bluuebunny/crossref_metadata_2025_split huggingface dataset:
The Cascade Anthracitic Coal-field of the Rocky Mountains, Canada
Authors: Merritt Wm. Hamilton 
Published: October 2009

This Coal-field occurs in the moat eastern valley of the Rocky Mountains, the Bow-River valley.
The Cretaceous rocks, which underlie a large area of foot-hills and prairie to the east, have here been caught up and crop out in the bottom of a trough between two parallel rows of mountains, composed of Palæozoic rocks, which rise to a height of about 3000 feet above the river on either side, or some 7000 feet above the sea. The softer shales and sandstones of the Cretaceous rocks have been worn away and form the valley-bottom, and are for the most part covered with gravel from 100 to 200 feet in thickness. The height of the valley above the sea is some 4300 feet.
Both the rocks of the mountains on either side and those of the valley are tilted up and show a dip of between 30° and 40° to the west of south (magnetic) and a strike of from 25° to 30° north of west (magnetic).
Though there are minor local disturbances of the rocks, this dip and strike may be said to be constant throughout the Coal-field.
From palæontological evidence, the age of the Palæozoic rocks is thought by Mr. Whiteaves, Palæontologist to the Geological Survey of Canada, to be of Lower or Sub-Carboniferous, or possibly Devonian age, though probably the former.

The fossils which I collected from these rocks were chiefly Crinoids,
Zaphrentis
,
Spirifera
, and long-winged
Spirifera
.

The rocks are massive Limestones and Dolomites.
The Cretaceous rocks consist of
The Terraces of Rotomahana
Authors: Martin Josiah 
Published: October 2009

The destruction, by explosion connected with the eruption of Tarawera, 10th June, 1886, of the world-renowned Terraces of Rotomahana invests with a melancholy interest the subject of this paper. A calamity so complete and overwhelming that not a vestige of these magnificent monuments of Nature's architecture remains to mark their site, has called forth expressions of sincere regret, not merely from the inhabitants of New Zealand, but also from every student of Nature's phenomena, every lover of the picturesque and beautiful, as well as from every casual visitor to this wonderful district.
As the chief centre of attraction to tourists through the Hot-Lake district, the Terraces of Rotomahana have been frequently described. Poets, men of science, and historians have endeavoured to express in varied language the impressions which these unique structures have produced upon them, while painting and photography have made known to some extent their delicacy of colour and variety of form. Most of the writers have, however, admitted their inability to give, from a rapid survey of the whole, more than a brief and incomplete description. In fact nothing beyond a generalized or vague idea could be acquired, except by a prolonged residence on the spot, a close familiarity with the place in all its varying aspects, a continuous study of the marvellous range of phenomena, and an intimate acquaintance with and patient observation of their periodicity and more salient characteristics.
The largest and most important structure, but lately so well known as the White Terrace, was of
The Eruption of Mount Tarawera
Authors: Hutton F. W. 
Published: October 2009

The eruption of Mt. Tarawera, in the North Island of New Zealand, took place on the 10th of June, 1886. I was not able to leave Christchurch at once, but arrived at Rotorua on the 26th of June. During my stay in the district, which lasted till 14th of July, I examined Rotomahana and Okaro, and went across the Kaingaroa plains to Galatea. Subsequently, with Prof. F. D. Brown and Prof. A. P. Thomas, I visited Lakes Rotoiti and Rotoehu.
Description of the District. About 25 miles south-west of Lake Taupe is Ruapehu (fig. 1), a truncated cone 9195 feet high, covered with perpetual snow. Until lately it was thought to be extinct, and is so described by Dr. yon Hoehstetter ; but for several months past steam has occasionally been noticed issuing from the summit, and on the 16th of April last, Mr. L. Cutten, Surveyor, ascended the mountain and found the crater on the top to be 300 feet deep, with hot, eddying, and steaming water at the bottom, which had melted the snow all round for 40 feet, although about 100 feet above the water there was a fringe of ice.
The next day a large column of steam, 100 feet high, ascended fromthe crater. No earthquakes are recorded in the neighbourhoodduring" the whole of this time. Between Ruapehu and Taupe liesTongariro, the principal cone of which, Ngauruhoö, as well as twoother smaller cones to the north, constantly emit steam. Ngauruhoöwas in active eruption on July 6,
On the Correlation of the Upper Jurassic Rocks of the Swiss Jura with those of England
Authors: Roberts Thomas 
Published: October 2009

In the summer of 1884 the author was sent out by the University of Cambridge, with a grant from the Worts Fund, to study the Jurassic rocks of the Jura. He was accompanied by Mr. E. W. Small, M.A., Christ's College. Some of the results then obtained are given in the present paper.
The Jura range of mountains is formed in great part of rocks of Jurassic age, which have been thrown into a series of folds running more or less parallel to each other in a north-east and south-west direction. These folds are usually quite simple, and it only rarely occurs that the foldings have gone on to such an extent that the beds are inverted.
If one examines a geological map of the district, it will be seen that the surface of the ground is occupied principally by Upper Jurassic Rocks; indeed all the higher ground is so formed, and it is only in the valleys and gorges which run transversely across the folds, or in the centre of the folds where the upper portion has been removed by denudation, that older beds are seen.
In this paper it is proposed to deal only with the Upper Jurassic Rocks. In this term are included all the beds which lie between the base of the Callovian and the summit of the Purbeckian, and as such it is generally understood by English geologists. This classification, however, differs from that given by many foreign authors, since what is here included in
Supplementary Note on the Walton-Common Section
Authors: Hudleston W. H. 
Published: October 2009

There seems to be so much uncertainty as to the character of the basal beds of the Lower Bagshots in the London Basin that any opportunity which affords us unmistakable evidence of their real nature should be seized without delay. We have had so much theorizing, based upon the evidence of well-sections and of limited exposures, that we turn with pleasure to a good continuous section like the one which has lately been disclosed between Walton and Weybridge on the London and South-Western Railway. The main features of the Lower Bagshot series in this section, at its actual junction with the London Clay, were very fully described by me in a communication made to the Society last year. Whether we regard the junction there shown as evidence of an unconformity or otherwise, the fact of a complete lithological change is patent to all.
1. Recapitulation of some points in the previous paper.
Resting immediately upon the grey-coloured and sticky London Clay, distinguished by its fine and perfectly regular bedding, is a sharp yellow sand full of current-bedding. This yellow sand I dabbed “No. 1 Bagshots.” Then follows the first clay series, which I called No. 2, or the “Blue Bagshots.” It is surmounted by a second sandy series, referred to in my previous paper as “No. 3 Bagshots.” As far as the new cutting for the widening of the line had then progressed, there was no reason to suppose that No. 3 was succeeded by a second clay series, beyond
On the Rocks of the Malvern Hills
Authors: Rutley Frank 
Published: October 2009

The rocks of the Malvern Hills have already been the subject of much discussion, and some of our most eminent geologists have devoted a large amount of time and trouble to the unravelling of their history.
One of the most important papers, however, upon this subject was written by Dr. Harvey B. Holl, over twenty years ago; and with this paper and a few maps I have spent several weeks in examining the range.
The general result of this examination may be of interest, inasmuch as it enables me to confirm to a great extent the statements made by Dr. Holl, whose careful observations and sound inferences cannot fail to impress those who endeavour to follow up his work.
One of the main points which Dr. Holl wished to demonstrate was, “that the rocks which had hitherto been treated of as syenite, and supposed to form the axis of the hills, were in reality of metamorphic origin, and belonged to the Pre-Cambrian, Azoic, or Laurentian Age.” I think that, at the present day, many geologists will be found who are ready to accept this conclusion, in spite of the protest of the late Sir Roderick Murchison.
Dr. Holl, in his paper, discusses first the structure and origin of the crystalline rocks of the Malvern Hills, he next treats of the adjacent Palæozoic strata, and finally endeavours to show the chronological relationship of the several events in their geological history.
Without attempting to follow out such an extensive programme, I have
On the Ancient Beach and Boulders near Braunton and Croyde, in N. Devon
Authors: Hughes T. McKenny 
Published: October 2009

The ancient high-level beaches of the south-west of England have long attracted notice. Paris referred some of them to blown sand; Carne and Boase mentioned the occurrence of similar phenomena around the coast of Cornwall. Godwin-Austen described a “raised beach” at Hope's Nose, and later on, in his paper on the superficial accumulations of the coasts of the English Channel, gave an account of several other deposits in different localities, which seemed to him to indicate an elevation of the coast-line. The position of many of these beaches is indicated by Greenough on his geological map and by De la Beche on the maps of the Geological Survey.
Among the raised beaches we generally find included the sandcliffs of Saunton Down and Middle Borough, on the coast west of Barnstaple. These deposits have a further interest attached to them from the occurrence at their base of large boulders of various kinds of rock, some of which, it would seem, do not exactly resemble any rock-masses in the drainage-areas from which they could have been transported to where they are now found by any kind of river-action.
Sedgwick, Murchison, Williams, and De la Beche have described these cliffs, pointing out the similarity of the deposits to those of the modern shore, and, assuming that the whole was an ancient beach, of course explained itz present position by changes in the relative level of land and sea. It seems to have been generally spoken of as a Raised Beach from the time
On some Results of Pressure and of the Intrusion of Granite in Stratified Palæozoic Rocks near Morlaix, in Brittany
Authors: Bonney T. G. 
Published: October 2009

In my paper on the “Structures and Relations of some of the Older Rocks of Brittany”* I briefly referred to the slaty rocks in the neighbourhood of Morlaix. As the main object of my journey was to study the older and, presumably, Archæan rocks of Brittany, only a moderate amount of time was devoted to those of later date, and not many specimens were collected. These, however, have proved of unusual interest; so I venture to offer a few remarks upon them to the Society, because, as I anticipated, they seem to throw some light upon the history of the genesis of certain crystalline schists.
The rock beneath and in the immediate neighbourhood of Morlaix consists of alternating bands, differing in texture and colour†. The grey material, at the time of deposition, was evidently a fine-grained silt or earthy sand, the dark a carbonaceous mud. The layers of the former commonly do not exceed an inch in thickness, and are often less; the others are frequently more; but extremely thin, more or less lenticular streaks of the one material are occasionally interlaminated with the other. Both are cleaved, the sandy band imperfectly, the dark band very completely. Commonly the planes of cleavage and stratification coincide, and then the rock has a compressed appearance; but minor folds and “wriggles” are frequent, so that the “stripe” is cut by the cleavage-planes at very different angles. In these cases the change in amount and direction of the cleavage, the thickening of
On
Thecospondylus Daviesi
(Seeley), with some Remarks on the Classification of the Dinosauria
Authors: Seeley H. G. 
Published: October 2009

In the Fox Collection in the British Museum is the anterior third of a vertebra,
with the number R/181 from the Wealden Beds of Brook, in the Isle of Wight, which indicates an animal of a type which hitherto has had but one other representative in Europe. With his usual acumen Mr. William Davies, F.G.S., recognized it as being the cervical vertebra of an animal closely allied to the genus Cœlurus of Marsh. No one would have been more competent than that veteran palæontologist to have written its history; and if I gladly undertake the task, it is because it enables me to suggest this honour to the work of a distinguished pioneer, whose labours on the Fossil Vertebrata have smoothed the way and facilitated the studies of every student of the National Collections for the last quarter of a century.
Imperfect as the specimen is, it may serve as a nucleus round which knowledge will accumulate, until the genus becomes as well known as the larger Wealden reptiles.
The centrum is elongated, compressed from side to side, with a flattened base, and flattened subquadrate anterior articular face, with the sides of the face prolonged backwards as subparallel sides, and as a ventral surface which is subparallel to the neural canal. The cervical ribs are co-ossified with the centrum and neural arch. The bony tissue, not unlike that of Ornithosaurs for its relative thickness, forms a dense external film, which defines the form of the
Supplementary Notes on the Stratigraphy of the Bagshot Beds of the London Basin
Authors: Irving A. 
Published: October 2009

In this paper it is intended to lay before the Society the results of additional work in this Formation done during the year 1887. It deals with the succession of the beds all along the northern margin of the district, from Farley Hill near Reading to Englefield Green, and with the development of the formation in the more westerly portion of the area (basin of the Kennet).
Part I.
In this part of the paper I shall attempt to show from the description of numerous sections that the inference as to marginal conditions in my last paper is found to hold all along the northern flank of the district.
In the recent discussion of this subject some ambiguity has crept into the use of the term “Middle Bagshot.” For my part I have, as I believe, consistently used the term throughout with the exact connotation which I gave to it in the year 1883*, and in the Quarterly Journal of the year 1885 (vol. xli. p. 494). In the Wellington-College section it is seen to include beds of the horizons Nos. 3-10; and whenever I have found a complexus of beds answering in general physical character to these, I have assigned them to the Middle Stage without taking the empirical consideration of mere thickness into account; since in none of the deep-well sections of the interior of the district have we anything approaching to a recurrence of such a series in either the Upper or Lower stages.
North Flank
On some additional Occurrences of Tachylyte
Authors: Cole Grenville A. J. 
Published: October 2009

Since the spring of 1883, when I had the honour of being associated with Prof. Judd in a paper on the Basalt-glass of the Western Isles of Scotland*, a few additional occurrences of tachylyte in the British Isles have come under my notice in the field. Specimens have been thus collected from Ardtun in Mull, Kilmelfort in Argyll, from near Bryansford, County Down, in Ireland, and among certain older rocks of the Welsh border. I am also enabled, by the kindness of my friend Mr. A. W. Dymond, to give an account of the microscopic characters of the tachylyte of the Quiraing in Skye.
The Duke of Argyll, in his classic description of the leaf-beds of Ardtun in Mull†, refers to a glassy layer between two of the basaltic masses of the headland; and the same occurrence was mentioned by Mr. Koch during the discussion on the paper dealing with Scottish basalt-glass. Mr. J. Starkie Gardner, who called my attention to the rock upon the ground itself, has described and figured the course of an intrusive sheet that forms a very conspicuous feature at Ardtun‡. At its most accessible portion it is about 8 ft. thick, and in the centre still retains, as shown by microscopic examination, a considerable amount of colourless glassy matter. In this matrix cumulites and belonites are developed; plagioclase felspar is abundant, interspersed with brown prismatic augite, while the magnetite is collected into crystals that are often well defined. On a sea-face so exposed the
On the Cae Gwyn Cave, North Wales
Authors: Hicks Henry 
Published: October 2009

Summary

The recent researches at Cae Gwyn have proved most conclusively that there was no foundation for the views of those who contended that the drift which crossed over the entrance and extended into the cavern was
remanié
, and had gradually crept down the hill. They have shown beyond the possibility of doubt that the deposits which overlie the bone-earth are
in situ
, and are identical with the typical glacial deposits of the area. It was found also that these deposits had at one time extended continuously across the valley above this elevation (400 feet above ordnance datum), and that the caverns had consequently been completely buried beneath them. The explorations carried on in 1885, 1886, and 1887, in the Cae Gwyn and Ffynnon Beuno caverns, show that they must have been occupied by the animals before any of the Glacial deposits now found there had accumulated, also that a thick floor of stalagmite had formed over these remains before the caverns were subjected to water-action. This action broke up the floor and completely re-sorted the materials, evidently washing out some, but also adding sandy and gravelly material to the deposits. Very large blocks of limestone, which were found at many points in the caverns, had evidently been disturbed by the same force, and had in many cases protected the original contents; they were, however, invariably found in the lowest deposits, and were covered over by laminated clay, sands, and gravels. It is certain that the caverns had been completely filled
The Greensand Bed at the Base of the Thanet Sand
Authors: Gardiner Margaret I. 
Published: October 2009

This bed may be seen at various points from Pegwell Bay in the east to Chislehurst in the west of Kent, and there is a bed at Sudbury, in the N.W. corner of Suffolk, which Mr. Whitaker considers to be the same. At Lewisham and Croydon, to the west of Chislehurst, it is missing, and the light buff micaceous sand which usually succeeds it in West Kent rests directly on the flint bed above the chalk; so that, unless either the 9 inches of greensand and flint or the 2 feet of grey sand last seen in 1830 at Epsom by Prof. Prestwich are the same, the succeeding beds of the Thanet Sand overlap it westwards.
Specimens have been obtained from Pegwell Bay, Chislet near Herne Bay, Upnor, Chislehurst, and Sudbury. Leaving for the present the Sudbury sand out of consideration, this basement bed is a very fine sand formed of about equal quantities of dark and light grains mixed with more or less clayey matter. Its appearance in a section varies considerably with the weather, for it is the dark greenish grey of the darker grains which gives the colour when it is wet ; but when it is dry the clayey matter becomes a white powder, and is a much more conspicuous constituent. A microscopic inspection shows the sand to consist of quartz, flint, glauconite, and small quantities of felspar and various rarer minerals, with a few casts of microscopic organisms.

Quartz
.—The quartz is in not much rounded
On the Durham Salt-District
Authors: Wilson E. 
Published: October 2009

The new salt-field in the North of England occupies the low-lying country bordering the estuary of the Tees, situate partly in Yorkshire, partly in Durham, and bounded by the Magnesian Limestone district of Durham on the north, by the Jurassic hills of Cleveland on the south, and by the German Ocean on the east.
At the present time this salt-field has a proved or fairly indicated area of at least twelve square miles. Of this area, however, more than half lies beneath the sea, and is therefore inaccessible by the only system of working at present in operation in the district. Beyond these limits, however, the Durham salt-field has probably a wide extension. Evidences of a limitation of the field in a northerly and also in a westerly direction have, indeed, been obtained; but what are its boundaries on the south and on the east we have not as yet, and perhaps never shall have, any means of determining.
Discovery of the Rock-salt at Middlesborough and Origin and Progress of the Salt Industry in South Durham.
In the year 1859, Messrs Bolckow and Vaughan, the celebrated ironmasters of Middlesborough-on-Tees, being in want of water at their Middlesborough Ironworks, had a borehole, 18 inches in diameter, put down to a depth of 1200 feet. Although large supplies of water were yielded by the more pervious strata passed through in this boring, this water was so highly charged with sulphate of lime as to be quite unfit for the purposes for which
On the Horizontal Movements of Rocks, and the Relation of these Movements to the Formation of Dykes and Faults and to Denudation and the Thickening of Strata
Authors: Barlow William 
Published: October 2009

I propose to call attention to some horizontal movements of rock occasioned by gravitation, the importance of which has, I believe, been almost entirely overlooked, and shall try to show that the great forces of denudation in many cases owe much of their power to fissuring and dislocation produced by these movements, also that to these movements is to be referred the production of dykes and faults.
In the Grand Cañion District of the American Union a wide expanse of elevated horizontal strata, some thousands of square miles in extent, has been denuded in such a manner as to display a succession of huge terraces or steps of successive strata, each terrace being terminated by a sinuous line of cliffs or abrupt slopes.

Between the succeeding escarpments the strata dip slightly from the crest of the one below to the foot of the next above. In the median parts of any given terrace the strata are very nearly horizontal and have inclinations scarcely exceeding one degree;
but as we approach the escarpment of the next higher terrace, the inclination increases to three or four degrees, becoming a maximum at the base of this wall
.

The cumulative effect of the slight dip thus displayed, which for the most part has a northerly direction, is that the top of a certain stratum, the Carboniferous, is more than 8000 feet lower at the north, below the topmost terrace, than at the south, where it comes to the surface and forms a wide plateau,