bluuebunny/crossref_metadata_2025 huggingface dataset:
On the Intrusive Character of the Whin Sill of Northumberland
Authors: Topley W. , Lebour G. A.
Published: October 2009

1.
Introduction
.—The basaltic rocks of the north of England occur in two forms—as
sheets
lying amongst the sedimentary strata, and as
dykes
cutting through them. The intrusive character of the latter is, of course, undisputed; but there is much uncertainty in the minds of many geologists as to the character of the former.

In this paper we purpose to show, from the detailed work of the Geological Survey, that in Northumberland there can be no doubt whatever as to the intrusive nature of the bed or beds of basalt known as the Whin Sill. This conclusion can be established both by the evidence of individual sections and by the line of outcrop of the trap.

The question of the nature of the Whin Sill is of importance in three ways:—1st, as a point of theoretical geology, bearing upon the history of volcanic action in Britain; 2nd, in reference to the classification of the Carboniferous System; 3rd, in its bearing upon practical mining.

The Whin Sill is best known in Teesdale, especially in the two fine waterfalls of High Force and Cauldron Snout. It also appears along the face of the Penine escarpment, and is beautifully exposed in the “Nicks” which furrow the face of that range. Although this district is known to us, we will not stay to describe it, because it has already much engaged the attention of geologists, especially Professors Sedgwick and Phillips. It is generally supposed that there is but little evidence of intrusion there; but this
On the Strata and their Fossil Contents between the Borrowdale Series of the North of England and the Coniston Flags
Authors: Harkness Robert , Nicholson H. Alleyne
Published: October 2009

In the following communication we propose shortly to consider the various groups of strata which intervene between the great volcanic series (Borrowdale Rocks) of the Lake-district and the well-marked band of sedimentary rocks to which Prof. Sedgwick applied the name of the “Coniston Flags.” In so doing we shall have occasion to note, in a general way, the physical characters and relations of the successive deposits in question; but we shall have to draw attention more especially to the organic remains which they contain and to some indications thus afforded as to their precise age and position in the geological scale.

The base of the great Silurian series of the north of England is constituted, as is well known, by the “Skiddaw Slates,” a thick mass of sediments, originally in the condition of black mud, clearly proved by their fossil contents to be of the age of the “Arenig group” of Wales. Succeeding the Skiddaw Slates there occurs a great series of volcanic products, termed by Prof. Sedgwick the “green slates and porphyries,” to which we have elsewhere given the name of “the Borrowdale series.” These consist of ashes and breccias, alternating with ancient lavas, a portion of the series being subaerial, whilst part is of submarine formation.

Throughout the greater part of this extent, for a thickness of some thousand feet, the Borrowdale series has hitherto proved unfossiliferous; fossils, however, make their appearance in a thin band of calcareous ashes near the summit of the group (Harkness and Nicholson
Supplementary Notes on the Fauna of the Cambridge Greensand
Authors: Jukes-Browne A. J.
Published: October 2009

In a paper read before the Society in January 1875, I discussed the relations of the Gault and Chalk Marl in Bedfordshire and South Cambridgeshire, and endeavoured to show that the fossil contents of the so-called Cambridge Greensand are for the most part remaniés and have been derived from the upper beds of the Gault.

The conclusions arrived at were briefly these:—that the Upper Greensand does not extend further in a north-westerly direction than West-end Hill near Cheddington in Bucks; that stratigraphically the Cambridge Greensand is of no importance, being a mere nodule-bed at the base of the Chalk Marl; that it rests unconformably upon denuded Gault; that a greater portion of the fauna belonged originally to the Upper Gault; that the remainder, really belonging to the bed itself, are species proper to the Chalk Marl rather than to the Upper Greensand.

A full list of the species then known as existing in the formation was appended; and the derived forms were therein separated from those presumed to be indigenous to the Greensand itself. This list was mainly prepared from an examination of the large collection of fossils in the Woodwardian Museum; and my investigations resulted in the determination of many species that were previously unnamed in that collection, and in the identification of others which had been wrongly named. All these species were separately noticed, with remarks upon their determination and synonymy.

These observations, however, were by no means intended as an exhaustive study of the fauna of the
Note on the Occurrence of the Remains of
Hyænarctos
in the Red Crag of Suffolk
Authors: Flower William Henry
Published: October 2009

In the rich collection of Red-Crag fossils gathered together during the course of many years in the neighbourhood of Waldringfield by the Rev. H. Canham, now through the joint liberality of Sir Richard Wallace and Mr. Canham located in the Ipswich Museum, is a very perfect mammalian tooth, which has been placed in my hands for identification. It proves to be the right upper first true molar of an animal of the genus
Hyænarctos
of Falconer & Cautley.

In the Quarterly Journal of the Geological Society, vol. xxxiii. No. 129 (Feb. 1, 1877), at p. 133, it is recorded that, at the meeting of the Society held on November 22, 1876, “Mr. Charlesworth stated that he had obtained from the Crag a tooth which had been pronounced by Mr. W. Davies, of the British Museum, to come nearest to that of
Hyænarctos
among known Mammalia.” The tooth referred to by Mr. Charlesworth is now in the collection of Mr. William Reed, M.R.C.S., of York, who has obligingly sent it to me for exhibition to the Society. It is the corresponding upper molar of the opposite side, and so like that of Mr. Canham's collection that, except for being perfectly unworn, it might almost have belonged to the same
individual.
On
Mauisaurus Gardneri
(Seeley), an Elasmosaurian from the Base of the Gault at Folkestone
Authors: Seeley Harry Govier
Published: October 2009

T
he
Gault hitherto has yielded but scanty remains of animals referable to the Reptilia and to the Palæosauria; so that more than ordinary interest attaches to the discovery, in a comparatively perfect condition, of remains belonging to a genus found hitherto only in New Zealand, which may be regarded as distinctive of the deposit. The remains of this Plesiosaurian were first found, rolled and abraded, at the foot of the cliffs; much of the caudal region of the animal may therefore have disappeared by attrition, and by the gradual decay of the bones as exposed in the clay, which has partly invested them with selenite. These bones were sent by Mr. Griffith, the well-known Folkestone fossil-collector, to J. S. Gardner, Esq., F.G.S., who traced them to their place in the Cliff, about 15 or 16 feet from the base of the Gault, and undertook excavations which have resulted in the discovery of a tooth, of the vertebræ of the neck and back, the principal bones of the limbs, and portions of the pectoral arch. The head, the tail, the pelvic bones, and the smaller bones of the limbs, together with most of the ribs, have not been found; and it is possible that some of these parts of the skeleton may have become severed before the specimen was covered up in the deposit, Mr. Gardner having used all possible efforts to discover the missing remains. The neural arches appear to have been united to the centrums; and several vertebræ were
On the Upper Limit of the essentially Marine Beds of the Carboniferous Group of the British Isles and adjoining Continental Districts; with Suggestions for a fresh Classification of the Carboniferous Series
Authors: Hull Edward
Published: October 2009

Introductory
.—It is only recently that the materials have been obtained for a complete comparison between the different members of the Carboniferous group as they occur in Ireland and Great Britain. Much misconception has, for example, prevailed in some quarters regarding the true position in the series of those beds which, in the south of Ireland, immediately overlie the Carboniferous Limestone; and by some means or other, which I have not fully been able to ascertain, the term “Coal-measures” has come to be applied to all the beds from the top of the Limestone up to the coal-bearing measures of the Leinster Coal-field and of the corresponding beds of Kerry, Limerick, and Clare. The consequence is that it has sometimes been supposed that the coal-bearing districts of the south of Ireland are much more extensive than is actually the case. As far as the maps of the Geological Survey are concerned, we are now taking steps to give to the public a truer idea of the actual limits of the coal-bearing strata, and also to correlate with the British series the strata between them and the Limestone. Mr. Hardman has nearly completed a resurvey of the coal-districts of Carlow, Kilkenny, and Tipperary, resulting in a more accurate and detailed representation of the different divisions; and I hope a similar revision will ultimately be extended to that large area in the south-west occupied by similar beds, with very little true Coal-measures at all, but which has been described only rccently as “one
Glacial Drift in the North-eastern Carpathians
Authors: Jack R. L. , Horne John
Published: October 2009

A. General Introduction.

W
hile
most of the European ranges have been subjected to detailed investigations with the view of determining the existence and sequence of glacial deposits, the Carpathian chain has hitherto escaped any minute examination. Enough has already been accomplished through the labours of continental observers to justify an attempt to correlate the deposits occurring in other countries with their representatives in Britain. From the data already obtained it is obvious that, even in widely separated areas, the physical changes which transpired during the Glacial epoch must have borne a strong resemblance to each other. In the north of Europe there is the clearest evidence for the former extension of the ice; and even south of the limits of the northern drift the observations already made point to the same conclusion. They prove that, in regions where snow-fields no longer exist, glaciers must have filled the valleys, leaving behind them moraines and erratic blocks as memorials of their presence; while in those countries where glaciers still hold sway the hills and valleys must have been covered with ice, which ground and polished the slopes and accumulated underneath a mantle of stony clay. But on adverting to the evidence regarding the former prevalence of arctic and boreal conditions, it would appear that there is a general uniformity in the succession of deposits belonging to different countries. Not only in Britain, but in Scandinavia and Switzerland, we find deposits of sand, gravel, and lignite containing Mammalian remains and traces of Man, intercalated in the
On the Vertebral Column and Pelvic Bones of Pliosaurus Evansi (Seeley), from the Oxford Clay of St. Neotts, in the Woodwardian Museum of the University of Cambridge
Authors: Seeley Harry Govier
Published: October 2009

Knowing how many Plesiosaurian genera have left their remains in the great Pelolithic system formed by the Oxford Clay, Ampthill Clay, and Kimmeridge Clay, and that triangular teeth have not been obtained from the Oxford Clay of St. Neotts, some amount of indecision may be justifiable in the generic determination of this species. Nevertheless the cervical and dorsal vertebræ closely resemble in typical characters those of Pliosaurs from the Kimmeridge Clay; and I do not detect in them or in the pelvic bones indications of approximation to the known characters of any other genus.

The remains are from the well-known pit in the lower part of the Oxford Clay at Eynsbury, near St. Neotts, which yields
Ammonites Duncani, A. Lamberti, A. coronatus, &c
. They comprise thirty-seven vertebræ in sequence, of which twenty are cervical and about sixteen dorsal; and there is one pubic bone and one ischium. But the vertebral bones were obtained at a former period, and the pelvic bones after an interval of some years. We owe the discovery and preservation of these fossils to J. J. Evans, Esq., of St. Neotts, who presented them to the University of Cambridge; and it is in honour of the discoverer that I propose the species should be named.

The Atlas and Avis (figs. 1, 2).

These vertebræ though in close contact, do not appear to have been ankylosed together. They have lost their neural arches, like all other Pliosaurian vertebrae. A large subvertebral wedge-bone beneath the atlas (
c
) projects for
On an hitherto unnoticed Circumstances affecting the Piling-up of Volcanic Cones
Authors: Mallet Robert
Published: October 2009

B
esides
the two great groups of conditions which mainly determine the general form and shaping-out of volcanic cones, many secondary forces concur in greater or less degree in the production of the varied and often complicated phenomena which constantly or occasionally are observable in or around these cones. Some of these forces are mechanical, others physical or molecular, acting separately or, more often, in combination. It is not my intention here to enter upon any systematic discussion of the play of these varied forces, which, it may be remarked, have never yet been submitted to a careful and systematic analysis by the mechanical and physical philosopher, and which remain amply to reward competent labour, when bestowed upon them, but which can only be adequately treated at a length and in such detail, descriptive and analytic, as must extend to a volume, or at least to a succession of memoirs.

My present purpose is merely to notice prominently one circumstance, very commonly belonging to the piling-up of volcanic cones, which, so far as my knowledge extends, has entirely escaped hitherto the observation of vulcanists, but which, nevertheless, must often exercise important influences upon the exterior form and internal structure of volcanic cones, especially at and about their lower portions, and may even occasionally affect surrounding strata, entirely outside the circuit of the base of the cone. Volcanic cones as found upon our globe, when largely viewed are little else than “cinder-tips,” aggregated of the loose material blown out in a heated
Note on some Recent Discoveries of Copper-ore in Nova Scotia
Authors: Gilpin Edwin
Published: October 2009

A
lthough
for many years the presence of various ores of copper was known in this province, it is but recently that discoveries have been made of economic value.

In the early French expeditions to Canada and Acadie (now Nova Scotia) were men similar to those styled by Sir Humphrey Gilbert “rare refiners of miners;” and their reports on the supposed mineral wealth of Nova Scotia and Cape Breton excited much interest in Paris, and formed one of the reasons that France struggled so strongly to retain her supremacy in British America.

Lescharbot, writing in 1609, speaks of the native copper of the Bay of Fundy as being “very pure in the stone,” and adds, “many goldsmiths have seen it in France, which do say that under the copper-mine there might be a golden mine, which is very probable.”

The stone he alludes to is the trap associated with the Triassic sandstones of the Bay of Fundy; copper is found scattered through it in small grains and lumps, but has not yet been found in workable quantity. Although this trap resembles that from the famous Lake-Superior copper-district, the zeolites and other minerals characteristic of the Nova-Scotia trap are wanting in the Lake-Superior trap; and on no ground, so far I am aware, can any equivalence of age be established.

Passing over without notice the numerous unsuccessful attempts that have been made to open productive copper-mines in Upper and Lower Carboniferous strata, we find that the eastern part of the province gives
The Precarboniferous Rocks of Charnwood Forest.—Part I.
Authors: Hill E. , Bonney T. G.
Published: October 2009

Introduction and General Description.

C
harnwood Forest
, as is well known, is a hilly district composed of a number of rather parallel ridges with a general trend from N.W. to S.E. These hills rise to a height of a few hundred feet above an undulating plain of Mesozoic rocks, which on the eastern side is interrupted by the wide valley of the Soar. They consist of rocks most of which are more or less metamorphic; but some are igneous; isolated bosses also crop up here and there from the surrounding Trias. This deposit runs, as it were, in fjords into the recesses of the older rocks, besides dividing the district by a kind of strait or sound. To the S.W. and S. the Trias stretches far away; but on the W. (not, however, much modifying the configuration of the district) lies the Leicestershire Coal-field. A boss of hornblendic granite, Mountsorrel, crops up at the western edge of the Soar Valley; and three or four masses of a somewhat similar rock occur at a greater distance to the south. These most likely are all outliers of the highland region of the forest, which is really the culminating point of an old mountain-land. This was probably to some extent defined before the Carboniferous epoch, and formed a scattered group of hilly islands in the Triassic waters.

The district has been investigated by Professor Sedgwick, Professor Jukes, Professor Ansted, the Rev. W. H. Coleman, and several others. An exhaustive list of the papers upon
Note on a Specimen of Diploxylon from the Coal-formation of Nova Scotia
Authors: Dawson J. W.
Published: October 2009

I
n
a recent visit to the South Joggins, with the view of further studying the fossils of that district, and more especially of searching for reptilian remains in any erect stumps of
Sigillaria
that might have been exposed by the action of the waves, I was zealously aided by my friend Mr. Albert J. Hill, Manager of the Cumberland Mine, who, after my departure, determined to take down some erect trees occurring in beds lower in the section than those containing the reptilian remains. In pursuing this investigation he discovered an erect tree twelve feet in height, having the whole of its woody axis perfectly preserved,
in situ
, and showing structure. As this appears to me to be important with reference to questions now in discussion, I beg to present to the Society Mr. Hill's description of the specimen and some remarks on its structure and affinities.

Mr. Hill thus describes the mode of occurrence of the specimen:—“The tree in question stood partially exposed near the top of a perpendicular cliff, one hundred and twelve feet above the beach (fig. 1). The means of reaching and successfully extracting it from the massive sandstone stratum in which it was still half imbedded, was a problem of no easy solution. The difficulty, however, was overcome by an adventurous workman, who undertook, by means of a ladder attached by a rope to a small tree upon the surface, to descend to a sloping ledge formed by the jutting-out of a coal-seam and super-incumbent
The Steppes of Southern Russia
Authors: Belt Thomas
Published: October 2009

I
first
saw the steppes of Southern Russia in the spring of 1873, and under circumstances calculated to impress some of their peculiar features on my mind. I had, in company with a friend, crossed the Caucasus from Tints to Vladikafkas. We had travelled by the great military road through the pass of Dariel, and down the stupendously precipitous valley of the Terek. At Vladikafkas we came out on a vast plain, sensibly level as far as the horizon, and running in between and around the spurs of the mountains, like the sea around the headlands of a precipitous coast. I have since then travelled for thousands of miles over similar plains in Asiatic and European Russia; but the vividness of my first impressions of the steppe of Vladikafkas has not been dimmed, although my interest in the great plains has been increased by the personal experience I have since gained of their almost continental extent.

At Vladikafkas I saw no sections to a greater depth than 15 feet. These showed the upper surface of the plain to be composed of about 4 feet of black soil, resting on a fine grey loess-like clay, the base of which was not seen. I was only able to make a short search, and found no organic remains.

In 1875, and again in 1876, I travelled much in Southern Russia; and I propose to lay before the Society the information I have obtained respecting the extent, the constitution, the geological age, and the
On Terminal Curvature in the South-western Counties
Authors: Ussher W. A. E.
Published: October 2009

M
ore
than two years ago my attention was drawn to this subject by the perusal of a paper by Mr. Mackintosh in vol. xxiii. of the ‘Quarterly Journal.’ Having in the interim neglected no opportunity of studying the phenomena in question over a large area, I arrived at conclusions adverse to those advocated by Mr. Mackintosh; so that the object of this paper is twofold :—first, to controvert Mr. Mackintosh's opinions; secondly, to put forward more tenable explanations. To carry out this object thoroughly is impossible without considering the Pleistocene history of Devon, &c., in some at least of its aspects; but as the wider subject is reserved for a future communication, I shall here only touch on it as briefly as possible.

P
art
I.

Mr. Mackintosh suggests four explanations of the instances of terminal curvature described in his paper*. They are as follows :—

1st. “Land-ice filling up the basin of the Bristol Channel” and travelling southward.

2nd. Floating ice, in bergs or in “any other form.”

3rd. “A swift oceanic current exerting a pressure on the underlying slates by means of a forcible drifting forward of detritus.”

4th. “A still more violent rush of waters caused by a sudden upheaval or depression of the land.”

The first of these alternative solutions finds most favour with their author. I do not deny its applicability to some instances of terminal curvature within three or four feet of the surface in glaciated districts; but in the South-western Counties, where evidence of
On Points of Similarity between Zeolitic and Siliceous Incrustations of recent Formation by Thermal Springs, and those observed in Amygdaloids and other altered Volcanic Rocks
Authors: Daubrée A.
Published: October 2009

The production of zeolitic minerals by the agency of thermal waters is not, as might at first sight have been supposed, a merely accidental circumstance confined to a particular locality, but appears to be tolerably general in many places—and is therefore of particular interest, not merely as illustrating the changes that have gone on at the springs themselves, but as furnishing a clue to the origin of many of the components of erupted rocks, and more especially of altered volcanic rocks.

I.
Zeolites and allied minerals produced by Thermal Springs
.

The locality where these minerals were first observed as deposits from hot springs is Plombières* (Vosges); and subsequently I have discovered them under similar conditions in Roman masonry at Luxeuil† (Haute-Saône), at Bourbonne (Haute-Marne), and in the neighbourhood of 0ran in Algeria. At all these places the mouths of the thermal springs, when first utilized for baths during the Roman occupation, were surrounded by works in concrete formed of fragments of brick and stone, both sandstone and limestone, united by lime mortar. When, in the progress of recent works, it became necessary to cut into these masses of ancient masonry, it has been found that certain portions of them have, under the action of the mineral-water, undergone changes of a very remarkable kind, both in a chemical and mineralogical point of view, and of the following character‡.

In the vesicular cavities of the bricks new minerals are prominently developed, being principally zeolites, among the most abundant of which is chabasite
Additional Notes on the Dimetian and Pebidian Rocks of Pembrokeshire
Authors: Hicks Henry
Published: October 2009

Conclusions

We are now, I think, in a position to attempt an inquiry into the probable physical conditions, locally at least, of these Pre-Cambrian epochs.

In the oldest formation, the Dimetian, we have not, unfortunately, at St. David's, a base to start from, since in no case probably have we reached the lowest beds. There are no true conglomerates in the whole series; and of the lowest beds, or those which seem to form the centre of an anticlinal, we are not sure whether they may not even be intrusive. The next beds in this group are a great series of altered quartz rocks and very fine-grained quartzites; but with these are associated a few of the ashy-looking bands mentioned as either intrusive along the bedding or contemporaneous basaltic flows. These beds alternate with one another, and hence appear as if contemporaneous. The prevalence of volcanic action at this time is therefore rendered more than probable. Still the enormous preponderance of quartz rocks throughout the whole formation, and the absence of ashy beds and of felstone lavas and volcanic breccias of any great importance, indicate to my mind that it was probably chiefly detrital in its origin, the result of the wearing-down of previously existing rocks. Whether this formation is chiefly made up of detrital or volcanic materials, however, is a question chiefly for the chemist and mineralogist.

The question which to us is now of importance is that of its position geologicaily ; and upon this point I venture
Appendix on the Microscopic Structure of some Dimetian and Pebidian Rocks of Pembrokeshire
Authors: Davies Thomas
Published: October 2009

D
imetian.

1. The rock from near the Church School is seen macroscopically to consist largely of quartz in individual crystalline grains, or in groups, thickly distributed through a porphyritic-felsite ground-mass. In fissures and nests in the mass of the rock much chlorite and also some epidote are present. Its affinity to the quartz porphyries is only apparent when examined in thin section under the microscope. Here the quartz is seen to be distinctly crystallized, with characteristically rounded edges, and also with inclusions of the ground-mass. The felspar crystals are numerous, and much altered though the indications of banding of a plagioclase felspar are not wanting.

The ground-mass is microcrystalline throughout, consisting of quite individualized grains of quartz and felspar, and in many parts presents a peculiar structure. Around the quartz and felspar crystals an incipient spherulitic arrangement has taken place, resembling to some extent that seen in some rhyolites ; but here the radial texture is modified by a tendency to a dendritic or a branched structure, a peripheral outline being in all cases absent. This structure is also developed from numerous individual centres in the ground-mass, having no apparent nucleus ; it bears no resemblance to the rhyolite of the breccia before described, though it is probably but a modified form of spherulitic structure. Much grer chlorite and a black indefinable substance is dispersed through the ground-mass.

2. This fine-grained, chlorite-spotted rock presents in thin section a completely crystalline ground-mass of felspar and quartz grains, the latter being but
On the Building-up of the White Sinter Terraces of Roto-Màhànà
Authors: Abbay R.
Published: October 2009

I
t
is proposed in this paper to describe certain peculiarities in the structure of the “White Terrace” of Roto-Màhànà, in the Northern Island of New Zealand, which appeared to the writer, when visiting the spot in 1875, to be of considerable interest, as affording an explanation of the manner in which this most remarkable sinter formation has been built up. The geyser which has deposited the silica of which the terrace is formed, is situated on the side of a little hill of rotten rhyolitic rock, at an elevation of about 100 ft. above the warm lake (Roto-Màhànà) into which the foot of the terrace projects. The rim of the geyser is between 300 and 400 ft. in circumference; and the banks that surround it are steep on all sides except where the water finds an exit. Opposite this opening the wall of earth is almost perpendicular, and some 50 ft. in height. The geyser-basin is about 15 ft. deep, with a flat rim from 4 to 6 ft. broad, the whole being composed of a beautifully white flocculent-like deposit of silica, that yields slightly, like frozen snow, to the foot. The pipe is about 8 ft. in diameter, and is situated slightly on the exit side of the basin. A little rocky island, that will be referred to later, lies in the opening by which the water makes its escape, at about one third of the distance across it from the northern bank.

It probably owes its existence to
The Precarboniferous Rocks of Charnwood Forest.—Part II
Authors: Hill E. , Bonney T. G.
Published: October 2009

The Microscopic Structure of the Charnwood Rocks.

In many cases the task of determining the nature and structure of these rocks is comparatively easy; but in others it presents great difficulties. These arise from the amount of metamorphism which the rocks have undergone since they were first deposited. This metamorphism may be said to be of a double nature :—the one, readily apprehended by the eye, that which has converted sandstone into quartzite, and fine felspathic detritus into something resembling a felspathic igneous rock, being in all probability the combined effect of pressure, heat, and water; the other, almost wholly revealed by the microscope, in which the last of the above-named agents of change has probably been the most active, and which may still be in progress—namely, the gradual decomposition of the minerals which once composed the rocks, and the formation of new ones by fresh combinations of the chemical elements thus set free. This process often obscures, far more than the former, the original structure of the rock; and it is this accordingly which causes our main difficulty in the study of these Charnwood rocks.

To investigate microscopically all the varieties of stratified rocks found in the Forest would be a most laborious task; and in all probability the result would not compensate for the labour. We have therefore selected a series of specimens which appeared either typical of the more important varieties, or likely to be useful in illustrating some point of structure or stratigraphy. Forty-four slides in
Description of a new Fish from the Lower Chalk of Dover
Authors: Newton E. T.
Published: October 2009

I
n
a former communication to this Society* I described certain specimens of fish-remains from the Cretaceous rocks of Britain which I believe to be the English representatives of
Portheus
and
Ichthyodectes
. In the present paper I have described another Cretaceous fish, belonging, as I think, to
Daptinus
, a third American genus not hitherto recognized in this country.

The specimen, which is imbedded in a block of Grey Chalk, was obtained from Dover by Mr. J. S. Gardner, and is now in the British Museum (no. 47250). It has been admirably developed under the careful superintendence of my esteemed friend Mr. W. Davies, to whom I am much indebted, as also to Dr. H. Woodward, for the facilities afforded me for the examination of this fossil. It consists of a skull with the facial and opercular bones of the left side almost perfect, and retaining very nearly their natural relations to each other. The surfaces of the bones are mostly abraded; but where they remain apparently intact, they exhibit no kind of ornamentation, except the radiating lines indicative of the direction of growth, which are commonly to be met with on teleostean fish-bones. In a side view (fig. 1) four vertebræ are to be seen; but probably two others intervene between the anterior of these and the skull, and most likely two more are overlain by the bone marked
pt.tem
.

The teeth have long, hollow roots, sunk in deep sockets, and were replaced vertically—characters which are displayed by a fortuitous fracture
The Submarine Forest at the Alt Mouth
Authors: Reade T. Mellard
Published: October 2009

O
n
the shore at Great Crosby, Lancashire, stretching, at irregular intervals, for a space of about a mile nearly due north from a stream of water called Thornbeck Pool, are the remains of a forest, which have from time to time attracted considerable attention. It has been described by various observers, the earliest mention I know of being in the ‘Gentleman's Magazine’ for 1796, p. 549, accompanied by an engraving, giving all the salient points which still distinguish the forest-bed. A view of these submarine forestal remains also forms the frontispiece of the memoir by Mr. C. E. De Rance on the “Superficial Geology of West Lancashire,” lately published by the Geological Survey. I have also described it in my paper on the Postglacial Geology of Lancashire and Cheshire*.

As it has been pretty roundly asserted by some local observers that neither these trees nor those of the equivalent bed on the Cheshire shore are
in situ
, though I had no doubts of the fact myself, to set the question at rest I invited several gentlemen†, most of them members of the Liverpool Geological Society, to be present on the 19th of January, 1878, at the digging-out and uprooting of one of the stools of the trees, which are now rapidly diminishing in number by the denudation of the sea.

A low stump was selected which had an oak trunk lying by it in a N.E. by E. direction, to all appearances in the position in which it had rotted
On the so-called “Greenstones” of Central and Eastern Cornwall
Authors: Phillips J. Arthur
Published: October 2009

Conclusion

In addition to the rocks which occur in Western Cornwall, some of the areas forming the subject of the present paper afford numerous examples of ancient lava-flows so interbedded with the slates and schists of the district as to lead irresistibly to the conclusion that they are contemporaneous igneous products.

These lavas, notwithstanding the alteration to which they have been subjected, closely resemble those of more modern date, and contain cavities which are now filled either with a mixture of viridite and calcite or with quartz through which vermicular chlorite is distributed. They sometimes assume a distinctly schistose structure, and contain crystals of a sanidine-like felspar, many of which are broken, while others have become sphærulitic, through a rearrangement of their constituents.

The crystalline greenstones of Central and Eastern Cornwall afford a more varied and instructive series than is furnished by those of the western portion of the county. Among them are typical dolerites on the one hand, as at South Petherwin, while on the other there are rocks which, as at Carkeel, are so altered as to consist only of a granular indefinite material traversed by indistinct microlitic bodies, and, in patches, stained brown by oxide of iron.

The pyroxenic constituent of these rocks, wherever its crystals admit of identification, is augite ; and they are consequently dolerites. By many petrographers they will doubtless be classed either as
diabases or melaphyres
; but when it is remembered that they differ from modern dolerites only in age, and by reason
On some Tin Stockworks in Cornwall
Authors: Foster C. Le Neve
Published: October 2009

T
he
name
Stockwork
is usually applied to large masses of rock impregnated with metallic ores or intersected by a number of mineral veins at short distances apart, sometimes crossing one another in all directions. Not having any word of our own, we have adopted the term Stockwork from the German
Stockwerk
. This expression probably owes its origin to the method of working formerly often adopted for such deposits, which were wrought by chambers arranged in
tiers
or
stories
.

The tin Stockworks of Cornwall may be divided into three classes, according as they are found in clay-slate (killas), granite, or elvan. I propose giving a short account of four of them which have never been thoroughly described.

Wheal Prosper and Michell
.—These are open workings about half a mile west of Lanivet church, near Bodmin. For a distance of upwards of 800 yards and a width of 30 yards the killas is intersected by numerous little tin-veins running E. 7° N. (true); the pit is usually 60 or 70 feet wide in the bottom, but in one part, where a series of N. and S. branches go across, the width is double that amount. In addition to the E. and W. and N. and S. strings, there are occasional
caunters
which are likewise stanniferons.

The killas is usually very soft and generally light-coloured, i. e. grey or white, or stained a yellowish brown by oxide of iron. In some places near the veins the killas is converted into a soft tourmaline-schist. The
The Secondary Rocks of Scotland. Third Paper. The Strata of the Western Coast and Islands
Authors: Judd John W.
Published: October 2009

C
onclusion
.

Although, as I have before stated, it has been thought advisable to postpone the discussion of the numerous problems of interest which suggest themselves to the student of the remarkable relics of the Secondary rocks in the Scottish Highlands, until the fourth and concluding portion of this memoir is published—yet there are several questions which at the present time engage the minds of geologists upon which, as it appears to me, the facts and arguments of the present part of this memoir have an important bearing; and these it may not be undesirable to notice briefly at the present stage of the inquiry. Other and more general discussions will be allowed to stand over till such time as I have made the proposed comparison between the characters and modes of preservation of the beds under consideration and those of their equivalents in Ireland, England, Scandinavia, and other portions of the Continent.

I may briefly point out in the first place the great interest which attaches to the fact that there exists in the north-western part of the British archipelago a series of strata of Cretaceous age exhibiting evidence of the prevalence of estuarine alternating with marine conditions. The great and deserved amount of attention which is now directed to the similar beds, developed on such a grand scale in Western America, renders the discovery of the minute Scottish representatives of the period particularly important at the present time. It is tantalizing, however, to the British geologist to have to
On an Unconformable Break at the Base of the Cambrian Rocks near Llanberris
Authors: Maw George
Published: October 2009

T
he
short paper which I have to lay before the Society has been suggested by several previous communications on the subject of rocks older than, and unconformable to, the Cambrian Slates of North Wales.

In the year 1867 I brought before the British Association at the Dundee meeting the accompanying section on the Llanberris and Carnarvon Railway, then for the first time exposed in a new cutting near Llanberris. The section was subsequently published in the ‘Geological Magazine’ for March 1868, to which I must refer the reader.

Up to this time no suspicion existed of the occurrence of an unconformable series of ancient rocks in North Wales older than the Cambrians.

Previous to this the researches of Dr. Hicks in Pembrokeshire established in that district the fact of the occurrence of great series of beds unconformable to the overlying Cambrians; but during the succeeding seven or eight years no fresh observations were made in the Llanberris district.

At the reading of Dr. Hicks's paper on December 2, 1874, I pointed out an apparent analogy between the Pembrokeshire series and that at Llanberris; and this, I believe, induced Professor Hughes and Dr. Hicks to visit Llanberris, and their observations on that district were recently communicated to the Society (Q. J. G. S. vol. xxxiv. pp. 137 & 147).

Rather singularly, they disagree with me in the conclusion 1 arrived at, that there was a visible break in the series of rocks exposed in the Llanberris railway-cutting, but admit that such
On a Section through Glazebrook Moss, Lancashire
Authors: Reade T. Mellard
Published: October 2009

T
he
Wigan Junction Railway now being constructed runs, for the length of a mile, through Glazebrook Moss. Walking from Glazebrook Station, on the Cheshire Lines Railway, towards Kenyon Junction, on the old Liverpool and Manchester Railway, we come, in about half a mile, upon the edge of the Moss, and here the Wigan Junction Railway goes through it in a cutting. In the deepest part the moss is about 18 feet from the actual surface to the boulder-clay on which it rests; but the drainage produced by the cutting has caused the moss to sink from 7 to 8 feet on either side in its vicinity.

The bulk of the moss is of the ordinary nature, and looks, on drying, more like sawdust than any thing else. Near the base, for 3 or 4 feet upwards, are the remains of trees—branches imbedded in the peat. Where the peat has been excavated down to the boulder-clay the stools of trees, in the position they had grown in, are now to be seen ; they are, with one exception, so far as I saw, either oak or birch; and the whole of the peat being removed from about them shows very plainly the roots penetrating into the clay. The upper layer of clay is of a grey colour, and is evidently the top-wash of the boulder-clay. A splendid prostrate trunk of an oak was bared when I viewed the cutting; it measured 46 feet long as far as exposed, and was fully
The Recession of the Falls of St. Anthony
Authors: Winchell N. H.
Published: October 2009

I
n
studying the superficial accumulations of the North-west, the phenomena of the drift in the vicinity of the Falls of St. Anthony have come under review, and it has been found that the intimate connexion between the history of that drift and the recession of the Falls has afforded another datum from which to compute the date of the last cold phase of the glacial epoch. The consideration of this question naturally divides itself into three parts:—

First
. The Drift in the vicinity of the Falls of St. Anthony.

Second
. The Gorge formed by the recession of the Falls.

Third
. The Recession of the Falls.
Notes on the Palæontology and some of the Physical Conditions of the Meux-Well Deposits
Authors: Moore Charles
Published: October 2009

T
he
various deep borings which have been put down at Crossness, Harwich, Kentish Town, and more recently at Meux's Brewery, in the Tottenham Court Road, have amply established the correctness of Mr. Godwin-Austen's deductions that a ridge of Palæozoic rocks passes under the Jurassic and Cretaceous beds of the south-east of England, the probability, if not the certainty, being that the rocks of which that ridge is formed are a continuation of those which skirt the South-Wales coal-basin, and which, in passing through Somersetshire, are continued in the Mendip range until lost under Secondary deposits near Frome.

In the above districts I have previously pointed out that the representatives of some of the Secondary beds are found associated with the older rocks, under very peculiar conditions, through a line of country from east to west of about sixty miles. At one spot thin deposits or pockets of Inferior Oolite may be seen lying unconformably upon the highly inclined but planed down edges of the Carboniferous Limestone; at another, conglomerates of Liassic or Rhætic age of a few feet in thickness, some of them exhibiting shore-conditions, may be found filling depressions in the limestone or passing down its vein-fissures; and however thin these deposits may be, they can be recognized as distinct, and as representing on the sides or otherwise of the southern portion of the Palæozoic anticlinal the presence in the district of Rhætic, Liassic, and Oolitic formations.

Perhaps the most interesting evidence of these peculiar physical conditions is seen
On ,
Pelanechinus
, a new Genus of Sea-urchins from the Coral Rag
Authors: Keeping Walter
Published: October 2009

T
his
is a Sea-urchin of more than ordinary interest, and remarkable for possessing an unusually developed system of overlapping plates around the mouth-opening. Such a structure is now well known in the deep-sea
Asthenosoma
(or
Calveria
), where it has been compared to the whole tests of some flexible Echini from the older (Palæozoic) rocks. I believe that the whole test of this Urchin also was flexible, though not nearly to the same astonishing degree as in
Asthenosoma
.

Dr. Wright, in 1855, described this species from very fragmentary portions under the name
Hemipedina corallna
; but since that date the more perfect specimens described below have been found, and the characters seen in these demand their wide separation from
Hemipedina
, and establish a new genus whose affinities are rather with the
Echinothuridæ
.

I have only two specimens to work at, not being able to find those mentioned by Dr. Wright on page 164 of his Monograph (Pal. Soc.). Both of these are, however, very good. One was found by my father at Calne in 1866, and is now in the Woodwardian Museum, Cambridge; the other, from the same locality, is in the cabinet of Dr. Wright. They have been kindly lent to me for description.
On
Rhamphocephalus Prestwichi
, Seeley, an Ornithosaurian from the Stonesfield Slate of Kineton
Authors: Seeley H. G.
Published: October 2009

Prof. Prestwich as obtained from the Stonesfield slate of Kineton, near Stow-on-the-Wold, a small slab which makes a valuable contribution to our knowledge of the structure of the skull in Ornithosaurs from the British Lower Secondary rocks. This specimen is little more than a cast from the upper surface of the cranium, not unlike in general character to the form originally described by Goldfuss as
Ornithocephalus Münsteri
. The skull itself was unfortunately in the corresponding slab, which has not been preserved; but a few slight fragments of bone remain sufficient to show the dense osseous tissue which is usual in Pterodactyles. The specimen yields a clear impression, which displays the proportions of the cranial bones, and the sutures between them, in a way so distinct as to enable me to state that this animal was certainly different generically from every other type which has hitherto been described. Whether, however, it pertained to a distinct species from those indicated by the fossils from Stonesfield which have already been figured by Professors Huxley and Owen is a matter upon which some doubt may be felt; but bearing in mind the relatively large size of the jaws and teeth in those fossils, I am strongly of opinion that this specimen indicates a smaller kind of animal, in which the dentary apparatus was less developed, and I therefore venture to suggest for it a specific name.

The remarkable feature which leads me to consider this specimen to be the type of a new genus