bluuebunny/crossref_metadata_2025_split huggingface dataset:
Note on the so-called “Soapstone” of Fiji
Authors: Brady Henry B. 
Published: October 2009

Soon after the cession of the Fiji Islands to the British Crown, some ten or twelve years ago, it was determined bv the authorities to remove the government offices from Levuka, a flourishing settlement on the little island of Ovalau, to some locality on one of the larger islands of the group. The site chosen for the new capital was Suva Point, a promontory on the south coast of Viti Levu, commanding a considerable bay or harbour to the west, and rising on the land side to an elevation of 300 or 400 feet. How far the geological aspects of the question were taken into consideration it is needless now to inquire; we may confine our attention to the fact that the area selected presents certain peculiar and interesting features in respect of its superficial deposits.
I visited the islands in 1874–5, but owing to repeated detentions, there and elsewhere, the result of quarantine regulations, the rainy season had already set in before permission was given to land, and at Suva I was in consequence unable to do any great amount of field observation. The geological features of the localities have, however, been described by a competent naturalist, Mr. Horne, in the following terms :—
“In Viti Levu and Vanua Levu, sedimentary or limestone rocks are found on all the mountains. Where absent, denudation, it is conjectured, has been the cause... At suva the strata on the sides of the slopes lie at a greater or less, while on the
On the Position of the Obermittweida Conglomerate
Authors: Hughes T. McKenny 
Published: October 2009

On the south-west side of the little valley of the Mittweida, within an easy drive from Annaberg, about 25 miles south of Chemnitz, and twice that distance south-west of Dresden, there is a remarkable section which seems to show a strong conglomerate, crushed, it is true, but otherwise not much altered, intercalated among the gneiss and mica-schist which cover so large an area in that part of Saxony. It is therefore of some importance to inquire how far it would be possible to admit other explanations of the section than that which seems at first sight to be the obvious inference, and to consider whether an examination of the rocks in the field and a comparison of the mode of occurrence of other similar conglomerates render it possible to explain away the apparent interstratification of the conglomerate and gneissie series.
I am indebted to Professor Credner, not only for much information on the subject, but for references to previous writers. The first notice seems to be that of Dr. Sauer, of Leipzig*, under whose guidance I visited this locality a few years ago, and whom I take this opportunity of thanking for much kind attention.
The occurrence of this conglomerate is indicated on the Geological Map of Saxony and in the section given in its margin†.
Professor Justus Roth, of Berlin, wrote a paper † upon these conglomerates in 1883, and afterwards referred to them in his work on General and Chemical Geology ∮ published in Berlin in 1887.
Von
Notes on a part of the Huronian Series in the Neighbourhood of Sudbury (Canada)
Authors: Bonney T. G. 
Published: October 2009

During my visit to Canada in 1884, I had the opportunity, through the liberality of the Directors of the Canada Pacific Railway, of examining more minutely than is possible to the passing traveller the geological structure of a part of the route over which the line had recently been constructed. I had further the great advantage of being accompanied by Dr. Selwyn, the Director General of the Geological Survey of Canada, to whom I record my most grateful thanks, not only for advice and guidance on the spot, but also for information and specimens subsequently supplied. The study of these has brought out some peculiarities which I think may help to render more precise the term Huronian, and throw some light on general questions of metamorphism*.
On the Canada Pacific Railway, the Laurentian series, which has been traversed for nearly 240 miles†, comes to an end near a little station called Wahnepitae. The last rock seen is highly crystalline, an eclogite or garnetiferous hornblendic gneiss, which apparently dips at a rather low angle towards the S.E. Hard at hand is a river, on the opposite side of which rises an ice-worn range of low rocky hills considered to be the Huronian. The valley is believed to follow the line of a fault. The latter rock is mainly composed of quartz and felspar, with but little mica, though occasional thinnish bands of a fissile mica-schist occur. It is much jointed, and appears to have a flaggy bedding, reminding me in its
On the Cae Gwyn Cave
Authors: Hughes T. McKenny 
Published: October 2009

In a communication which I made to the Society “On the Drifts of the Vale of Clwyd and their Relation to the Caves and Cave-deposits”*, I considered the subject under the following heads:—
(1) The Age of the Drift.
(2) The Relation of the Deposits in the Caves to that Drift.
In discussing the age of the drift, I was of course obliged to offer a tentative classification of the Pleistocene deposits of the district in order to show the relative position and age of the St. Asaph beds, to which I referred the drift on the flanks of the hill in which the Ffynnon Beuno Caves occur.
The classification I suggested has been called in question, and I have relegated the discussion of this part of the subject in its wider bearing to a separate paper.
It will be desirable, however, to restate briefly the conclusions at which I then arrived. They were:—
That the interpretation of the glacial phenomena of North Wales is much more simple than that suggested by most recent observers in East England.
That we have evidence of the following sequence of events:—
That glacier-ice came down from the Snowdon and Arenig group of mountains, riding across pre-existing north and south valleys as far at any rate as the Cheshire plain on the east, and as far as the Irish Channel, which was the corresponding north and south valley on the west.
That glacier-ice came also from the north and held back the
On two New Lepidotoid Ganoids from the Early Mesozoic Deposits of Orange Free State, South Africa
Authors: Woodward A. Smith 
Published: October 2009

The fine series of South-African fossils brought to the British Museum in 1883 by Dr. Hugh Exton, F.G.S., Curator of the Bloemfontein Museum, Orange Free State, has already furnished two important novel types of Vertebrata, made known at the meetings of this Society by Professor Sir Richard Owen*. There still remain, however, other interesting forms, adding to our knowledge of the palæontology of the early Mesozoic strata whence they were derived, and among these are some beautifully preserved examples of a Lepidotoid Ganoid fish. Two specimens of another new Ganoid have also been lately received from the same source, and the affinities of these types have so important a bearing upon the question of the age of the Stormberg Beds of South Africa, that it seems advisable to place on record their discovery and to offer a detailed description of their characters.
I. Seminotus capensis, sp. nov.† (Pl. VI. figs. 1-5.)
The first series of the fossil fishes in question comprises portions of four individuals displayed upon the surface of a slab of sandstone, mainly in counterpart. Each of these shows more or less of the scaly trunk; and, in addition, one example exhibits the head, pectoral fin, and dorsal fin; another, the dorsal and caudal fins; a third, a nearly complete tail and the anal fin; while the fourth is almost perfect behind a point a little in advance of the pelvic fins. There are thus materials for determining all the more salient features of the
On Insoluble Residues obtained from the Carboniferous-Limestone Series at Clifton
Authors: Wethered Edward 
Published: October 2009

The Carboniferous-Limestone rocks at Clifton are well known and have been the subject of several communications to the Geological and other Societies. Among the authors of such communications I may mention Sir H. de la Beche, Sir A. Ramsay, Dr. Buck]and, Mr. Conybeare, Mr. Etheridge, Mr. Tawney, and Mr. Stoddart; the papers and monographs written by the investigators just named deal mostly with the physical, stratigraphical, or palæontological problems which the rocks of the gorge of the Avon have presented for solution; I am not aware that any one has examined the residues obtained from the limestone after boiling portions in strong acid.
Professor Hull's classification of the Carboniferous series seems to me to be the most comprehensive yet produced; but there may be some difference of opinion as to the term Yoredale when applied to the Upper Limestone of the Bristol and Somersetshire coal-fields. If Professor Hull means, by the term Yoredale, the beds which mark those physical conditions which closed the Limestone Period and ushered in the Millstone Grit and Coal-measures, then he is correct in saying that there is at Clifton a series of deposits, represented by a thickness of about 100 feet, which mark the close of the Limestone Period and the coming in of the Millstone Grit. They are the beds referred to by Sir H. de la Beche as “Upper Mixture of Sandstones, Marls, and Limestones.”
Hitherto the limestones known as the “Black Rock” have been regarded as the base of the Middle
On
Ailurus anglicus
, a new Carnivore from the Red Crag
Authors: Dawkins W. Boyd 
Published: October 2009

§I. Introductory.
In the fine collection of fossils from the Crag of Norfolk and Suffolk, presented to the Museum of the Yorkshire Philosophical Society at York by Dr. Reed, is a battered and water-worn specimen, which is of singular interest, because it carries the range of one of the most restricted of the genera of the Oriental Province far to the west and to the north of its present habitat. It is a small fragment of the right lower jaw, with the last true molar in position, found in the Red Crag of Felixstowe, the rest of the ramus and the angle and articular and coronoid processes being broken away (see figs. 1 and 2).
§2. Description and Comparison with Ailurus fulgens.

After a long and careful study, I find that the lower jaw in question differs in a marked degree from all the European fossil Carnivores, and presents no important points of difference when compared with the series of jaws of recent
Ailurus
in the British Museum.

The last true molar in the fossil is implanted in the jaw by two fangs, the anterior being the smaller, and supporting the anterior cusps,
A
and
D
of figures 1, 2, 3, 4. The multicuspid crown is composed of three small, obtusely pointed cusps,
A, B, c
of figs. 1, 3, and 4, on the outer side, while the inner (figs. 2 and 3) is occupied by the large cusp
D
and a smaller hind cusp
F
, connected by a line
Note on the Movement of Scree-Material
Authors: Davison Charles 
Published: October 2009

The slope of screes being, as a rule, not much under the greatest angle at which it is possible for their component material to rest, it follows that a very slight force is in general required to put the surface-stones in motion. This is evident, too, from the number of stones dislodged when a block falls down from above; also from the difficulty experienced by persons in trying to cross them. “Every movement,” says Scoresby, describing the descent of a mountain covered with loose stones in Spitzbergen, “was a work of deliberation. The stones were so sharp that they cut our boots and pained our feet, and so loose that they gave way almost at every step, and frequently threw us backward with force against the hill. We were careful to advance abreast of each other, for any individual being below us would have been in danger of being overwhelmed with the stones, which we unintentionally dislodged in showers”†.
The instability of scree-material being so great, the causes of its motion are consequently numerous. Many have at various times been pointed out, more especially in considering the origin of different accumulations of angular débris, such as the limestone-breccias of Gibraltar or the stone-rivers of the Falkland Islands, the main difficulty in these cases being, however, to account for the transport of the material over surfaces inclined at a small angle. References to these well-known discussions are perhaps hardly necessary, it being the object of this paper to call attention
On the Cambrian and associated Rocks in North-west Caernarvonshire
Authors: Blake J. F. 
Published: October 2009

Introduction.
The area to which the present memoir refers has for a long time attracted the attention of geologists, partly because within it may be found the oldest portion of the Cambrian series, and therefore the supposed base of our known stratified rocks, and partly because, of late years, there has been an expectation of finding here some representatives of still older series.
The most recent observers, indeed, agree in regarding the whole of the mass coloured as porphyry between Bangor and Caernarvon, and some part of that coloured altered Cambrian, as belonging to a Pre-Cambrian epoch, and the felsite of Llyn Padarn and Moel Tryfaen they treat in the same way. There is no difference of opinion between them on this latter area, but as to the former, though all divide the mass into three parts—the mass near Caernarvon, the mass near Dinorwic, and that near Bangor,—Prof. Hughes considers all three a connected series of “beds,” Prof. Bonney regards the Caernarvon rock as very old, and the other two as connected, while Dr. Hicks regards them as representing three independent and unconformable groups. Again, Prof. Bonney and Prof. Hughes differ as to the stratigraphy near Bangor, with the effect that the former considers much more to be Pre-Cambrian than the latter does. All three views are diametrically opposed to that of the Survey, not only as to theories but as to many of the facts. Nor has the Survey given way. Prof. Ramsay, in 1881*, says the proposed changes
An Estimate of Post-Glacial Time
Authors: Reade T. Mellard 
Published: October 2009

Of late several attempts have been made to show that the close of the Glacial period was very recent.
Having personally devoted considerable attention to what is called Post-glacial or “superficial” geology, I am much struck with the imperfect knowledge with which the question of Post-glacial time is frequently approached.
The writers seem to be unaware of, or to insufficiently appreciate, the grand sequence of events recorded in the deposits on the Lancashire and Cheshire coasts which have taken place since the snow and ice of the Glacial period disappeared.
On the borders of the coast-line between the Dee, the Mersey, and the Ribble, the student who cares to pursue the subject can do so with great advantage. But through the horizontality of the deposits, and their general low level, none occurring above the level of the 25 feet Ordnance datum and all reaching down to below the level of the lowest spring-tides, the study has to be pursued through the medium of excavations and borings. This I have done in observations extending over many years, and I now propose to show their bearing upon the absorbing question of recent geological time.

Denudation of the Low-Level Marine Boulder-clay.

The whole of the country to which these notes specially refer was formerly entirely covered with a mantle of Low-level marine Boulder-clay and sands. These I have described at length in several papers.
That the valleys of the Dee, Mersey, and Ribble were at one time filled with Low-level marine Boulder-clay, we
Notes on Rock-specimens collected by Mr. Fox from the Islands of the Lizard Head
Authors: Teall J. J. H. 
Published: October 2009

The two small islands of Mên Hyr and Vasiler lie half a mile due south of Polpeor. A line drawn between these islands in a N.W. by W. direction passes through the Clidgas Rocks, the Man-of-War Rocks, and the Stags. These islands, together with Taylor's Rocks and Mulvin, which lie slightly to the south-west of the above line, constitute what may be termed the Outer Group. Inside these we have Enoch Rock, Pen Ervan, Labham Reefs, Labham Rocks, Mên Par, the Shag Rock, Wiltshire, the Quadrant, and Sanspareil. We will now describe the rocks from the different islands, taking the latter in the order mentioned.
Outer Group.

Mên Hyr
.—A coarse gneissose rock showing a marked foliation. Dark lenticular patches, rich in ferro-magnesian minerals, alternate with light-coloured patches of similar form composed of quartz and felspar or pseudomorphous substances after felspar. Under the microscope the rock is seen to be composed essentially of felspar, quartz, dark mica, and hornblende. The felspar is so altered in places as to have lost all individual action on polarized light; it is then represented either by aggregates of a vividly polarizing scaly mineral (mica) or by patches which appear opaque by transmitted, and snow-white by reflected light. The unaltered felspar is abundant in certain portions of the slide; the larger grains are mostly striated. Quartz occurs in grains and granular aggregates. The quartz and felspar in certain portions of the slide exhibit the relations characteristic of igneous rocks; in others they form a fine-grained granulitic
On the Probable Mode of Transport of the Fragments of Granite and other Rocks which are found imbedded in the Carboniferous Limestone of the Neighbourhood of Dublin
Authors: Ball V. 
Published: October 2009

For some time I have been endeavouring to obtain specimens of the limestone containing fragments of granite which were first found nearly forty years ago in the neighbourhood of Dublin. The quarries being now filled up and inaccessible, I followed on the track suggested by having observed a specimen built into a garden wall, and through the aid of Mr. H. B. White, M.E., I was enabled to discover a wall in which such specimens occurred in considerable abundance. The permission of the owner, Dr. E. P. Wright, having been obtained, a fine series of blocks, in which the granite was visible, was delivered at the museum; these, after they had been trimmed and split by a stone-mason, afforded such a variety of beautiful specimens that I have thought it would interest the Society to exhibit a selection of them, as I believe comparatively few geologists have had an opportunity of examining anything of the kind.
The examination of these specimens has revealed the presence not only of angular fragments of granite but also of schist, quartzite, and vein-quartz, such as might have been derived from the metamorphosed Silurian rocks which rest on the granite near Dublin, and are in one locality exposed in a sea-cliff at the base of Killiney hill. As a rule, these fragments, though in some cases permeated with calcareous matter, show little if any signs of of decomposition; the surfaces of contact with the enveloping limestone are sharp and clean, and the adhesion is very
On the Monian System of Rocks
Authors: Blake J. F. 
Published: October 2009

Introduction.
Is there no order in Pre-Cambrian rocks? Do they consist in one area of great undulating masses of gneiss, in which those who have studied them refuse to recognize any stratigraphical sequence, and in another of tiny fragments of formations, two or three of which may be contained within an area of a few square miles ? and are these types in no way connected ? Such were the questions which forced themselves upon me after brief consecutive visits to the Highlands and St. David's. Consulting my friend Dr. Callaway on these points, he advised me to go to Anglesey, where I should find rocks that might fairly be compared with the gneiss of the Highlands in character, in close proximity to, if not associated with, volcanic rocks of the type of St. David's. I went; and after three years' work in summer and spring vacations have arrived at conclusions which I now venture to lay before the Society.
But in the forefront of this inquiry we are met by the fact that Sir Andrew Ramsay, who knows the district as one knows one's native hills, has declared that there are no Pre-Cambrian rocks in Anglesey at all. Can we ignore this fact? or must we not first ascertain the reasons which have led to this conclusion ? If after a study of the area, sufficiently prolonged to place one's self somewhat on a level with his knowledge of the rocks, one reads his words, they strike one as
On the Spheroid-bearing Granite of Mullaghderg, Co. Donegal
Authors: Hatch Frederick H. 
Published: October 2009

On returning from a recent inspection of the field-work of the Geological Survey in Ireland, Prof. A. Geikie brought with him some remarkable specimens of spheroidal concretions, which, on account of their interesting structure, he thought worthy of detailed examination and description. For this purpose they were entrusted to me, and the present paper records my observations.
These bodies were found by Mr. J. R. Kilroe, of the Geological Survey of Ireland, in granite at Mullaghderg, Dungloe, Co. Donegal. According to Mr. Kilroe, they occur in a mass, measurig 5 or 6 cubic yards, which lies in coarse granite. It consists “of concretionary balls, varying in size up to 6 inches in diameter. The balls are usually flattened and lie almost contiguously, the interstices being filled by granite, which is similar in character to, though muchfiner-grained than, that surrounding the entire mass.”
In a letter I have since received from Mr. Kilroe he informs me that dykes are numerous in the locality where the spheroids occur. One of these passes quite close to the mass containing the concretions; but since the latter are confined to a small space and do not follow the dyke, I see no reason for connecting their formation with its intrusion.
The Normal Granite.—Of the granite referred to above, Mr. Kilroe was kind enough to furnish me with specimens.
It is a coarse-grained rock, varying in colour from a pale fleshtint to a reddish brown. The specimens in my possession have a somewhat loose and crumbly
The Upper Eocene, comprising the Barton and Upper Bagshot Formations
Authors: Gardner J. Starkie , Keeping Henry , Monckton H. W. 
Published: October 2009

T
he
introduction of the Oligocene stage into our classification has necessitated a partial revision of the grouping of our older British Tertiaries. Whether this introduction of a new primary division into the Tertiary system was necessary or expedient may still be questioned; but it has been generally adopted and is, for the time being, established. The division does not coincide in England with a marked change in either fauna or flora, though the series seems nevertheless tolerably complete and well developed; its limits, however widely stretched, show that the Oligocene stage compares neither with the Eocene nor the Miocene in importance.

Opinions have differed as to where the line of division should be drawn; whether this should be as low down as the top of the Barton Beds or at the base of the Headon Beds, or even higher. For our part, we think it desirable to uphold the view which places the demarcation between the top of the Bagshot Sands of Alum Bay and the base of the Lower Headon Series, though it is perfectly obvious that any such line in the midst of our series must be a purely artificial one.
An almost necessary consequence of the change in the classification has been the readjustment of the divisions of our truncated Eocene, only the middle and lower division remaining, so that the term “Middle” without, an Upper Eocene would no longer be an appropriate one. But the Middle Eocene, embracing as it does such formations as the Nummulitic