bluuebunny/crossref_metadata_2025_split huggingface dataset:
Description of Parts of the Skeleton of an Anomodont Reptile (
Platypodosaurus robustus
, Ow.) from the Trias of Graaff Reinet, S. Africa
Authors: Owen  
Published: October 2009

I
n
a former paper† a dental character in a Triassic reptile was indicated which is repeated in some implacental members of the Mammalian class. I have also noticed a like correspondence in the skeleton of another reptile from the same formation in South Africa‡.

Pursuing the work of extricating from the matrix the Triassic fossils since received from that continent, indications still more interesting of such relationship have come to light, which I now proceed to submit to the Geological Society.
The evidence of the genus and species of extinct reptile above named, forming the subject of the present paper, consists of a series of seven thoracic vertebrae, with portions of ribs, a sternal bone, scapula, and a right humerus, all cemented to a mass of dark quartzose rock. A smaller mass included a femur with the pelvis; but the latter is still under the chisel. The parts exposed in the first block are the left side of the vertebræ, the scapula, and the whole of the anterior surface of the humerus, which bone remains attached, somewhat behind its natural position, to the right side of the present portion of thorax.

Vertebræ.—Of each vertebra the centrum is subcompressed ; the sides are slightly concave lengthwise between the thick convex borders of their mutually articulating terminal surfaces; these are concave (P1. XVI. fig. 1,
a, b
), the hinder one (
b
) is the deeper ; the extent of intervening part of centrum (
c
) is 5 lines. The external smooth lateral surfaces slightly
Note on the Occurrence of a new Species of
Iguanodon
in a Brick-pit of the Kimmeridge Clay at Cumnor Hurst, three miles W.S.W. of Oxford
Authors: Prestwich J. 
Published: October 2009

T
he
fact of this discovery was briefly announced in the Geological Magazine for May 1879. Since then the further progress of the works has made clearer the position of the seam in which the bones were found, and shown more exactly its relation to the mass of the Kimmeridge Clay and to the overlying Lower Greensand, about which some doubt was expressed at the time. This and the many fossils now obtained from the
Iguanodon-seam
must remove all such doubt.

The pit is situated to the left of the road leading from Oxford to Cumnor, at the foot of an outlying mass of Lower Greensand, forming a conspicuous and isolated hill rising to the height of about 500 feet. The Kimmeridge Clay here immediately underlies the Lower Greensand, without the intervention of the Portland beds (which are present on the other side of the Thames valley at Shotover), and rests upon the Coral Rag, which crops out at a distance of a few hundred yards both to the eastward and westward of the pit.
A tramway driven into the side of the hill led to the discovery of the bones in a thin sandy seam intercalated in the clay, and, at the point where discovered, about 4 feet deep beneath the surface.
The prolongation of the tramway, however, has now shown that the sandy seam runs into the hill, dipping at an angle of from 3° to 4° ; and by following up the beds till they pass under the
On the Discovery of the Place where Palæolithic Implements were made at Crayford
Authors: Spurrell F. C. J. 
Published: October 2009

I
n
the large chalk-pit at Crayford, Kent, and in the adjoining brick-pits I have noticed for some time flint flakes which I was unable to convince myself belonged to the brick-earths in which they were found, believing, from their shape, colour, and mineral condition, that they had come from another stratum of the river-deposits.

I, however, watched regularly, with great care, and during the late winter found a few flakes which, from their appearance, I felt belonged to the gently deposited brick-earths in which they lay; but they were solitary and rare, and it was not until the beginning of March last that, on the removal of a part of the face of the cliff, I came upon a dense layer of chips, specimens of which are exhibited.
The sands and clays constituting the brick-earths of Crayford, lie under a low cliff of chalk and Thanet Sand, with a cap of gravel known as Dartford-Heath gravel. This ancient cliff (fig. 1) has in parts been worn lower than others ; at one of these spots, where the wearing has invaded the chalk itself, the brick-earths are exposed lying against the chalk, which is much weathered and has the face covered with chalk-rubble ; at the base of this section is a step in the chalk cliff, and a sort of foreshore seems to have been formed, consisting here of hard sand, and there of small heaps of flint stones brought down from the cliff above by aerial action. It is
On the Skull of an Ichthyosaurus from the Lias of Whitby, apparently indicating a new Species (I. Zetlandicus, Seeley), preserved in the Woodwardian Museum of the University of Cambridge
Authors: Seeley H. G. 
Published: October 2009

E
arl
Z
etland
many years ago presented to the Woodwardian Museum a superb skull of
Ichthyosaurus
, which pertains to a new species, and from its value in exemplifying the osteology of the skull is in many respects the finest specimen known.

The anterior part of the snout is lost, but what remains of the head is 28 inches long.
The snout has the aspect of having been at least 6 inches longer. Where fractured in front the
jaw is 3 inches wide and
2½ inches deep. Its greatest transverse width behind the eyes and in front
of the quadrate bones is
16¼ inches, so that it would appear to have been somewhat more than twice as long as wide. The occipital region unfortunately is badly preserved, and the basioccipital bone is a little displaced downward and forward. There is also some imperfection of the bones of the right orbit; but otherwise the skull is in excellent preservation. Being in a hard limestone it has escaped compression and distortion, and the limestone having been cleared with a chisel, the bones of the palate as well as those of the upper surface of the skull are beautifully displayed.
In transverse section behind, the outline is a trapezoid; the upper outline of the skull,
being flat and horizontal, is 10 inches wide and parallel to the lower outline. The base,
as already mentioned, is 16¼ inches wide. The oblique sides formed by
Note on the Occurrence of Remains of Recent Plants in Brown Iron-ore
Authors: Phillips J. Arthur 
Published: October 2009

This bed of fossiliferous iron-ore is situated at Rio Tinto, in the province of Huelva, Spain, and is in close proximity to the celebrated copper-mines of that name.
In this portion of Southern Spain deposits of cupreous iron pyrites, consisting of a series of lenticular masses of ore, having a general direction a little north of east and south of west, extend from Aznalcollar, near Seville, in the east, for a distance of more than seventy miles westward to within the Portuguese frontier.
At Rio Tinto the deposits of this mineral are very extensive, and consist of a compact and intimate admixture of iron pyrites with a little copper pyrites, through which strings of the latter mineral sometimes ramify.
Although these mines appear to have been worked, and the copper smelted upon the spot, from time immemorial, it is evident from the vast heaps of furnace-slags, and from the extent of the various other remains in which coins and inscriptions of the reigns of the Emperors from Nerva to ttonorius have been discovered, that their great development under the Romans took place during the first four centuries of the Christian era. After the f.~ll of the Roman empire they seem to have been abandoned down to as late as the year 1727, from which date they were intermittently worked by the Spanish Government and by ,~arious private speculators until 1873, when they were purchased by an :English company. The extent of the mining and metallurgical operations anciently carried on in
On the Constitution and History of Grits and Sandstones
Authors: Phillips J. Arthur 
Published: October 2009

The careful and exhaustive researches relative to the constitution and mode of formation of arenaceous rocks which have recently been published by Professor Daubrde, Dr. Sorby, and others, leave open a comparatively restricted field for the pursuit of similar investigations.Having, however, during the last two years paid considerable attention to the study of rocks of this class, I now venture to bring before the notice of the Geological Society some facts and deductions therefrom which would appear to have escaped the attention of previous observers.
For the convenience of developing certain ideas relative to this subject, I propose in the present paper, in the first place, to describe various grits and sandstones which have been microscopically and otherwise examined. In doing this the older rocks will be considered first, and those of more recent age subsequently noticed in the order of their geological sequence. The chemical composition of some typical rocks will also be given.
Secondly, the results of observations bearing on the effects produced by the action of flowing water on particles of sand and gravel transported thereby will be described ; and finally, the more important observed facts will be summarized, and their bearings discussed.
The difference between grit and sandstone is one not always distinctly marked ; and numerous definitions of the two rocks, often somewhat contradictory, have been given by various geologists at different times. It has even been stated by an eminent authority that rocks which in the north of England would be called grits,
The Permian, Triassic, and Liassic Rocks of the Carlisle Basin
Authors: Holmes T. V. 
Published: October 2009

I am enabled, by permission of Prof. A. C. Ramsay, Director-General of the Geological Survey, to lay before you the general results of the Survey examination of the Permian, Triassic, and Liassic rocks in the country bordering the Solway Firth; but I do not propose to discuss here the glacial drift and other superficial beds by which the surface of the ground is almost entirely covered, and which are the main hindrance to an understanding of the rocks which form my subject this evening.
Papers on the Permian and Triassic rocks of the North-west of England have been read before this Society by Prof. Sedgwick, by Sir Roderick Murchison and Prof. Harkness, and by Mr. E. W. Binney. But as few districts promise less, except as regards drift and peat-mosses, than that immediately around the Solway, it has hitherto been dealt with, as a whole, in a brief and cursory fashion. In addition, a knowledge of certain borings, the results of which are by no means generally known, is absolutely necessary to a correct view of the structure of the Carlisle basin (see Map, Pl. XI.).
The lowest bed with which we are here concerned is the great brick-red Upper Permian sandstone, so well shown at St.-Bees Head, and named, therefore, the St.-Bees Sandstone. Between St.-Bees Head and Maryport the coast consists of the underlying Coal-measures, the St.-Bees Sandstone having been swept away by marine denudation. But at Maryport it again becomes visible, its most northerly appearance being below Swarthy
Further Notes on the Family Diastoporidæ, Busk. Species from the Lias and Oolite
Authors: Vine George Robert 
Published: October 2009

Since my first paper, “A Review of the Family Diastoporidæ for the purpose of Classification”, was written, a very important book has been published, namely ‘A History of British Marine Polyzoa,’ by the Rev. Thomas Hincks. In this work the classification adopted by Prof. Busk in his Monograph of the Fossil Polyzoa of the Crag, 1859, and also in his British-Museum Catalogue, part iii. Cyclostomata, 1875, is set aside for one that I have little hesitation in saying will prove to be far more valuable to the working student. Instead of separating
Diastopora
, and making it the type of a family, Mr. Hincks places this genus with others in his second group of the Cyclostomata, which he calls Incrustata, D'Orb. The family name which he adopts is Fam. II. Tubuliporidæ, which includes the genera

Stomatopora,
Bronn

Tubulipora,
Lamarck

Idmonea,
Lamouroux

Entalophora,
Lamouroux
.

Diastopora,
Lamouroux
(pt.).

Seeing that I have already committed myself to Prof. Busk's arrangement, it is impossible for me now to retreat; and, with this explanation, I must be excused for still adhering to the family name I used at first‡.
In his remarks on the Cyclostomata, Mr. Hineks says :—“ Simplicity is in the highest degree characteristic of the group; the cells are universally tubular; the polypide is without complexity of structure, and has a small number of tentacles; all appcndicular organs are wanting” §. In another
Description of a Peat-Bed interstratified with the Boulder-drift at Oldham
Authors: Hollingworth Geo. H. 
Published: October 2009

In the early part of September last Mr. James Nield, of Oldham, called my attention to a bed of peat which he had discovered on the site of the railway-extensions then being made by the London and North-Western Railway Co., at Rhodes Bank, Oldham.
The length of the section exposed to view was 53 feet in a north-to-south direction, and the maximum depth 14 feet; but the depth of the drift, as proved at the colliery about 100 yards to the west, is
34 1/2 feet.
The deposit is situate in the valley of the Medlock, about 25 feet above its present level ; but it has not beeen exposed by that brook,at this point, where there is from 2 to 6 feet of the upper clay still resting upon the peat. The upper clay, peat, and lower clay have probably been denuded by the action of the brook some yards to the west. The upper clay is continuous to the east for at least 200 yards, and was proved to be about 4 feet thick for 15 yards to the east of the section by the operations of the Railway Company in search of sand. At that point the sand was more than 6 feet in thickness, thc bed of peat having run out. The boulders are mostly thickness, thc bed of peat having run out. The boulders are mostly thickness, thc bed of peat having run out. The boulders are mostly from a distance (porphyries, granites,&c.) ;
On an Extinct Chelonian Reptile (
Notochelys costata
, Owen), from Australia
Authors: Owen Richard 
Published: October 2009

Hitherto the fossil reptilian remains transmitted to me for description from Austrralia have been limited to parts of the skeleton of asteh great horned Lacertian (
Megalania prisca
, Ow.).

The first evidence of a Chelonian from that continent was sent in the present year (1881), by our fellow Member Professor Archibald Liversidge, of the University of Sydney, New South Wales. He kinldy permitted a mould to be taken of the specimen, with the request that the original should be returned to him after a description and figure bad appeared. The mould and casts are in the British Museum, Cromwell Road.
The specimen was found in a formation at Flinders River, Queensland; but the nature and age of the deposit are not stated. It is petrified and, with the imbedding matrix, of great weight.
The fossil consists of an anterior portion of the carapace (fig. 1) and of the plastron (fig. 2) brought into unnaturally close contact by phosthumous pressure.

The preserved part of teh plastron includes the right and left coalesced hyo- and hyposternals (fig. 2,
hps,r
, and
hps, l
), indications of teh episternals and the entosternal; and, anterior to these parts of the plastron, both scapulo-acromial bones(
51
) have been brought into view.
Additional Discoveries of High-level Marine Drifts in North Wales, with Remarks on Driftless Areas
Authors: Mackintosh D. 
Published: October 2009

Summary of Facts and Inferences

In speculating on the origin of the high-level marine drifts described in this and in previous papers, the following facts and inferences ought to be duly taken into consideration:—

1.
High-level marine drifts, in addition to directly local stones and stones from neighbouring areas, consist to a greater or less extent of far-travelled erratic stones, while in none of them are the stones entirely local.

2.
The stones are generally much rounded, and that frequently over large areas.

3.
All the great drift-areas contain a considerable, and some of them a large percentage of granite, especially Eskdale granite, which is at least partly owing to the extent to which the Eskdale area is covered with granite fragments and pebbles in positions favourable to removal by floating ice.

4.
All the great drift areas (so far as yet known) are situated on or towards the outer slopes of mountain districts.

5.
In the interior of mountain districts high-level drifts are either absent or limited to patches.

6.
The drift-areas are more or less bounded above and below, as well as longitudinally, by areas in which the stones are angular or subangular.

7.
None of them are situated further south than latitudes in which both land ice and floating ice may at one time have existed.

8.
In all the areas there is a tendency to a knoll-shaped configuration, and in a greater or less number of instances a tendency in the knolls to occupy perched positions.

9.
The gravel and sand generally contains very few large boulders; but the latter are common in and on the surface of the clay, which generally overlies, but in many instances graduates (on the same horizon) into gravel and sand.

10.
The shells found in the drift are almost universally fragmentary, and that often, if not generally, in proportion to the roundness of the associated stones. They are likewise often confined to particular spots, as if elsewhere they had never been present, or had been destroyed by the stranding of floating ice, as is the case on many Arctic sea-shores at the present day.

11.
The idea of shell-fragments having been pushed up hill along with portions of existing sea-beds is opposed by so many facts as to render it altogether untenable.

12.
The extent to which the form of the ground has been preserved since the close of the great submergence can only be explained by supposing that either the time which has elapsed since that event, or the rate of subaërial denudation during that time, has been overestimated; in other words, the denudation must have been slow in proportion to the length of time in order to account for the little-altered surface-configuration of the drift-areas described in this and in my former paper.
On the Chalk-masses or Boulders included in the Contorted Drift of Cromer, their Origin and Mode of Transport
Authors: Reade T. Mellard 
Published: October 2009

Though for many years engaged in the study of Drift, it was not until the summer of last year that I found my way to the cliffs of Cromer.
The sections to be seen along the Cromer coast have formed a stock subject with geologists since R. C. Taylor, in 1827, and Lyell, in 1840, wrote upon them. Nevertheless they are not likely to lose their interest; for the phenomena they present are so strange and striking, and so out of the usual run of drift sections, that he would be a very unimaginative geologist who failed to be impressed by them.
Since my return I have looked up the literature of the subject. Perhaps I ought to have done so first: but there is a certain advantage in one's mind being as a blank sheet; for then the impressions come direct through one's own eyes instead of being coloured by the views of others.
The result of this examination leads me to think there is still room for further description, as well as for a reconsideration of the origin and mode of transport of the so-called “Boulders,” or Chalk-masses—a question that has been so far, it seems to me, treated in a very general, cursory, or inadequate manner.
The term “Boulder” is, of course, used by writers in its geological sense of a transported mass; but as in the vernacular it means a rounded and waterworn stone, the use of the term is very likely, without due warning, to create an image of something very different from what the Norfolk cliffs disclose.
On the Geology of a part of Costa Rica
Authors: Attwood George 
Published: October 2009

Conclusions

The conclusions at which I have arrived from a personal survey and examination of the country which I have just described, and also from the analyses and microscopical examinations made by Mr. W. H. Hudleston and myself are as follows:—

1st.
The country rock, or the general representative rock of the country, is a consolidated volcanic ash associated with augite-andesite.

2nd.
The filling of the fissures, now mineral lodes, in the Aguacate Mountains took place in the Tertiary age, and most probably in the Pliocene.

3rd.
The augite-andesites of the Aguacate Mountains are probably contemporaneous with, and have thus contributed largely to the mineral deposition and formation of the metalliferous lodes. The veinstone being found more or less mixed up with the decomposed rock, appears to indicate that their ages may be identical.

4th.
The quartz-trachytes and sandstone are recent, and most certainly Post-tertiary.
On
Neusticosaurus pusillus
(Fraas), an Amphibious Reptile having Affinities with the Terrestrial Nothosauria and with the Marine Plesiosauria
Authors: Seeley H. G. 
Published: October 2009

Conclusion
In endeavouring to estimate the value of the various resemblances to Crocodiles which I have attempted to indicate, it must be remembered that in discussing an animal which lived in the beginning of the Secondary period, comparison has had to be made with a type which still exists, and which, therefore, can scarcely give much clue to the actual modifications which its ancestral forms presented in Triassic times. But as the Crocodiles are traced back through the Teleosaurs and Belodonts there is a nearer approximation of structure towards Plesiosaurs, which may especially be seen in the conformation of the skull, form of the vertebræ, articulation of cervical ribs, and development of transverse processes from the neural arch in the dorsal region, no less than in the conformation of the elements of the pectoral and pelvic girdles. The proportions of the limbs, too, become more those of a Crocodile in such a genus as Neusticosaurus; and this genus demonstrates, I think, that the Plesiosauria must have had ancestors which lived entirely upon land, before the limbs came to be used for natation. That those animals were more nearly allied to Crocodiles than to any existing reptilian order, seems to me highly probable.
On the Relations of the Eocene and Oligocene Strata in the Hampshire Basin
Authors: Judd John W. 
Published: October 2009

Conclusion
The Lower Tongrian, as is well known, has no marine representative in the Paris basin, the great freshwater gypseous series occurring on this horizon; but in the small basin of the Cotentin, as M. G. Dollfus has so well shown, the Lower Tongrian or Brockenhurst series is represented by the “argile à Corbules”.

The Headon series, including both the sands and overlying clays, contains a fauna which, by Hébert, Sandberger, Mayer, and other authors, has been recognized under the name of the zone of
Cerithium concavum
. The Brockenhurst series contains a fauna which has been quite as universally recognized as agreeing with that of the continental Tongrian or Lower Oligocene.

Now, if my interpretation of the section be the true one, the beds containing the Tongrian fauna in the Hampshire basin overlie those containing the fauna of the zone of
Cerithium concavum
and this is the relation which is believed to exist between their continental representatives. Most geologists, indeed, group the zone of
Cerithium concavum
with the Upper Eocene or Bartonian, and the representatives of our Brockenhurst series with the Lower Oligocene.

But, according to the views of Messrs. Keeping and Tawney, the beds which in this country contain the Lower Oligocene fauna form a thin and very inconstant bed in the midst of the strata containing the fossils of the zone of
Cerithium concavum
.