 281.

Cretaceous Madreporaria, 44, 52.

Crinoids from the Upper Devonian,
Germany, 170.

Cromer Forest-bed, Flora of, 410.

ee a Shales in Houpeh, China,
379.

Dy J. D., Lower Silurian Fossils,
377.

Davies, W., Note on Edestus, etc., 141.

Davis, J. W., Fish-remains from Moun-
tain Limestone, Derbyshire, 146;
Tertiary Fish-remains, 93.

Davidson, C., Rock-Surface under a
Talus, 65; on Undisturbed Spots in
Earthquake Areas, 157.

Davidson, G. M., on the Rocky Moun-
tains, 505.

Dawson, Sir W., Fossil Algw, 503;
on the Geology of the Arctic and
Atlantic Basins, 504,

Index.

EVO

Death of Prof. J. Morris, 93.

—— Mr. W. W. Leighton, 144.

Deelly, R. M., Trent Basin, 284.

Deep-Boring in New Red Marls, 453.

—— in Kent, 510.

Deep Well Section at Brookwood, 353.

Deeside, Karly Human Habitations, 33.

Decapod Crustaceans of the Oxford Clay,
378.

Dentition of Galesaurus planiceps, Ow.,
572.

Depéret, C., on the Pliocene Vertebrata
of France, 328,

De Rance, C. H., on Erosion of Sea-
Coasts, 26.

Derbyshire, Fish-remains from, 146.

Desmidopora alveolaris, Nichs., 289.

Development of the North American
Continent, 97.

Dimorpharea expansa, Tomes, 451.

Diphyphylium, on the Genus, 232.

Does Teredo inhabit Fresh Water P 336.

Dollo, M., on the Evolution of the Dino-
sauria, 275; New Chelonians from
Belgium, 521.

Dover, Beds between Upper and Lower
Chalk, 137.

Downes, W., Ou a Section near Honi-
ton, 308.

Duncan, P. M., on Cretaceous Madre-
poraria, 52; on a New Species of
Axosmilia, 340.

Durham, J., Volcanic Rocks of N. EK.
Fife, 333.

ARTHQUAKES and other Earth-
Movements, 371.

Earthquake Phenomena, 157.
Edestus and Pelecopterus, etc., 141.
Davisii, H. Woodw., 1.
Elonichthys Aitheni, Traquair, 440.
—— macrodon, Traquair, 441.
——— microlepidotus, Traq., 441.
Emmons’ Original Taconic Series, 277.
Emydine Chelonian from India, 330.
Kocene Chelonians from Belgium, 521.
Eocene, Teredo-bored Wood in the, 161.
Eophyton 2 explanatum, Note on, 337.
Erinaceus eningensis, Lydekker, 41.
Erisichthe, Note on, 237.
EKruption of Mount Tarawera, 384,
Hssays on Speculative Geology, 293, 300.
Etheridge and Carpenter, Blastoidea, 419
—— R. jun., Notochelys costata,

239.

—_ Volcanic Eruption in
New Zealand, 398.

Evolution of the Herbivorous Dinosauria,
275.

Index.

FAU

AUNA Antiqua Sivalensis, 43.
Feilden, H. W., on Hippopotamus
amphibius, 235.
Ffynnon Beuno Caves, 489, 566.
Fisher, O., Geologists visiting Wey-
mouth, 336.
Fish-remains from New Zealand, 93.
Foliation of Lizard Gabbro, 575.
Folkestone, Landslip near, 240.
Ford and Dwight, Fossils from Meta-
morphic Limestone, 277.
Forest of Dean, Limestones of the, 529.
Form of Rock-Surface under a Talus, 65.
Fossil Algz, from Canada, 5038.
Elephants of Germany and Italy,

135.
Fish-remains from the Mountain

Limestone, 148.
Fish in the Old Red Sandstone,

507.

Flowering

Plants, 495.

Mammalia of Maragha, 134.

—— from Baltavar, 227.

Radiolaria from Jura, 79.

Fossils of the Rhetic Formations of
Warwickshire, 508.

Fringed Ostracoda from the Carbonifer-
ous, 433.

Fritsch, Dr. Anton, Fauna of the Gas-
coal, 44.

or Phanerogamous

Gone Dolerites and Basalts,
wile

——— Metamorphosis of Lizard, 481.
Galicia, Rock-Salt Formations of, 121.
Gardner, J. 8., Distribution of Teredo-
bored Wood, 161; Does Teredo in-
habit Freshwater P 336; on Mesozoic
Angiosperms, 193; Fossil Flowering
Phanerogamous Plants, 495.
Gas-coal of Bohemia, 44.
“Gault ’’ so-called of West Dereham,
Norfolk, 55.
Geology of Bridlington Bay, 86.
—— Eskdale, Rosedale, etc., 87.
Holderness, 85.
South Australia, 278.
South-West Lincolnshire, 86.
— the Coasts adjoining Rhyl,
etc., 87.
——— the Kimberley District, 166.
the Pays-Bas, 171.
— the Vale of Clwyd, 89.
Geological Age of Beds containing Plants
in India, 232.
——— —— North Atlantic, 189.
History of Cornish Serpen-
tines, 359.
Map of Alsace-Lorraine, 78.

579

HOR

Geological Map of Lower Egypt, 30.
—— Society, 39, 91,134, 180, 230,
330, 375, 572.
Survey of India, 170, 173, 462.
of United States, 464.
Record, 88.
Relations of Rocks of Assouan,

101.

Geologists visiting Weymouth, 336.

Gilpin, E., Geology of Cape-Breton
Island, 378.

Glacial Periods in Low Latitudes, 300.

Phenomena of the Isle of Got-
land, 367.

——w— Shell-bed in British Columbia,
233

Glaciation of South Lancashire, 331.

Gloucestershire, Inferior Oolite, 186.

Granitoid and Felsitic Rocks, 330.

Graptolite, Family Dichograptide, 13.

Gregory, J. R., on Two French Meteo-
rites, 357.

Gresley, W. S., on a Modern Ferru-
ginous Conglomerate, 11.

Griesbach, C. L., Geological Formation
of Afghanistan, 121.

Griffith, A. B., Eocene Formations in
Servia, 380.

Guide to Department of Geology, etc.,
428.

Gunn, J., on the Rocks of Caithness, 31.

ARDMAN, KE. T., on the Geology
of the Kimberley District, 166.

Harrison, W. J., Deep-Boring in Keuper
Marls, 453.

Hauer, F. von, Annals of Natural History
Museum of Vienna, 169.

Heim, A., Glaciers of Isar and Linth,
259.

Herrmann, Dr. O., on Dichograptide, 13.

Hicks, H., Bone-Caves in N. Wales, 39;
on the Rocks of Pembrokeshire, 330 ;
on the Ffynnon Beuno and Cae Gwyn
Caves, 566.

Highbury Microscopical Society, 138.

Hill, W., Beds between the Upper and
Lower Chalk of Dover, 137.

Hill, W., and Jukes-Browne, A., Zone
of Belemnitella plena, 136.

Hinde, G. J., Note on EHophyton ? ex-
planatum, 387.

Hippopotamus amphibius, Distribution of,
235.

Hippopotami, Recent and Fossil, 114.

Holl, Harvey B., Obituary of, 526.

Homotaxis and Contemporaneity, 293.

Honiton, Tunnel Section near, 308.

Hornblende-bearing Rocks from Inch-
nadampf, 346.

580

HUD

Hudleston, W. H., Section through
Walton Common, 93.

Hughes, T. McKenny, Geology of the
Vale of Clwyd, 89; on Perched Blocks,
375; on the Ffynnon Beuno Caves,
489; Silurian Rocks of North Wales,
509; Sectionsinthe Arenig Series, 509 ;
Pleistocene Deposits in the Vale of
Clwyd, 509.

Hulke, J. W., On Maxilla of Iguanodon,
282.

Hull, Prof. E., Geology of Western
Palestine, 227 ; Outline Map of Egypt,
etc., 80; Lower Old Red Conglomerate
in Donegal, 31; Reply to Prof. Le
Conte, 189; Survey of Western Pales-
tine, 286.

Hyalostelia (Pyritonelia) fasciculus, Note
on, 337.
Hyotherium, Jaw of, from the Pliocene

of India, 574.

Hyoid and Mandibular Arches in a

Cretaceous Shark, 285.

GUANODON, Maxilla of, 282.
Igneous Rocks of Stanner, 219.
Igneous Rocks, etc., of the Warwickshire
Coal-field, 557.

Inchnadampf, Hornblende-bearing Rocks
from, 346.

Indian Tertiary Vertebrata, 173.

Treland, Crystalline Schists of, 507.

Trish Metamorphic Rocks, 7.

Irving, A., Bagshot Beds of London Clay,
402; Brookwood Deep-Well Section,
353.

OHNSTON-LAVIS, H. J., on the
Earthquakes of Ischia, 369.

Jones, T. R., Fossil Ostracoda from
Colorado, 146; Paleeozoic Phyllopoda,
456.

Jones, T. R., and Kirkby, J. W., Car-
boniferous Ostracoda, 248, 282, 433.
and Sherborn, C. D., on

Jurassic Microzoa, 271.

Judd, J. W., A Problem for Cheshire
Geologists, 89; on Gabbros, Dolerites,
and Basalts, 91; on Marekanite and
its Allies, 241; on Nile Delta-Borings,
226; on the Term Neocomian, 382.

Jukes-Browne, A. J., on the Term Neo-
comian, 311, 431.

Jurassic Brachiopoda, 217.

IDSTON, R., Catalogue of Palzeozoic

Plants, 177; on a New Species of
Psilotites, 1386.

Kinahan, G. H., on Metamorphic Rocks,

Kirhbya variabilis, J. & K., 249.

Index.

MIC

Kirkby, J. W., and T. R. Jones, Carbon-
iferous Ostracoda, 248, 282, 433.

Keenen, A. von, on Upper Devonian
Crinoids, 170.

Koninck, L. G. de, on Carboniferous
Limestone, 463.

APWORTH, C., Cambrian Rocks at
Nuneaton, 319.

Layis, H. J. Johnston, Volcanic Eruption
in New Zealand, 528.

Le Conte, J., Development of North
American Continent, 387; Permanence
of Continents, 97, 288.

Lethea erratica, 35.

Lias of Fenny Compton, 168.

Liassic Madreporaria of Gloucestershire,
107.

Limestones of the Forest of Dean, 529.

Lindstrom’s Silurian Crustacea of Got-
land, 33.

Linnean Society, 36.

Lobe-line of certain Species of Am-
monites, 442.

London Clay and Bagshot Beds, 402.

Lorié, J., Geology of the Pays-Bas, 171.

Lower Lias of Leicestershire, 59.

Lydekker, R., Catalogue of Fossil Mam-
malia, 175, 425; Crocodilian genus
Tomistoma, 41; Fauna Antiqua Siva-
lensis, 48 ; Fossil Mammalia of Mara-
gha, 184; New Emydine Chelonian,
380; New Species of Hrinaceus, 41 ;
Siwalik Crocodilia, etc., 173; the
Cetacea of the Suffolk Crag, 573;
Jaw of Hyotheriwm from the Pliocene
of India, 574.

ACH ARODUS from the Forest-
bed, Kessingland, 234.

Mackintosh, D., Interglacial Land Sur-
faces at Crewe, 90.

Madreporaria from the Inferior Oolite,
387, 443.

—————— Upper Lias, Gloucester-
shire, 107.

Marcou, J. B., North American In-
vertebrate Paleontology, 368.

Marekanite, and its Allies, 241.

Medlicott, H. B., Boulder-beds of the
Salt Range, 462.

Memorial to Dr. T. Davidson, 528.

Merritt, W. H., on Anthracitic Coal-
fields, 379.

Mesozoic Angiosperms, 193, 342.

Metamorphic Rocks, 7.

Metamorphosis of the Lizard Gabbros,
481.

Meteorite from Bois de Fontaine, 357.

Michie, J. G., Harly Human Habitation,
33.

Inted.

MID

Middlesex, Well-section in, 379.

Microzoa found in Jurassic Rocks, 271.

Milne, J., on Earthquakes, 371.

Minute Structure of Stromatopora, 368.

Modern Ferruginous Conglomerate, 11.

Monckton, H. W., and Herries, R. S.,
on the Bagshot Beds, 335.

Monograph of the Karthquakes of Ischia,
369.

Mons, Phosphatic Beds near, 281.

Monument to Horace-Bénédict de Saus-
sure, 142.

—__—_—- Oswald Heer, 148.

Mosasaurus gracilis, Remains of, 134.

Morris, Professor J., 938, 95.

ATHORST, A. G., On Tracks of
Animals, 409.
Neocomian, Application of the Term, 311.
on the Term, 382, 4381.

Newton, E. T., Contribution to History
of Cetacea, 234.

New Type of Perissodactyle Ungulate,
49, 140.

New Zealand, Recent Volcanic Eruption,
398, 524.

Nicholson, H. A., British Stromato-
poroids, 123; on a New Genus of
Silurian Corals, 289.

Niezwiecki, J., Rock-salt Formation of
Wieliczka, 121.

Notochelys costata, Owen, 239.

Notidanus, Paleontology of Genus, 205,
253.

Daviesii, A. S. Woodw., 212.
lanceolatus, A. S. Woodw.,214.
dentatus, A. 8. Woodw., 214.
amalthei, Oppel, 525.

North American Continent, Development
of, 287.

Nuneaton, Sequence of Cambrian Rocks
at, 319,

Volcanic Rocks at, 322, 557.

BITUARY of C. W. Peach, 190.
——_—_—_ J. B. Jeafireson, 188.
Harvey B. Holl, 526.

—_—_____ J, Morris, 95.

A. von Lasaulx, 144.

Obollela granulata, Sharman, 566.

Observations on some Imperfectly known
Madreporaria, 52.

Occurrence of Lower Old Red Conglome-
rate in Donegal, 31.

Oldham, R. D., on Homotaxis and Con-
poraneity, 293; on the Olive Group
Salt Range, 462; Probable Changes
of Latitudes, 300.

Olenus Nuneatonensis, Sharman, 565.

Old Red Sandstone under London, 43.

—_—

581
PUN

Organisms in Limestones of the Forest
of Dean, 529.
Ormerod, G. W., Old Sea-beaches at
Teignmouth, 91.
Ostracoda from the Carboniferous, 248,
282, 433.
from Colorado, 146.
from Northamptonshire, 248.
Owen, Sir R., on a New Perissodactyle
Ungulate, 140 ; on the Skull and Den-
tition of Galesaurus planiceps, 572.
Oxfordshire, Madreporariafrom the Oolite
of, 887, 443.

| Ol rahe Neer Society,
Publications of, 130, 237.
Palzontologia Indica, 463.
Paleoniscide from the English Coal-
measures, 440.
Paleozoic Phyllopoda, 456.
———— Starfishes, Contributions to the
Knowledge of, 119.
Papers Read at the British Association,
Section C., 477.
Bearing on Geology in other
Sections, 480.
Pea Grit, a new Species of Axosmilia
from the, 340.
—— —— of Leckhampton Hill, 525.
Peach, C. W., Obituary of, 190.
Pebble from the Olive Group Conglome-
rate, 492.
Penck, K. A., Eocene Strata in Carinthia,
120.
Permanence of Continents and Ocean
Basins, 97, 375.
Petho, J., Fossil Mammalian Remains,
227.
Phanerogamous Plants, 495.
Phenacodus, Notes on, 238.
Physical Geology and Geography of
Arabia, etc., 227.
Placophyllia gracilis, Tomes, 319.
Platastrea endothecata, Tomes, 447.
Pleistocene Deposits in the Vale of Clwyd,
509.
Pleistocene Succession in the Trent Basin,
284.
Pliocene Vertebrata of France, 328.
Pohlig, H., On the Pliocene of Maragha,
135.

Prestwich, J., Geological Text-book, 81.

Price, F. G. H., Landslip near Folke-
stone, 240.

Psephodus simplex, Davis, 151.

Psilotites from the Lanarkshire Ooal-
field, 136.

Pterograptus dilaceratus, Herrmann, 17.

Punjab Salt Range, Discoveries in the,
286; Facetted blocks, 574, !

582

PUN

Punjab Salt Range, Geology of, 131.
Striated Boulder

from the, 494.

UILTER, H. E., On the Lower Lias
of Leicestershire, 59.

ATE of Erosion of Sea-coasts, 26.
Recent Brachiopoda, by the late Dr.
Davidson, 36.

Recent and Fossil Hippopotami, 114.

Red Crag, Vertebrata of the, 283.

Reid, C., Flora of the Cromer Forest
Bed, 410; on Glacial Shell Beds, 233;
Geology of Holderness, 85; on the so-
called Gault of Norfolk, 55.

Relations. of the Lincolnshire Carstone,
377.

Renard, Prof. A., on Rock Specimens,
33.

Report on Paleeozoic Phyllopoda, 456.

on Specimens from Nile Delta-
borings, 226.

Richthofen’s Atlas of China, 34.

Roemer’s Erratic Blocks of N. Germany,
35.

Rock Specimens from Fernando Noronha
Group, 33.

Rocky Mountains, On the, 505.

Royal Geological Society of Ireland, 131.

Rudler, F. W., Rocks of Arabia Petrea,
267.

Ruest, Dr., Jurassic Radiolaria, 79.

Rutley, F., on Eruptive Rocks, 334; on
Igneous Rocks, 557.

Rutot, A., on the Tuffeau de Ciply, 10.

Riynchonella liostraca, 8. Buckman, 217.

CHLOSSER, Max, on the Ungulata,
326.
Schuster, M., Atmospheric Dust, 122.
Seeley, H. G., Review of Cope’s Work,
410, 465, 512.
Selachian Genus Notidanus, 205, 253.
Serpentinous Rocks of Cornwall, 359.
Servia, Eocene Formation of, 380.
Sharman G., on the so-called “ Gault”’
of Norfolk, 55; on new Species of
Olenus and Obollela, 565.
Sherborn, C. D., and T. R. Jones, on
Jurassic Microzoa, 271.
Shone, W., Silting-up of the River Dee,
0

90.

Short Notices of Scientific Papers, 367,
408.

Silurian Corals, 289.

Silurian Rocks of North Wales, 509.

Skertchly, S. B., On Slickensided Sur-
faces of Chalk, 335.

Stanner, Igneous Rocks of, 219.

Stephanocenia dendroidea, Tomes, 392.

Index.

UND

Stephanocenia expansa, Tomes, 393.
Striated Boulder from the Salt Range,

494.

Striated Pebble from the Salt Range,
492.

St. Minver, Cornwall, Eruptive Rocks
of, 334.

Stolterforth, Dr., Surface-Dredging in
the Dee, 91.

Strahan, A., Carstone of Lincolnshire,
877; Denudation of North Wales, 89;
Glaciation of South Lancashire, 331 ;
Rocks surrounding the Warwickshire
Coal-fields, 540.

St. Erth, Pliocene Beds of, 186.

Sturtz, B., Paleozoic Starfishes, 119.

Succession of the Later Tertiaries in
Great Britain, 67.

Survey of Western Palestine, 286.

Swanston, W., on Mosasaurus gracilis,
134.

Swindon, Account of a Well-sinking at,
188.

ABLE of Liassic Fossils, 61.
Table of Species of Paleozoic
Phyllopoda, 461.

Teall, J. J. H., Notes on Hornblende-
bearing Rocks, 346; Metamorphosis
of the Lizard Gabbros, 481.

Terebratula ewides, S. Buckman, 218.

Testimonial to Dr. H. Woodward, 45.

Tertiaries, Succession of, 67.

Text-book of Geology by J. Prestwich,
81.

Thames Valley,
Kaling, 135.

Thamnastrea expansa, Tomes, 450.

heteromorpha, Tomes, 450.

Thamnosmilia annulata, Tomes, 396.

Thomson, J.,on the Genus Diphyphyllum,
232.

Tomes, R. F., on Liassic Madreporaria,
107; on Madreporaria from the In-
ferior Oolite, 387, 443.

Tomistoma, in the Miocene of Malta,

1

Surface-deposits at

Topley, W.,on Erosion of Sea-coasts, 26.

Transactions of Cumberland and Durham
Association, 328.

Traquair, R. H., New Species of
Palzoniscidee, 440.

Triassic Outlier off the Lizard, 284.

LRICH, E. O., American Palmon-
tology, 374.
Unconformity between Bagshot Beds and
London Clay, 402.
Undisturbed Spots in Earthquake-shaken
Areas, 157.

Index.

UNE

Uneroded Surface Rocks under a Talus,
65.

Ungulata, Dr. Max Schlosser on the,
326.

United States Geological Survey, 172,
464.

AN DEN BROECK, On the Tuffeau
de Ciply, 10.

Vertebrata of the Tertiary Formations of
the West, 410, 465, 512.

Vienna, Annals of Natural History
Museum, 169.

Volcanic Eruption in New Zealand, 523.

Volcanic Rocks of North-eastern Fife,
330.

at Nuneaton, 322, 557.

AVA OES: W., Salt Range Fossils,
463.
Waller, T. H., Volcanic Rocks at Nun-
eaton, 322.
Walton Common, Section through, 98.
Warwickshire Coal-field, 540, 557.
Warwickshire, Two Rhetic Sections in,
185.
Water-bearing Nodules in the Lower
Greensand, 381.
Supply from Wells, 111.
Watson, W., on the Black Rock of
Kiltearn, 29.
Wethered, E., on the Pea-Grit of
Leckhampton Hill, 525; Structure
and Organisms in Limestones, 529.

583

ZOO

Whitaker, W., on some Borings in Kent,
41,510; onthe Waterworks at Brighton,
32; Water Supply from Wells, 111;
Well-sections in Middlesex, 379.

Whiteaves, J. F., On Cretaceous In-
vertebrata, 129.

Witchell, E., Basement-beds of Inferior
Oolite, 186.

Woodward, A. Smith, on a Columella in
the Skull of Ichthyosaurus, 4380; on
the Genus Notidanus, 205; on Hy-
bodus dubrisiensts, 285 ; on Notidanus
amalthet, 525,

Woodward, H., on Edestus Davisit, 1;
Guide to the Department of Geology,
428; on a New Type of Perisso-
dactyle Ungulata, 49; on Recent and
Fossil Hippopotami, 114.

Woodward, H. B., Old Red Sandstone
under London, 43; Well-sinking at
Swindon, 188.

Woodward, H. P., Geological Map of
Barossa Gold-field, 278.

Worth, R. N., On a Submarine Triassic
Outlier, 285.

Wright, J., Cretaceous Foraminifera of
Keady Hill, 368.

Wynne, A. B., Geology of the Punjab
Salt Range, 131, 2386, 280; Striated
Pebble from the Salt Range, 492.

OUNG, John, on ‘‘ Cone-in-Cone,’’
139.

7 0oLoGicaL Society, 285, 430.

——————
STEPHEN AUSTIN AND SONS, PRINTERS, HERTFORD.

"
fi

. fi if %
rie 4 ‘ “ ial
p ‘

Use beets re cr Gif Badal AS xe ND ae YY ze
\y/ ANS Vv ROLET AS LING

Huyy WY WM ildinni as svUNUe iy Wey
oa MOY Ve ok UY FU vu JWWuy Yuu gesuy ex 2 vr iaheh
JM Hyg OM MAM SA
ilihennc YY
: = Anant Wi

SWUM WUC jbir MY uu

y \ =a hy | tid ; flees SRG) Nell ! y
ee se ‘0 aw tuu gut wtgigiods

| es

Vi
YOUU

ana wiv
yi Watt. vi

all

. vive Ke vi
Soi Wy

(as) a lhe A= Naa ea wy, oe ae Wel ea y | WS NG
" es PO ES on

ons

is
\

<Z

YY

~

Ne

SASAY

Were ua"
woconiagigto™

veuus UNOS

(<a re

ES eye AS Jue: uve

\S

= a
cay ne
a oat?

No MLSS WU Wy WV vy
\ w Ai ic ’ ‘ails chi YW

HAND ee hs NF Ww? ow ¥ WwW ~~. FV yy _ WWW (Se fete ue OW OS Ee - ee her aN
AU AUAUU, WVU WNW, vy te rT "YY Yee uve WAY |
j\- GUYS YY Ate SOLO WY veyy AAS S : WI yy AVIS VAS Vy Ah if ¥UY| Y ;
AAV bets 1 ach irl hal © poceineTe BATA A RARRAA Gi te
| WM Wd Voy YY | Ji Y Vs 2X Moy Luv V/ wis Wy L en fh j
Z © Pst GOAOS! SARA “ee Ww! Miwon YY ewe wy, cose Me
2i™, & i NS e S SCS Di ones eee WAU, us ¥ : : Ys He US We

ne

SEF 10 2010
Pare
LE
mike
me
<< a
C « &i
wee KC « c
a RG
©
Ce
Kan
axe
—
reg
<
rG
Cc
Ci

WY “ Wee,
MM uj Ny vy Nin WY

WVU GUI OC yoy VY

YUU Vi GUY So gt in
Vy VY Mo Md MYUUE WAU “WY

wy PADI ANS YS ot ~
ne Ad “WU
Holt me 3 v v
ive SW y \\ \ Ny UI 3 ww wie \ vy |
, “V V 4 / V / ¥\ % KY nV Wi yY wy CG oe ee Sa
1 ¥ ( j | VI / LOSING \s V vi Ng Y uty IV YW YUY Ny |
Soe YY UU Aerie Shs yuu ee we Wu SAS RAC REG we Ye YOUR

- \ A \ \
y Xt y\ Nye f re ple AA ef eee Rey epee \ /\ 1 | | se “1
Wei SAAS, VY \ tee Ae tod SU Nop eA fy MIG ws ji 4 ey AeA ea h VY vi ew | AY Hite} dhe (eal ji AN w/ Gr q 7

|

|

i

|

CC Le AEC CC. SN EE ge cae eS =-
Ci CL KE CK SO QC x qu a ee OS <a a a, EEG

INN

Se -

GC Ke

Dewees oes > # a
6 SS — SS ; Se =
_. We : = i ear oe aa —— SS Ss
“ ; ibe LOE E ‘ i a 7 m= = oa fies § EA id
5 = ‘ Cee - : : CG &E é é * ;
ee Gaia. LE CERT r =, F = aa

=
=a

VWiidgg 3 2044 102 911 989

AS s
ws
B
q

La

a eee : K€
ae Sea Ae a ie
CEE R - ee ee a =
SE. ant COC

Ce