bluuebunny/crossref_metadata_2025 huggingface dataset:
On the Geology of the South Devon Coast from Torcross to Hope Cove
Authors: Bonney T. G.
Published: October 2009

T
he
wild and picturesque coast which fringes the most southern part of Devonshire has already attracted the notice of not a few geologists. As, however, a detailed list of their writings, carried up to the year 1879, will he found in a valuable paper by Mr. Pengelly, published in the ‘Report and Transactions of the Devonshire Association for the Advancement of Science, Literature, and Arts’ (vol. xi. p. 319); and as no material addition to our knowledge, so far as I am aware, has since been made, it is needless for me to burden the pages of our ‘Journal’ with a copious history of the literature of the subject. Suffice it to say that the geology of this district is described in the paper of Sedgwick and Murchison “On the Stratified Deposits of Devonshire” (Trans. Geol. Soc. ser. ii. vol. v. p. 633), and in the “Report” of Sir H. De la Beche. In these two works, which after the lapse of more than forty years are still of the greatest value, the stratigraphy of South Devon is excellently sketched, and the main problems relating to it are clearly enunciated. Briefly stated, the latter amount to this: Does this district indicate a progressive metamorphic action, which increases in intensity as we proceed southwards? or do we find here two distinct and independent series, the southern, a group of highly metamorphosed rocks, true schists, the northern, slates, such as are common elsewhere in Devonshire, with no signs of a transition from
British Cretaceous Nuculidæ
Authors: Gardner J. Starkie
Published: October 2009

T
he
Nuculæ
and
Ledæ
with their allies, are now generally separated from the Arcidæ, and in a palæontological point of view this separation is amply justified; for their distinctive characters have persisted throughout many geological periods, and may be recognized to some extent now in the Silurian fauna. The family of the Nuculidæ includes a number of genera and subgenera which it would be inconvenient to adopt here; for while probably every geologist would distinguish a
Nucula
from an
Area
or from a
Leda
, even if imperfectly preserved, none but a specialist would be able to separate a
Yoldia
from a
Leda
, and only then in the event, not common among Cretaceous fossils, of the internal characters of the shell being revealed. Were all adopted, the Nuculidæ from the Gault of Folkestone alone would require seven subgeneric names; but their distinctive characters are relatively too trivial to be of palæontological value.

The details of the hinge and the position of the muscular attachments do not appear to be of very great importance in this group and are not always visible in the fossils; they are therefore omitted from the abridged descriptions of the species.

Both
Ledæ
and
Nuculæ
occasionally abound in the marine formations of the Cretaceous system, except in the White and the Red Chalk, whence they may have been dissolved out. The species do not differ greatly from those of the Jurassics, nor from those of the present day.

Besides the definition of new or imperfectly described species,
On the Cambrian Conglomerates resting upon and in the vicinity of some Pre-Cambrian Rocks (the so-called Intrusive Masses) in Anglesey and Caernarvonshire
Authors: Hicks Henry
Published: October 2009

I
n
papers which I communicated to the Geological Society in 1877 and 1879, I brought forward evidence to show that some rocks in Caernarvonshire and Anglesey which were indicated on the maps of the Geological Survey as great eruptive masses intruded into strata of Cambrian and Silurian age, were really rocks of Pre-Cambrian age. I pointed out that there was the clearest evidence to show that the lowest Cambrian conglomerates known in those areas, instead of having been altered by these so-called eruptive masses, as would be inferred from the maps of the Geological Survey, repose unconformably upon the rocks composing these masses, and were mainly built up of materials derived from them by denudation. In the paper of 1877 I stated that the pebbles in the conglomerates were “usually distinctly rounded and generally imbedded in either an unaltered or semicrystalline matrix, from which they can be easily removed,” and that “they were evidently in their present state, as regards consolidation, before they were cemented together to form the conglomerates, and must have been derived from rocks highly metamorphosed at that time, such rocks, indeed, as now occur immediately under them, and which, we venture to believe, belong to a Pre-Cambrian series.” In the same paper I mentioned that the false appearance of being intrusive masses exhibited by these rocks and “the passage by gradual alteration mentioned by various observers, are mainly due to the fact that the matrix in the conglomerates has been derived from rocks immediately below or
Petrological Notes on some North-of-England Dykes
Authors: Teall J. J. H.
Published: October 2009

T
he
object of the present paper is to give a petrological account of some North-of-England dykes. The specimens on which the observations are based were mostly collected by myself during the winter of 1881–82; a few, however, were given me by Prof. Lebour and other friends.

In the microscopic work I have derived great assistance from my friends Mr. I’Anson of Darlington and Dr. Trechmann of Hartlepool. To Mr. I’Anson I am indebted in another way; for he kindly handed over to me the analysis of the Great Ayton rock which was prepared for him by Mr. Stock. My indebtedness to the latter gentleman, and also to Mr. Stead of Middlesborough, will appear in the sequel. Without the valuable chemical work communicated by these gentlemen my paper would indeed be incomplete. It is no part of my purpose to describe the mode of occurrence of these dykes, and therefore the general course of each is indicated mainly by reference to works already published. One or two new facts of importance are, however, given; especially in relation to the dying-out of dykes beneath the surface.

The dykes are first of all described in the order of their occurrence from south to north, and at the conclusion of the paper some general remarks on their mutual relations are given.
On the so-called Spongia paradoxica, S. Woodward, from the Red and White Chalk of Hunstanton
Authors: Hughes T. McKenny
Published: October 2009

T
he
sea-cliff of Hunstanton in Norfolk offers one of the most interesting sections along our eastern coast. We there have an opportunity of examining in detail all the beds from well down in the Lower Greensand fairly up into the Chalk, and we see that, where we should have expected to find the Gault and Cambridge Greensand, there is instead a conspicuous band of red rock about 4 feet in average thickness, which, when examined closely, seems to pass up into the Chalk above, part of the lowest bed of which is mottled with stains and nests of red earthy oxide of iron, and to pass down through more and more sandy layers into the Lower Greensand underneath, as if it was either largely derived from the Lower Greensand, or the conditions of deposit of the Lower Greensand were still going on while the earlier part of the Red Rock was being formed. When we stand off at a little distance, however, the line of demarcation appears more sharply defined by the results of weathering. Palæontologically, too, it is a section of great interest. The Red Rock and the lower part of the Chalk are full of organisms of various kinds, of which lists have been given by Taylor, Samuel Woodward, Rose, Wiltshire §, Seeley ∥, and others; and in these lists we find repeatedly the description or mention of a fossil which, from the time of Woodward on, was referred to under the name of
Spongia
or
Siphonia paradoxica
.
On the Occurrence of Antelope remains in Newer Pliocene Beds in Britain, with the Description of a new Species,
Gazella anglica
Authors: Newton E. T.
Published: October 2009

I
n
the year 1878 Mr. H. B. Woodward, of the Geological Survey, obtained from the Norwich Crag at Thorpe, near Norwich, a fragment of a horn-core closely resembling the corresponding part of a Goat; and although the genus was not known to occur in beds of undoubted Pliocene or Pleistocene age in Britain, I felt justified in calling attention to it by inserting “Capra?” in the list of Mammals from these beds, which appeared in the Survey Memoir ‘On the Country around Norwich’ (1881), p. 55. More recently my colleague has been fortunate enough to get another and much more perfect horn-core from the same place. As will be seen from the description given below, there can be no question as to the close relationship of this specimen to the Antelopes, and more especially to the
Gazelles
; but it is not certain that the first-found of these horn-cores belongs to the same genus as the second; indeed, the slight impressions of the brain convolutions, which are traceable on the inner wall of the frontal bone, seem to indicate a greater complexity of these parts than is found in the second specimen. However, seeing that we now have undoubted evidence of an Antilopine form occurring in these deposits, it will perhaps be better to refer the less perfect specimen to the Antilopidæ, and not to the genus
Capra
.

The second and more perfect specimen (Pl. XIV. fig. 1) consists of a right horn-core with its frontal bone and a fragment of
The Silurian Species of Glauconome, and a Suggested Classification of the Palæozoic Polyzoa
Authors: Shrubsole George W. , Vine George R.
Published: October 2009

T
he
genus
Glauconome
, originally founded by Goldfuss, was so modified by Lonsdale, as to become virtually a new genus, of which
Glauconome disticha
from the Dudley Limestone is the type. Later on came the discovery by Sedgwick of apparently a similar polyzoan from the Bala beds of North Wales. This was regarded by Prof. McCoy as identical with the Wenlock species, and, as such, has been generally received.

We have been of late examining these Silurian species of
Glauconome
, both as to their identity with one another and their connexion with the Carboniferous and Devonian species, and we find that the Bala and Wenlock species are not even generically related, while the members of the large Carboniferous group have not the least affinity with the type species from the Wenlock beds.

The present Bala, Devonian, and Carboniferous species evidently belong to a modified group of the Cyclostomatous Polyzoa, while the type species from the Wenlock can only be classed in a distinct division of the Polyzoa, for which at present no provision is made.

In coming to this decision, we have been mainly guided by zoarial form, and not outward resemblance. Evidence in this direction has been carefully sought for in the several species. In
Glauconome disticha
from the Wenlock Limestone we find the cell open and exposed throughout its entire length; this, we find, is not accidental, but characteristic. The cells are built up of a series of thick longitudinal walls running parallel with the branch, and divided at
On Strain in Connexion with Crystallization and the Development of Perlitic Structure
Authors: Rutley Frank
Published: October 2009

I
n
a paper on “The Microscopic Structure of the Vitreous Rocks of Montana, U. S. A.,” read in connexion with a paper upon the mode of occurrence of those rocks by Mr. J. Eccles, and since published in the Quarterly Journal of this Society (vol. xxxvii. p. 391), I had occasion to allude to a peculiar phenomenon of depolarization in the little grains of obsidian constituting a rock which was very aptly called obsidian sandstone by the officers of the U. S. Geological Survey. I there pointed out the relation which the depolarization bore to the perlitic structure visible in the little obsidian fragments, and also indicated the probable connexion of these strains in the glass with the development of crystals.

The following notes may serve still more clearly to verify the statements then made.

The present observations were made upon a small but thick slice of obsidian from Java, given me some years ago by Prof. W. Chandler Roberts. On examining this section under the microscope, in plane polarized light, a considerable number of crystals may be seen, and in nearly every instance the surrounding glass, where it comes in contact with the crystal, shows very well-marked depolarization, which I think I might say, without any doubt, is due to the tension or strain produced in the glassy obsidian by the development of crystals or by a strain preceding the development of crystals, as I suggested in the paper already alluded to.

In Pl. XVIII. fig. 1, for instance
On a new Specimen of
Megalichthys
from the Yorkshire Coal-field
Authors: Miall L. C.
Published: October 2009

A
large
and unusually complete example of
Megalichthys Hibberti
was lately found in the roof of the Halifax Hard Bed at Mr. F. B. Ellison’s Firebrick Works, Idle, near Leeds, by Mr. Andrew Oldroyd. The fossil, which was presented by Mr. Ellison to the Museum of the Leeds Philosophical and Literary Society, is externally in good preservation and but little disturbed; the ventral surface is uppermost, and the pectoral, ventral, anal, and caudal fins can be more or less satisfactorily made out. The dorsal surface and vertebral column are altogether absent; but nevertheless this specimen gives more information concerning
Megalichthys
than any other which has come to my knowledge. Quite unusual pains were taken by Mr. Oldroyd to recover every fragment of the fish. The remains measure 3 feet 8½ inches in length, of which the head includes about 10 inches and the tail about a foot; 5 or 6 inches appear to be wanting from the end of the tail. The fine skull of
Megalichthys
figured by Agassiz in the Poissons Fossiles, and still in the Leeds Museum, is a trifle larger than the corresponding part of the new specimen.
Megalichthys
may therefore have attained a length of from 4 to 5 feet.

The skull of the fossil now under description shows the mandible and mandibular teeth, a little of the fore end of the snout, the opercula and the jugular plates; but no novel feature is thereby brought to light.

The pectoral fins are quite distinct and nearly
Observations on the Geology of the Line of the Canadian Pacific Railway
Authors: Dawson J. W.
Published: October 2009

H
aving
had an opportunity last summer of passing over the line of this railway, and of examining some of the sections exposed on the road and in its vicinity, it may be useful to note the facts observed.

All of the country on both sides of the line has been more or less explored by the officers of the Geological Survey, more especially by Dr. Selwyn, Dr. G. M. Dawson, and Dr. R. Bell; and without repeating what they have published, I shall confine my remarks chiefly to facts discovered or brought into greater prominence in the construction of the road.

Between Ottawa and Port Arthur the road was only partially opened last summer, though it had penetrated into the region of typical Huronian rocks north of Georgian Bay. Next summer it will be opened throughout, or at least to Algoma Mills, whence steamers will run on Lake Superior to Port Arthur. This section of the road will be of great geological interest, as it abounds in cuttings through Laurentian and Huronian rocks, and will also expose the Kewenian or Upper Copper-bearing series and other formations which, though newer than the Huronian, are believed to be Pre-Cambrian. Last summer, travellers were conveyed by steamer from Collingwood to Port Arthur, through Lakes Huron and Superior, and it was at Port Arthur that their geological experiences began.

Port Arthur is at the head of Thunder Bay and opposite it are the grand trappean masses of Thunder Cape and of the islands in
On the Serpentine and associated Rocks of Porthalla Cove
Authors: Collins J. H.
Published: October 2009

T
hese
rocks were briefly described by me in a paper communicated to the Royal Geological Society of Cornwall, in the year 1879, as “much-contorted strata of slaty green and red serpentine and hornblende rocks in numerous alternations, all, however, having a strike to the N.N.E.”

In the same paper I stated my belief that the whole series consisted of “highly altered Lower Silurian stratified rocks.”

The Cove has been more recently visited by Prof. Bonney, and his remarks thereon were published in the Quarterly Journal of the Geological Society for February 1883. A brief reference is therein made to my paper, and the Professor considers that I have “completely mistaken the relations of the rocks to each other”. I am glad therefore to be permitted to bring my views on this subject under the notice of the Society in sufficient detail to enable me to justify the opinions so distinctly controverted, so far at least as to show that the hornblende schist, serpentine, and other rocks described are distinctly interstratified, and that there is a real “passage” from one to the other. I am more especially glad of this opportunity, because the real question at issue is that of the origin of certain masses of serpentine rock, than which there are few more interesting or more important in the whole range of chemical geology. With much of what Prof. Bonney has written concerning the rocks of the Lizard district I very cordially agree, and I can from personal observation corroborate
On the Recent Encroachment of the Sea at Westward Ho !, North Devon
Authors: Spearing Herbert Green
Published: October 2009

F
or
the last nine years the sea has been encroaching on the land near Westward Ho ! at the rate of about 30 feet a year. This encroachment only affects about a mile of the coast-line, but it is of special interest both on account of the formations which it exposes and the rapidity with which the sea has eaten into a district which had hitherto been apparently but little injured by it.

I have not been able to obtain any correct map of the district older than the parish map of Northam, and that does not give the actual limits of high tide with any accuracy, so that it is impossible to say how much further the land may have extended seaward when Westward Ho! was still unnamed and almost uninhabited. A very old inhabitant, however, told me that the grass used to extend for several yards beyond the old road leading from the ladies’ baths to the Burrows, which was still in existence in 1875, when I first went to Westward Ho!

The accompanying map is reduced from one constructed from an actual survey that I made in 1879, but the line of the top of the former ridge in 1875 was sketched in from memory, aided by the parish map.

The district which is principally affected by the encroachment is a large sandy common called the Northam Burrows. This common is the southern part of the delta of the united rivers Taw and Torridge, and the inland part
On Further Discoveries of the Footprints of Vertebrate Animals in the Lower New Red Sandstone of Penrith
Authors: Smith George Varty
Published: October 2009

H
itherto
not many footprints have been met with in the Penrith Sandstone. Impressions of the same nature as those found in the equivalent strata at Dumfries have been previously met with at Brownrigg in Plumpton, about five miles north-west of Penrith; and the late Mr. Binney and Prof. Harkness have noticed similar impressions in the flaggy beds near Penrith, but they were not so distinct as those found at Brownrigg. A notice of the discovery of a variety of impressions in the Lower New Red Sandstone of Penrith may therefore be interesting, and may serve to throw some light upon the general nature of the terrestrial vertebrate life of that period.

The footprints now referred to were met with in a quarry situate on the eastern slope of a hill, at a point about 200 yards north of the highway from Penrith to Alston, and about three and a half miles east of Penrith.

The geological position of the sandstone is shown approximately in the accompanying diagram section, which is based upon one by Prof. Harkness. This shows that the Penrith Sandstone rises from beneath the Magnesian Limestone, traces of the latter rock being found at a short distance to the north-east of the quarry, in the bank of the river Eden.

The tracks on cast No. 1 appear to be those of an animal which evidently used its fore feet simply as supports, while throwing the weight of its body mainly on its hind feet. The impressions made by
The Range of the Palæozoic Rocks beneath Northampton
Authors: Eunson Henry John
Published: October 2009

I. P
revious
K
nowledge
of the U
nderground
G
eology
.

T
he
first investigation into the underground geology of Northamp-tonshire, or the strata lying immediately beneath the thick deposit of the Liassic series, consisting of limestones and clays, which covers the county to a large extent, was made in the year 1836. A company was then formed and a shaft sunk near the village of Kings-thorpe, about two and a half miles N.E. of the town of Northampton, for the purpose of reaching the Coal-measures, which, upon the advice of practical men, it was thought could be found at no great depth below the surface, ”though competent scientific individuals, as Mr. Smith, the father of English geology, and Mr. Richardson, then of the British Museum, expressly denounced it as a mistaken enterprise“.

An account of this shaft (fig. 4, p. 496) has been given by the late Mr. S. Sharp, F.G.S., in the ‘Geological Magazine,’ from which I extract the following passage t :—

“No accurate detailed section of the shaft was taken at the time; but at a depth of 210 feet from the surface, a water-yielding ‘Limestone rock’ in the Middle Lias (Marlstone)was pierced, which produced 36,000 gallons of water per hour. At a depth of 880 feet (as is stated in pencil-notes on a diagram in my possession, which notes are said to have been made by Dr. William Smith, F.R.S., F.G.S., &e.) the New Red Sandstone was reached, and a flow of brackish water of a like volume
On the Internal Structures and Classificatory Position of
Micrabacia coronula
, Goldfuss, sp.
Authors: Duncan P. Martin
Published: October 2009

Micrabacia coronula, Goldfuss, sp., called
Cyclolites
by William Smith (1816), is a characteristic fossil of the Upper Greensand, and has been found at Warminster and, according to W. Smith, at Chute Farm and Paddle Hill, near Dunstable, and in the beds at Essen and Le Mans; it is also found in the “Cambridge Greensand.” Bolsche has described a
Micrabacia
from the Senonian.

The external characters of the species have been beautifully delineated by Milne-Edwards and Jules Haime, in their monograph of the British Fossil Corals , and the description of the specimen used as a type is, as might be anticipated, careful and correct. Allowing for variation in some parts, the description permits any specimen to be recognized, specifically, from the appearance of the external structures. It does not appear that these authors made sections of this coral, and as their work was classificatory and not necessarily morphological, they probably did not think it necessary to investigate the internal structures specially.

The generic diagnosis of the type was also carefully given by Milne-Edwards and Jules Haime, and the genus
Micrabacia
was separated from the genus
Fungia
, Dana, by them.

They placed the genus in the family of Aporose Corals called Fungidæ by Dana, and in their own subfamily Funginæ, which includes Fungidæ with perforated walls. The generic and specific diagnoses and the synonymy are given in the ‘Histoire Naturelle des Coralliaires,’ vol. iii. p. 29.

After the careful descriptions of these authors had appeared, came the work of M. de
The Archæan and Lower Palæozoic Rocks of Anglesey
Authors: Callaway C.
Published: October 2009

In papers communicated to this Society and the Geological Magazine I have described in some detail the Archæan formations of Anglesey. I came to the conclusion that there was no satisfactory evidence of more than two of these systems, the Gneissic and the Slaty—the former metamorphic, the latter, on the whole, hypometamorphic, but passing here and there into true schists, hardly less altered than some of those which occur in the older series. This work was too laborious and absorbing to permit me to pay minute attention to the Palæozoic strata of the island; and this was the less necessary, since other workers were approaching the investigation from the side of the newer rocks. Their labours tended strongly to support my views, so far as they referred to the central part of the island; but much remained to be done in the north and west. I therefore determined to work round the margin’s of the Archæan areas on which Holyhead and Amlwch are respectively situated, and I have had the satisfaction of ascertaining that these masses are fringed on the east and south respectively by shore-deposits, which furnish evidence similar to that which has been for some years familiar to us in the conglomerates which overlie the central axis. I have also discovered most interesting proof of the relations between the two Archæan systems.

A. R
elations
B
etween
the
A
mlwch
A
rchÆan
M
ass
and
the
P
alÆozoic
R
ocks
to
the
S
outh

AS the Palæozoie strata of Northern Anglesey dip in
On the New Railway-Cutting at Guildford:—The Pleistocene Sands and Drift-Gravels observed there
Authors: Godwin-Austen H. H.
Published: October 2009

In December 1880 the following note of the southern end of the cutting on the Main Line just north of Guildford station was taken, the eastern side having been recut to widen the line:—

This section, though not so clear as it was when fresh cut, is still well displayed, and the shell-bed is very distinctly seen.

This cutting was described long ago by Prof. Prestwich; but the details of the Woolwich and Reading beds may be useful for comparison with the section on the other side of the valley.

The new cutting north-east of Guildford, on the Guildford and Surbiton direct Line, now in process of formation, is of great interest, not only as showing a thick mass of drift, resting very irregularly on the Chalk, but also as again opening up the Reading beds, which are so rarely seen in this neighbourhood. It begins near the eastern end of King’s Road (Stoke road), and in a sharply curving course cuts the London road just north of Alderney Place, and then runs roughly parallel with that road to the south of Oak Lodge; so that it is about a mile long.

Owing to the northerly dip the Eocene beds occur only at either end, the central and deeper part of the cutting being more to the south, and showing only chalk beneath the drift, the thickness of which latter, moreover, may have some effect in carrying the boundary-line of the Eocene beds to the north.

At the western end
On some Remains of Fossil Fishes from the Yoredale Series at Leyburn in Wensleydale
Authors: Davis James W.
Published: October 2009

In Yorkshire the fossil remains of fishes in Carboniferous strata other than those of the Coal-measures are comparatively rare. Some species have been found in the Millstone-grit series, notably in a calcareous bed of sandstone at Hebden Bridge, near Halifax. Immediately below the Millstone Grit in Wensleydale there are a number of alternating beds of limestone, shale, and sandstone, about 1000 feet in thickness, to which Prof. Phillips applied the term “Yoredale Series” In the uppermost bed of these rocks, namely the Crow Limestone, a number of fish-remains have been discovered, and in the next limestone, about 60 feet lower in the series, a most important stratum has been found, which contains an immense assemblage of the remains of fossil fishes of extremely varied and, in some instances, extraordinary types. The limestone was named by Prof. Phillips the “Main Limestone,” and is locally known by the term “Red Beds,” derived from the reddish colour of the limestone. It has a crystalline texture and presents a coarse and rough appearance. It has been worked at the Harmby limestone-quarry near the railway-station at Leyburn, and it is from this quarry that the greatest number of fossils have been obtained. They principally occur on one horizon about 30 feet below the original surface of the ground; and when a fresh exposure of this horizon or stratum is made during the operat:ion of quarrying, the fish-remains, consisting for the most part of teeth, and an occasional spine, may be seen scattered over the surface
A Critical and Descriptive List of the Oolitic Madreporaria of the Boulonnais
Authors: Tomes Robert F.
Published: October 2009

I have been favoured from time to time by M. Rigaux, of Boulogne, with specimens of corals for determination, which had been collected by him in the Great Oolite and Coral Rag of the Boulonnais. He has quite recently very kindly afforded me the additional opportunity of studying the whole of his collection of specimens; and the results of a comparison made between them and English species will form the substance of the present paper.

It will be observed that I now regard
Isastræa moneta
as a second species of
Bathycœnia
its very great similarity to the Fairford species, Bathycœnia Slatteri, on which I founded the genus, having been already noticed by me. The discovery of some forms apparently allied to that genus, which nevertheless are found to possess well-developed tabulæ, renders the position of Bathycœnia in the Eusmilinæ more than doubtful.

In my paper on the Corals of the Great Oolite, I hazarded some remarks, accompanied by explanatory figures, on a species of coral from the bottom of the Great Oolite near Stonesfield, which from the presence of distinct tabulæ and the very feeble development of its septa, I placed, though not without some hesitation, among the Zoantharia Tabulata. For that species, if it proved to be distinct from the one on which was founded the genus
Cyathophora
, the generic name
Depaphyllum
was proposed. But I am still in uncertainty as to the proper generic nomenclature of the species, because I do not yet know whether the genus
Cyathophora
Notes on the Foraminifera and Ostracoda from the Deep Boring at Richmond
Authors: Jones T. Rupert
Published: October 2009

These comprise six specimens of
Cristellaria
and one
Lituola
. The latter may be regarded as
L. nautiloidea
, var., and is small, discoidal, depressed (slightly biconcave), with blunt or rounded edge. It belongs to the
Haplophragmium
division, is much like the recent
H. emaciatum
, H. B. Brady, ‘Report on the Foraminifera obtained during the Voyage of the “Challenger,” p. 305, pl. 33. f. 27, and is not far removed from
H. nanum
, H. B. B., and
H. acutidorsatum
, Hantken; but the last is involute, instead of evolute, in its growth.

The specimen before us may be termed
Lituola nautiloidea
Lam., var. (
Haplophragmium
)
depressa
, nov., or, for convenience,
L. depressa
. It looks so smooth and worn that it is possibly a
derived fossil
. Pl. XXXIV. fig. 2.

Of the
Cristellarice
, which are all of small size, and some minute, there are the following species or varieties:—

(1)

Cristellaria rotulata
(Lamarck), thin-edged, with convex umbilicus, and raised septal lines; the chambers are rather small, very oblique and subfalcate, about nine in the last whorl (Pl. XXXIV. fig. 9). There is also a very small, ill-grown
C. rotulata
, with the posterior angle of some of the chambers projecting from the circular edge; not an uncommon condition.

(2)

Cristellaria cultrata
(Montfort), with keel, central boss, thick and raised septa, and about 7 chambers in the last whorl, Pl. XXXIV. fig. 11.

(3)

A less circular (more elliptical) variety of the last-mentioned form, with 6 chambers visible, the last of
On a new Deposit of Pliocene Age at St. Erth, near the Land's End, Cornwall
Authors: Wood Searles V.
Published: October 2009

In the autumn of 1883 my friend Mr. F. W. Harmer, F.G.S., being at Penzance, chanced to hear of the occurrence near that place of a bed containing some shells not recognized as now living on the coast of Cornwall. Being introduced to Mr. Thos. Cornish, of Penzance, as a gentleman who had taken an interest in the matter, he got him to forward to me such of the shells as he possessed. These consisted of specimens of
Nassa mutabilis, N. serrata
, and
Turritella triplicata
; and I sent them to Mr. Robert Bell, F.G.S., to see and to show to Dr. J. Gwyn Jeffreys. We all three doubted their being genuine, the
Nassœ
presenting, indeed, the appearance of imperfect fossilization.

Sometime afterwards Mr. Cornish sent me some more specimens. These removed my doubts; but from the incredulity with which Mr. Bell was met in the comparisons which he made of them for me with specimens in the recent and foreign collections of the British Museum, I pointed out the desirability of having the pits reopened before I brought the matter to the attention of the Society, and this Mr. Cornish determined to have done.

The past exceptionally dry summer in Cornwall has afforded the opportunity for this; and on the 26th of August last a party consisting of our Foreign Secretary, Prof. Warington Smyth, and twelve other gentlemen, mostly geologists, residing in the county, accompsnied Mr. Cornish and witnessed the reopening of one of the disused excavations, obtaining also a
On the Lower Eocene Plant-beds of the Basaltic Formation of Ulster
Authors: Gardner J. Starkie
Published: October 2009

The general features of the basaltic district of Ireland have been too frequently described to need more than a few introductory words here. It is situated in the N.E. of Ireland, and forms a plateau with steep escarpments on every side, except in the direction of Lough Neagh. The formation rests upon a very uneven surface, and the thickness of the lowest of the three divisions into which it has been classified is thus very variable. It is described by Hull as “silicated felspathic trachytes, porphyry, pearlstone, pitchstone.” But a good deal of the lava resting upon the Chalk appears outwardly to be amorphous trap. The second division contains all the plant-beds hitherto found in the basaltic formation in Ireland, with the possible exception of those of Lough Neagh. The third is composed of solid sheets of columnar and amorphous basalt. The greatest total thickness observed in Ireland is at Sleamish, a mountain 1437 feet high, all that is visible (at least 1100 or 1200 feet) being composed entirely of basalt. These basalts have been eroded on a colossal scale, for the valleys are scooped out of solid horizontal sheets, as pointed out by Conybeare to this Society so long ago as 1816. They seem to have formed almost the southern limit of a formation which once stretched continuously to Iceland, and to what thickness they were originally erupted can never be known ; but the upper or columnar basalt series, now only 400 or 500 feet thick in Antrim,
The Tertiary Basaltic Formation in Iceland
Authors: Gardner J. Starkie
Published: October 2009

A grant from the Government Fund enabled me to visit Iceland 1881, with a view of studying its interbasaltic flora. I explored considerable part of the island and visited every locality that I could reach where lignite had been met with. I did not take notes of some of the localities where my visits were hurried; but the conclusion I invariably arrived at was, that the sedimentary deposits in which vegetable remains are found, are situated among the glassy rhyolitic flows above the columnar series of basalt. The rhyolites are usually pale in colour, and with banded structure, but are sometimes black pitchstone or obsidian. They cap the loftiest mountains of the district west of Akreyri, and extend at least to Baula, a mountain in the same latitude as Snaefell, and possibly beyond this. They also occur on the east coast, though I did not reach any of them in that part of Iceland, which I only visited from the Danish mail-boat, which calls in many of the fiords. I did not pay particular attention to their thickness, but at Sandafell I measured 30 feet of white, pink, ivory-coloured, and black glassy lavas. The thickness is, I believe, sometimes greater than this, and they are interrupted and overlain by smaller flows of basalt. The horizon is, however certainly continuous, and marks a very definite stage or phase in the great series of Tertiary eruptions which extended from Ireland to Iceland in Eocene times.

I cannot yet present data to show
The Drift-deposits of Colwyn Bay
Authors: Reade T. Mellard
Published: October 2009

In a former paper I gave a short sketch of the drift disclosed in the ballast-pit at Colwyn-Bay station; and as in February of 1884 I had an opportunity of extending my observations over a larger area, I now propose to give an account of them.

From Colwyn Head to Rhos Point is a distance of about three miles; and all along the shore, except where obscured by the Colwyn Bay parade or grassed over by the railway company, are to be seen in cliffs excellent sections of the drift.

This drift, extending backward to the foot of the hills which sweep in a curve from headland to headland, rests nearly wholly on the Silurian rocks, representatives of the Wenlock Shale.

Colwyn Head or Penmaen Cliffs, and Rhos Point, are denuded remnants of the Carboniferous Limestone, and near to each of these headlands the drift is seen to rest directly on the limestone, there being no exposure of the underlying Silurians anywhere to be seen in Colwyn Bay.

The surface of the drift is remarkably level, excepting where it gradually creeps up the hills. Most of the houses in Colwyn Bay are built upon it. It is crescent-shaped on plan, thinning out towards the outward curve, which rests on the hills, and thickening towards the Bay.

The drift may be roughly grouped into three divisions in ascending order, as follows :— 1.
Bluish-grey Till
(bed l, figs. 1 & 2), hard and tough, evidently composed of the combined grindings or
The Boulder-Clays of Lincolnshire. Their Geographical Range and Relative Age
Authors: Jukes-Browne A. J.
Published: October 2009

In section 3, we came to the conclusion that the brown and mottled clays of the Fen-border and the Ancholme valley were newer than the Chalky Boulder-clay of those districts; further that there was a decided break and an apparent unconformity between the two groups. In the last section I denied the existence of any break in the Brown-clay series of East Lincolnshire (
i.e.
the Purple and Hessle Clays), and showed that Mr. Lamplugh holds the same opinion with regard to the continuity of this group along the Holderness coast. It seems therefore only reasonable to conclude in the first place that the Glacial beds found on the west and on the east of the Lincolnshire Wolds do not form parallel series. If the Chalky Boulder-clay and the Purple Boulder-clay were correlatives, we should be confronted with the anomaly of a continuous succession existing on one side of the Wolds, while there is a discontinuous succession on the other.

Assuming that they are not parallel series, and also supposing for the moment that the brown clays on either side of the dividing ridge in Lincolnshire are complete correlatives, then it is the Chalky Clay which is unrepresented on the eastern side. Now in East Lincolnshire the base cannot be seen; but in Yorkshire there is a grey and chalky Basement-clay (beneath the Purple-clay) which was originally regarded by Messrs. Wood and Rome as the equivalent of the Upper Glacial-clay of East Anglia. Moreover we have Mr. Lamplugh's testimony as to
On the Mammalian Fauna of the Val d'Arno
Authors: Major C.J. Forsyth
Published: October 2009

§ 1. Introductory.
The Fauna of the Val d'Arno.

In the following essay on the fossil mammalia of the Val d'Arno I have subjected the list of species to a critical examination and brought it down to the knowledge of to-day. It will be sSen from the following lists that i have been able to add a considerable number of species to those known in former years.

§ 2.
Relation to the Older Faunas
.

On the boundary-line between the Miocene and Pliocene we find in southern Europe, and especially ia the region of the Mediterranean, and also as far to the east as the Siwalik mountains of India, a richly developed fauna in which the
Hipparion
is the most widely spread and important representative. This fauna is met with at Pikermi in Attica, at Concud, and at Alcoy in Spain, at Oraa and Constantine in Algeria, at Montpellier and Merit Léberon (Cucuron) in :France, at Casino near Siena, in Italy, at :Eppelsheim in Germany, as well as in Austria-Hungary, the Balkan peninsula, and in Asia Minor. Not one of the members of the fauna discovered in these localities occurs in the somewhat younger fauna of the Val d'Arno. Yarious relations are certainly to be pointed out. The two Pliocene Antelopes,
Palæoryx
Meneghinii
, Rüt., from Olivola in the valley of the Magra, and
Palæoreas
montis
caroli
, in the valley of the Arno, are closely allied to species of the same genera found in Pikermi. The same intimate relation exists between the
On the S. W. Extension of the Clifton Fault
Authors: Morgan C. Lloyd
Published: October 2009

On the right bank of the Avon, somewhat below the Suspension Bridge and a little beyond the Clifton station of the Bristol Port railway, the Clifton fault cuts across the strata somewhat obliquely. On the southern side of the fault is massive Mountain Limestone, forming the bold bluff of the Observatory Hill. On the northern side are much contorted red grit and limestone shales (see Map, p. 147).

Viewed from the opposite side of the river, the right bank, from the Suspension Bridge for half a mile northwards, shows the following features. The eastern tower of the Suspension Bridge is built on a solid mass of limestone, the western face of which fronts the river as an almost perpendicular wall of rock. At right angles to this, and parallel with the bridge-road, there is a second face due probably to a joint plane, or a minor dislocation of the strata parallel with that caused by the Clifton fault. This vertical face forms the southern boundary of a little recess in the rocks, in which lies the Clifton station. On the northern side of the station rises the somewhat dislocated mass of limestone which forms Observatory Hill, and which, on its southern side, abuts against Millstone Grit and Upper Limestone Shales brought down by the Clifton fault. The whole appearance of the side of the ravine now changes, and in place of vertical limestone cliffs there is a wooded slope. Close to the river, however, the rocks are well seen in
Chilostomatous Bryozoa from Aldinga and the River-Murray Cliffs, South Australia
Authors: Waters Arthur Wm.
Published: October 2009

The fossils described in the present paper were collected by Professor Ralph Tate, who kindly sent them over to me for description. With a few exceptions, they are from Aldinga, or the “River-Murray Cliffs.” A few small and imperfectly preserved specimens are from a bore-hole in Adelaide, representing a find which seems to have considerable geological interest. They are evidently from a clay matrix, and belong to species common in the clay of Curdies Creek. The collection furnished various Cyclostomata, which have already been dealt with in a former paper (Quart. Journ. Geol. Soc. vol. xl. p. 674).

As a considerable number of Australian fossil Chilostomata have already been described, we naturally find many old friends; but there are also several new forms of extreme interest, especially as bearing upon the question of the various modes of growth of the Chilostomata. The previous collections have furnished a large number of instances of a species growing in both Eschara- and Lepralia-forms, and we again find new examples of this, among which
Membranipora rhynchota
, Busk, in the Eschara stage, is especially interesting; and there are examples of already-known
Smittiœ
and
Monoporellœ
occurring in a reticulate form; but this time the chief interest is in a number of specimens which grow in a cupulate manner, which we might either call Cupularia- or Lunulites-form, and for convenience we will adopt the latter. There is
Lepralia edax
in this form; a
Microporella
for which the name
pocilliformis
is proposed; and, further, a second
Microporella
, which
On the Ostracoda of the Purbeck Formation; with Notes on the Wealden Species
Authors: Jones T. Rupert
Published: October 2009

§ I. Introduction.

In the ‘Geological Magazine,’ dec. 2, vol. v. (March and June 1878), pp. 103 & 277, I offered some observations on the Ostraeoda of the Purbeck and Wealden Formations, and endeavoured to determine the species already described and figured by Sowerby, Fitton, F. A. Römer, and W. Dunker, and by E. Forbes, Lyell, and P. de Loriol. One of these species was further noticed (as
Cythere
?
purbeckensis
) in the ‘Proceedings of the Geologists' Association,’ vol. viii. 1883, p. 58, together with an additional species which I had defined as
Cythere boloniensis
[
bononiensis
] in the Bull. Soc. Géol. France, ser. 3, vol. viii. 1882, p. 616.

Having been enabled, by the help of the Rev. O. Fisher, Mr. W. Cunnington, Mr. Horace B. Woodward, Mr. J. C. Mansel-Pleydell, Prof. J. F. Blake, and other friends, to add considerably to my own collection of Purbeck Entomostraca, among which are many specimens collected by Fitton and Brodie, and having been kindly aided in my practical work by Mr. E. T. Newton, F.G.S., and Mr. C. D. Sherborn, I have begun to examine and determine the whole series of Ostracodous species characteristic of the Purbeck-Wealden beds. As far as opportunities have offered, I have also studied the specimens preserved in other collections and museums.

§ II. T
he
O
stracoda
of the P
urbeck
B
eds
.

Sources of Information.

Professor Edward Forbes commenced this work of determining the Purbeck Ostracoda long ago; but his results were not fully recorded, nor, indeed, is it now
Evidence of the Action of Land-Ice at Great Crosby, Lancashire
Authors: Reade T. Mellard
Published: October 2009

In previous papers I have described a deposit of rubble-débris and red sand lying on the Triassic rocks and underlying the Low-level Boulder-clay and sands in the neighbourhood of Liverpool, which I suggested was due to the grinding and crushing action of land-ice. I also pointed out that where this deposit did not occur, the rocks, as is well known, are usually polished, grooved, and striated. Until lately no opportunity has occurred of testing the validity of this view by reference to any other than sandstone rock that such land-ice may have moved over.

In October 1884 I described, in the ‘Geological Magazine,’ a section of Keuper marls at Great Crosby previously unknown, and since then I have made frequent observations of the upper part of the marls in relation to the Low-level Boulder-clay that overlies them.

From time to time as the excavations have proceeded, it became clearly apparent that the upper part of the marls had been from some cause or other much disturbed. There were imbedded in it large angular and sometimes nearly square blocks of sandstone. These were not merely pressed into the surface, but actually imbedded in the marl at all angles. In the undisturbed marls are well-defined bands of a harder nature, and one of these bands was at one place broken up and contorted, the fragments displaced, and irregularly forced into and amongst the worked-up softer marls or shales (see fig. p. 455). This was very striking, as the band continued in an