bluuebunny/crossref_metadata_2025_split huggingface dataset:
Note on the Animal Remains
Authors: Davies W. 
Published: October 2009

The animal remains found in both caves comprise teeth and bones of 11 genera and 16 species, as shown by the annexed list:―
If the animals here enumerated, three are extinct, viz. the Irish Deer, Woolly Rhinoceros, and the Mammoth. The Spelæan Lion and Hyæna were considered by Goldfuss and the older naturalists to be also extinct species; but later investigations show that their remains are undistinguishable from bones and teeth of the existing Lion and the Spotted Hyæna respectively. Other species now extinct in Britain are the Wolf, Bear, Wild Boar, and Reindeer, also the Wild Ox or Bison.
With regard to numbers, the teeth and bones of the Horse, Rhinoceros, Hyæna, and Reindeer are respectively the most numerous in the order here presented. That the Hyænas for a long period had entire possession of the caves is proved by the paucity of the remains of the Bear, another cave-haunting animal, thus showing that there had been no joint or alternate occupation by these animals as in some recorded instances.
The state of preservation of the bones, apart from the imbedding matrix, resembles that of similar remains from other caves in limestone rocks, and inhabited by Hyeenas. Few are entire ; many of the limb-bones have their softer ends gnawed away, leaving the hard and denser bone of the shafts still bearing the marks of teeth. Others appear to have been fractured both longitudinally and transversely by some force when the bone was fresh, as if for the extraction of the marrow; and, again, a few crushed specimens, by
On some Borings in Kent: a Contribution to the Deep-seated Geology of the London Basin
Authors: Whitaker William 
Published: October 2009

It will be of interest therefore to give a full account of these borings, of which only short notices have yet appeared, and to review the bearing that the result of the later one has on our knowledge of the underground formations of the London Basin.
The borings are about 210 yards westward of the Factory Basin, in what was, until the extension of the docks was made, the marsh on the southern side of the former St. Mary's Creek, that creek having also been included in the new dockyard. The surface of the ground is about ten feet above Ordnance Datum.
The earlier boring, which reached Lower Greensand at a depth of over 903 feet, being of small size, in the lower part at all events, it was resolved to put down another and larger one near by, in order to get a large amount of water from the Lower Greensand; and it is to the second boring that this paper chiefly refers, because of the unforseen result.
One would have thought that Chatham was favourably placed for getting a large suply of water from the Lower Greensand, which formation has a broad outcrop only a few miles to the south. It was therefore with some surprise that one heard that, after passing through only 41 feet of sandy beds (below the Gault), a mass of clay was reached at the depth of 943 feet.
At first this clay was naturally taken to be either a very clayey development
Note on some recent Openings in the Liassic and Oolitic Rocks of Fawler in Oxfordshire, and on the Arrangement of those Rocks near Charlbury
Authors: Bather F. A. 
Published: October 2009

This account was written to bring before the notice of practical geologists some new sections on the works of Messrs. Bolton and Partners, at lawler. The district treated of lies in quarter-sheet 45 S.W. of the Survey Map, and was described by Prof. Hull in his accompanying memoir, 1859, to which nothing was added by Prof. Green in his memoir, 1864. Accurate description rather than speculation has been aimed at; still, as some alteration seems necessary, its probable lines are suggested from personal examination of the neighbourhood. The Evenlode valley exposes Liassic rocks to about ¾ mile below Pawler, where Great Oolite is brought down by a fault. Since the locality is well known, I proceed to describe the sections in ascending order.
The cores of the boring were not preserved; they were, I am told, of the same character throughout. The line of junction of beds є and ζ is 14 ft. above the bed of the river.
Section B, in a coombe across the road N.E. of the brickyard, clearly marked on the map by a branching-off of the Lias and Inferior Oolite into the Great Oolite plateau. A deserted opening extends S.W. by N.E., along the north side of this coombe for nearly 200 yards. The strata here are so variable in thickness that no definite section can be given. The lowest is marlstone rock-bed δ, varying from 8 to 10 ft., but in one part so displaced that it appears in vertical section 12 ft. thick.
On a recent Section through Walton Common exposing the London Clay, Bagshot Beds, and Plateau-gravel
Authors: Hudleston W. H. 
Published: October 2009

During the past autumn the London and South-Western Railway Company has been engaged in widening the line between Walton and Weybridge stations, and consequently there has been an excellent exposure of the beds composing the Walton-Oatlands plateau. The communication now made to the Society relates only to such portion of the railway-cutting as extends from Walton station in a west-south-west direction to the boundary of Oatlands Park, and more particularly to that portion of it known as “America.” The total length, as measured on the 6-in. Ordnance map, is 1070 yards. This distance is divided unequally by the railway bridge on Walton Common known as “Sir Richard's.” The distance between Walton station and the centre of this bridge is 710 yards, whilst the distance from this point to the boundary of Oatlands Park is 360 yards, or thereabouts.

For the purposes of description and convenience of reference, the entire section may be divided into
four
blocks.

Block A extends from Walton station to where the unaltered London Clay in seen to occur
in situ
—a distance of 313 yards.

Block B extends from this to the point where the Bagshot Beds are first seen
in situ
—a distance of 345 yards.

Block C extends from the above to the point where the Bagshots are first cut through to the level of the line, and the hollow filled up with Plateau-gravel—a distance of 165 yards.
Block D exhibits the relations of the Bagshots to the Plateau-gravel, where the latter is most fully developed—a.
On the Pliocene of Maragha, Persia, and its Resemblance to that of Pikermi in Greece; on Fossil Elephant remains of Caucasia and Persia; and on the Results of a Monograph of the Fossil Elephants of Germany and Italy
Authors: Pohlig H. 
Published: October 2009

I. In 1884 I had the opportunity of making a geological tour in Persia, espeeially in the northern provinces, one of my principal objects being to excavate a deposit of Pliocene mammals discovered about 30 years ago by the Russian travellers Göbel and Khanikoff near Maragha, to the east of the lake of Urumia. Abich, Brandt, and Grewingk have already published short notes upon the subject, but the locality where these fossil bones were found has not been exactly specified.
Arrived at Maragha I found several deposits of fossil bones, and excavated them as long as the season permitted. The results obtained I first announced in two letters sent from Maragha to Prof. yon Lasaulx† and to Dr. Tietze‡, including a preliminary list of the Plioeene mammals of Maragha which had been obtained up to that time, and so far as I could determine them on the spot without means of comparison. The collections made by me in Persia are now mostly deposited in the Museum of Prof. yon Fritseh at Halle.
In the course of last year a young German residing in Persia successfully continued my excavations at Maragha, and it was a portion of the bones collected by him that M. Gaudry saw in the Museum at Vienna (see Geol. Mag. December 1885, p. 558).
As I am now engaged in preparing a monograph on the fossil mammals of Maragha, I wish in this paper to give a sketch of the deposits containing these remains and also a
On the Alteration of coarsely Spherulitic Rocks
Authors: Cole Grenville A. J. 
Published: October 2009

As has been previously stated, all the phenomena that accompany spherulitic structure on an ordinary scale appear reproduced among lavas that may be called coarsely spherulitic. Ill-defined segregations, differing little from the matrix, the fluidal and banded structures of the rock running indifferently through both, are found measuring an inch or two in diameter, equally with forms of marked radial or concentric character. The scale on which certain processes of decomposition and reconstruction, especially those that affect differently the spherulite and the matrix, are revealed in these bold examples, and the interest attaching to their effect upon the ultimate character of the mass, have led me to bring together a few observations on the alteration of coarsely spherulitic rocks. Some of the finest instances, moreover, may be found in our own British lava-flows of Palæozoic age, and with these the field-worker is not unfrequently called upon to deal.
The well-known black pitehstone of Planitz, near Zwickau in Saxony, which is of Permian sge, contains angular aggregates of calcite and chalcedony enclosed in large brown nodlfles. These remarkable occurrences were referred to by Cotta as early as 1849†, and his figure was copied by Delesse in a comprehensive paper on “Les Roches globuleuses”‡ Cotta considered the nodules surrounding the chalcedony as inclusions of an adjoining porphyry, like those in the pitehstone of Spechthausen ; but the microscope proves them to be in reality large brown spherulites, often 3 centims, in diameter, and differing only slightly from the glass. Why the agents of
On the Pliocene Beds of St. Erth
Authors: Kendall Percy F. , Bell Robert George 
Published: October 2009

In presenting this paper for the consideration of the Geological Society, we desire to state at the outset that it is intended only as a report upon reaching a stage in the investigation of this interesting deposit, and that any speculative remarks which we may venture to offer are intended rather as indicating certain directions to which inquiry may be turned with a prospect of useful result, than as well-matured conclusions to which we are prepared rigidly to adhere.
The materials at present available do not warrant us in taking a less guarded attitude, the list of fossils which we bring forward, though very large, being, we are convinced, capable of considerable increase by a more extended examination of the beds than we have hitherto been able to make.
The attention of the Society was first directed to the St. Erth deposits by a communication from the late Mr. S. V. Wood, which was read at an early meeting last session. That paper was considered by Mr. Wood to be of a tentative character, nothing very accurate being known of the physical conditions of the deposit, nor was there anything like a good knowledge of its contents, and it was his hope that the attention of competent geologists might be drawn to its occurrence, so that it might be worked out and surveyed in a better manner than, in his invalid condition, he was able to perform. Shortly afterwards Mr. Wood died, and by his desire the whole of the material
The Melbourn Rock and the Zone of
Belemnitella
plena from Cambridge to the Chiltern Hills
Authors: Hill W. , Jukes-Browne A. J. 
Published: October 2009

The Melbourn Rock was described by one of us in 1880 as a band of rocky chalk occurring in Cambridgeshire at a distance of about 80 feet above the Totternhoe Stone, and forming the base of a middle division of the chalk. Since then the outcrop of this rock has been traced south-westward through the counties of Hertford, Bedford, Buckingham, and Oxford, and has been found to be remarkably constant in its character and behaviour. It is generally found at the top of a well-marked feature or slope, and where it recedes into coombes, these are generally steep-sided; at the head of such valleys there are frequently powerful springs, which are thrown out by the marly beds at the base of the rock, so that it is of practical importance as a water-bearing stratum.
While one of us has been engaged in drawing this line of outcrop for the Geological Survey and in noting the exposures along its course, the other has carefully compared these sections, as they were discovered, with those previously described in Cambridgeshire, has collected such ibssils as were to be found, and has cut and examined under the microscope numerous slices from the different beds of rock and from the chalk below and above. In the present communication, therefore, we propose to offer the results of our combined observations on this rocky band and the beds associated with it ; and for permission to make use of the information gained during the official survey of the
On additional Evidence of the Occurrence of Glacial Conditions in the Palæozoic Era, and on the Geological Age of the Beds containing Plants of Mesozoic type in India and Australia
Authors: Blanford W. T. 
Published: October 2009

The two subjects mentioned in the title of this paper are accidentally connected, the evidence of contemporaneous origin in certain Indian and Australian beds that contain plants of Mesozoic types being strongly supported by peculiar physical characters believed to be due to the action of ice. The last number of the ‘Records of the Geological Survey of lndia,’ contains several contributions to the history of the question, and these appear to me to form an addition to our knowledge of general stratigraphical geology of importance sufficient to justify my calling the attention of the Society to them. The subject is one to which I have given much attention in past years, and which I have discussed at various times, and this will, I trust, serve to excuse my writing upon it, although I have no new observations of my own to produce.
The principal papers to which I wish to call attention are, first, one by Mr. Richard Oldham entitled “Memorandum on the Correlation of the Indian and Australian Coal-bearing Beds,” chiefly giving the results of a visit to Australia by a geologist who had had the advantage of seeing some of the Indian Gondwána beds; and, secondly, one by Dr. W. Waagen, with the title of “Note on some Palæozoic Fossils recently collected by Dr. H. Warth in the Olive Group of the Salt Rauge.” A paper by Mr. Griesbach on rocks near Herat, and a recent observation of Mr. E. Oldham's in Northern Rajputána, furnish some additional facts of value.
On a Mandible of
Machærodus
from the Forest-bed
Authors: Backhouse James 
Published: October 2009

About two months ago I obtained from the Forest-bed of Kessingland, Suffolk, a specimen which I take to be the right mandibular ramus of a species of
Machærodus
(Plate X.). As I believe that no example of the lower jaw of any species of this genus has been met with in this country, I venture to send the following description of it.

Length from posterior margin of condyle to upper edge of symphysis at insertion of second incisor 204 mm.
Vertical depth below premolar at shallowest part of ramus 38·25 mm.
Depth at middle of diastema 51 mm.
Depth at lowest point of symphysis 63·75. Originally the depth at this point has apparently been 70, if not 75 mm.
The diastema is large (41 mm.) and, like the portion of the ramus immediately beneath it, curved inwards; it presents a fossa of 6 or 7 mm., from the direct line between the canine and cheek-teeth, for the accommodation of the upper canine. The anterior foramen is large, and in a line parallel to the adjoining base of the ramus. The condyle is imperfect, the length of the remaining portion being 38·2 mm., and the vertical thickness 19·1 mm. The coronoid process has lost its upper third, the remaining portion being 25 mm. in height and 38 mm. in width at the base.
In regard to the teeth, the sectorial has an antero-posterior diameter of 32 mm.; it is much worn diagonally by the action of the corresponding upper tooth, and
On the Existence of a Submairine Triassic Outlier in the English Channel off the Lizard
Authors: Worth R. N. 
Published: October 2009

It is with great pleasure that I am able to report to the geological Society the existence of a submarine Triassic outlier in the English Channel, off the Lizard. The possibility of the presence of Triassic rocks in the Channel-area has been more than once suggested, and the occasional dredging of a fragment of sandstone has strengthened the hypothesis: no distinct evidence has, however, until now been procured.
A short time since Mr. Matthias Dunn, of Mevagissey, who is intimately acquainted with all the conditions of the Channel fishery, called my attention to the fact of the frequent occurrence of sandstone fragments in the bed of the Channel in a certain direction, and at my desire promised to supply me with a series of specimens. This he has now done, and the facts thus revealed are of a very remarkable character. All the examples were brought up entangled in the hooks of the fishermen's “long lines,” which are laid along the sea-bottom for distances ranging even up to six miles. The positions from which the rocks come can therefore be ascertained with considerable precision; and each specimen or group of specimens was accompanied by its compass-bearing on some well-known point of the land, and the distance thence in miles. The bearings are magnetic and strictly correct; the distances are estimated, and therefore liable to a certain amount of error; though from constant practice and their knowledge of the peculiarities of the sea-bottom the fishermen are singularly accurate in these estimates.
On the Glaciaton of South Lancashire, Cheshire, and the Welsh Border
Authors: Strahan Aubrey 
Published: October 2009

South Lancashire and Cheshire
.

The occurrence of glacial striæ in the neighbourhood of Liverpool was first recorded by Mr. G. H. Morton, F.G.S., in 1859, though they had been previously noticed by Mr. J. Cunningham, F.G.S. In 1862 Mr. Morton described before this Society and the Liverpool Geological Society striæ on both sides of the river Mersey. Prof. Hull in 1864 § recorded the strim of Bidston Hill, pointed out to him by Mr. Cunningham, remarking that they point in the same direction as those of Liverpool. These had been previously noticed by Mr. Morton as having the precise direction N. 30° W.
In consequence of his discovery of striee on both sides of, but at no great distance from, the Mersey, Mr. Morton in 1866∥ advocated the hypothesis of a glacier having descended the valley of the river; but in 1870 ¶ having discovered similar markings away from the river, adopted the theory of an ice-sheet having passed over this part of the country from S.E. to N.W.
In the same year Dr. Ricketts, F.G.S., recorded striæ at Thatto Heath, and stated that the moving power which produced them had taken a course from south-east to north-west, the evidence of this being that grooves larger and deeper than others passed away from small indentations, which may have been the impressions of pebbles, in a north-west direction.
In 1872 Mr. Mellard Reade, C.E., F.G.S., described cross striæ at Bootle, running E.N.E. and N. 22° W., and advocated the hypothesis of
The Bagshot Beds of the London Basin
Authors: Monckton H. W. , Herries R. S. 
Published: October 2009

The following communication is intended as a supplement to a paper read before the Society by one of the authors in 1883 (Quart. Journ. Geol. Soc. vol. xxxix. p. 348), and the two together form an amplification of an article on the same subject by Mr. W. H. Herrics (Geol. Mag. dec. ii. vol. viii. p. 171).
In our last paper we devoted our attention almost entirely to the Upper and Middle Divisions of the Bagshot series. We now propose to treat more fully of the Lower Division, and to show that the occurrence of pebble-beds is by no means confined to one horizon in the Bagshot series, as would seem to be supposed by some observers.
In the interval much has been written about the geology of the Bagshot district, no less than five papers by the Rev. A. Irving, and one by Mr. Hudleston, having appeared.
The views lately advanced by Mr. Irving are very much at variance with the hitherto accepted interpretation of the geology of this district, and to a great extent we find ourselves compelled to differ from him. He considers (Quart. Journ. Geol. Soc. vol. xli. pp. 506, 507) that the Upper and Middle Bagshot beds, in some places, overlap the Lower Bagshot Beds, and rest directly on the London Clay, which had been thrown into a slight syncline previous to the deposition of the Lower Bagshot strata. He founds his argument partly on the relative thicknesses of the Lower Bagshot beds and the
Volcanic Rocks of the North-east of Fife
Authors: Durham James 
Published: October 2009

Those who are acquainted with the more salient features of the geology of the great central valley of Scotland are aware that the broad band of Old Red Sandstone which extends from the base of the Grampians about twenty-five miles to the south-east is intersected by belts of volcanic rocks in lines, running from north-east to south-west, nearly coinciding with the strike of the beds. Of these volcanic belts by far the most extensive is that which forms the Fig. 1.
Sketch Map of the Country round Newport, Fife
southern boundary of the Lower Old Red Sandstone in this part of Scotland, and crosses the country almost uninterruptedly from sea to sea. It comprises some important ranges of hills, of which the Ochil range is the most conspicuous.

The north-east extremity of this great belt of volcanic rocks reaches the North Sea at the south side of the Firth of Tay, and forms, with certain interruptions, the southern shore of the estuary for some 18 or 20 miles; it here varies from five to ten miles in width, and on its south-eastern edge is in contact with the Upper Old Red and Carboniferous rocks. It seems probable that the line of contact is a line of fault.
As may be supposed, the long llne of shore in the Firth of Tay furnishes the most convenient section for studying the rocks which compose this igneous belt. Not only are such sections formed by the recent
Notes on the Relations of the Lincolnshire Carstone
Authors: Strahan Aubrey 
Published: October 2009

The Carstone of Lincolnshire lies immediately below the Red Chalk, and rests upon the fossiliferous clays and limestone known as the Tealby Beds. The Tealby Beds were described in detail for the first time in 1867 by Professor Judd; and their relations to the Speeton section, and to beds of the same age throughout Northern Europe, were discussed in 1870 by the same observer. In 1883 the survey of the district was completed, with the result of verifying in almost every particular the conclusions which had been so ably worked out by Professor Judd. On one point only I ventured to form a somewhat different opinion, namely on the relations of the Carstone to the Red Chalk above and to the Tealby Beds below.
The following table gives (in brief) the correlations advocated by Prof. Judd, and shows also the names of the various subdivisions which have been adopted for the Survey publications, and which will be used in this paper :—
The Carstone, which was doubtfully correlated with the Upper Neocomian of Speeton, was believed by Prof. Judd to be quite unconformably overlain by the Red Chalk. This theory of an unconformity, however, has not been confirmed by an examination of the numerous sections of the junction that are exposed. The overlap of the Carstone by the Red Chalk, which at first sight seems strongly to support Prof. Judd's view of their relations, appears to be due to the steady attenuation of the Carstone northwards that is shared by