bluuebunny/crossref_metadata_2025_split huggingface dataset:
On the Palæozoic Basin of the State of New York. Part III. An Inquiry into the Sedimentary and other External Relations of the Palæozoic Fossils of the State of New York
Authors: Bigsby J. J. 
Published: October 2009

The objects proposed in this inquiry are—to give more precision to facts as yet imperfectly ascertained, and to discover, if possible, new materials for the history of these early times, and new points of connexion between the palæozoic basins of the State of New York and of Wales—countries which are therefore the subject of frequent comparison in these pages.
This communication is divided into four parts. The first part, after a few preliminary observations on the agencies by which the sediments or sea-bottoms were laid down, will treat of their mineral character. The second will be devoted to the distribution and immediate relations of animal life to the strata which the fossil remains occupy. The third will deal with the “recurrence” or vertical range of these fossil species,—their order of precedence, duration, increment, and decrement throughout the older palæozoic epochs. The fourth, and concluding, part will consist of general statements and inferences.
By the expression “external relations” is meant such as do not directly lead us to the consideration of structural or physiological distinctions; the latter belong to a separate and very important field of investigation.

§ 1.

Conditions and characters of Sediments
.—It being a generally received fact that palæozoic fossils usually passed their lives in and about the sedimentary strata in which they are found, some very brief remarks on the origin and nature of the latter may be excused. The agents concerned in the formation of strata may be divided into two great classes :—1st. The constant and superficial, often
On the Veins of Tin-ore, at Evigtok, near Arksut, Greenland
Authors: Tayler J. W. 
Published: October 2009

The area over which the veins of tin extend is about 1500 feet in length, by 80 in breadth; their
number is eighteen or twenty; and they run in various directions, some E. and W., others N.E. and
S.W., or N. and S. The tin occurs also disseminated in crystals through the rocks, and accompanying
the finer-grained galena and tantalite. The appearance of the veins at the surface is not very
promising, the tin being in small detached crystals, scattered through the gangue (which is mostly
quartz). The widest of those veins is 10 inches,—the tin being 1 or
1 ¼ inch, occupying one side of the vein. The gangue here is felspar, quartz, sparry
iron (carbonate of iron?), and fluor-spar. This vein runs E. and W., into the white cryolite.
Another vein, about 200 feet west from the cryolite, is visible for about thirty paces; at the
surface it is not more than ⅓ of an inch thick, but at a depth of 6 feet it is 3 inches thick. Other veins are,
at the surface, mere strings, varying from ½ to ¼ of an inch thick. Nearly all these veins occur in a large vein or bed of felspar
and quartz, some of the crystals of the latter having a diameter of 18 inches. This mass contains,
in a limited space, various other minerals, such as galena, blende, copper-, iron-, and
arsenical-pyrites, fluor-spar, black cryolite, tantalite, molybdena, sparry iron, zircon,
&c.
There are some peculiarities connected with these tin-veins, which deserve consideration, and
would lead one to expect that at a greater depth they might afford a large produce. The only
surface-vein which can be seen sectionally 9 (no sinkings having yet been made) widens rapidly as
it descends; and in other spots sectional
On some Recent Discoveries of Flint Implements in Drift-deposits in Hants and Wilts
Authors: Evans John 
Published: October 2009

Having within the last few days visited, in company with Mr. Prestwich, the scenes of two recent discoveries of Flint Implements in gravel in the south of England, I think a few notes upon the subject may be of interest to this Society.
The discoveries in question have taken place, the one on the seashore, about midway between Southampton and Gosport, where Implements have been found by Mr. James Brown, of Salisbury; and the other at Fisherton, near Salisbury, where they have been discovered by Dr. H. P. Blackmore, of that town.
On Missing Sedimentary Formations, from Suspension or Removal of Deposits
Authors: Bigsby J. J. 
Published: October 2009

Conclusion
Missing formations are among the several consequences of emergence and immersion, themselves the effects of one of the great cosmic agencies—oscillation of level—which may be gradual or paroxysmal, through all the degrees of velocity and energy.

Oscillation is, in a sense, universal in time and place; but, apparently, its action is irregular. While its influence is felt in most places, as well in the interior of continents as in the ocean depths, it is most easily detected near great waters; and there seem to be both great and small breadths of country which are at least places of
comparative
rest. The most conspicuous of these are the axial lines of Scandinavia and the South Seas; but Egypt, parts of the Danubian Valley, of Borneo, and Venice (E. de Beaumont) all seem to have been long stationary. Oscillation is the result of a power which operates from beneath through all existing groups of strata. It necessitates and facilitates the emigration of animals and plants, kills or multiplies life, driving it far and wide in search of proper pressure, food, shelter, and such like. Great elevation conduces to variety in life, and great depression extinguishes the higher forms of life.
On the Geology of Arisaig, Nova Scotia
Authors: Honeyman D. 
Published: October 2009

Conclusion
I have thus directed attention to the results of a detailed examination of the Silurian strata of Arisaig. This being the undoubted type of a very considerable proportion of our Nova-Scotian Silurian system, and bearing so striking a resemblance, as regards its fauna, to the British Upper Silurian, is a sufficient reason for so directing attention to the subject.
The conclusion thus arrived at is, that the members of the series are respectively the approximate equivalents of the Mayhill Sandstone, Lower Ludlow, Aymestry Limestone, and Upper Ludlow. Mr.Salter suggested to me the propriety of distinguishing the respective members of our series by local names. I have not been able to act on the suggestion, on account of the mode of distribution of the several members of the group. I have therefore distinguished them as Arisaig A, B, B′, C, and D. I have not yet attempted to measure the entire thickness of the several strata. Supposing Dr. Dawson's estimate of the thickness of the groups B′, C, D to be correct, although I consider it much below the reality, we have of them about 500 feet; I found the thickness of B 170 feet, and of A 200 feet; total, 870 feet.
Facts and Observations connected with the Earthquake which occured in England on the morning of the 6th of October, 1863
Authors: Austin Thomas 
Published: October 2009

Earthquakes in the British Isles, though not quite such rare events as generally supposed, usually attract but little notice, but that which shook the country and alarmed the people on the 6th of October 1863, from its greater amount of violence, has aroused attention to the subject.
The disturbance may be defined as extending from a point in St. George's Channel 40 or 50 miles to the north-west of Pembrokeshire (it was felt by the captains and crews of more than one vessel when off the Welsh coast), to its eastern limit in Yorkshire, though there is some doubt if it extended quite so far in an easterly or northerly direction. It was certainly not felt at Scarborough in Yorkshire, nor at Ashford in Kent; but it was felt at Gad's Hill, near Rochester, which may therefore be considered as its eastern limit in the southern counties. The northern limit was not much beyond Clay Cross, near Chesterfield.
On the Rhætic Beds and White Lias of Western and Central Somerset; and on the Discovery of a new Fossil Mammal in the Grey Marlstones beneath the Bone-bed
Authors: Dawkins W. Boyd 
Published: October 2009

In the year 1861 I spent some time in examining the interval between the Red Marls and the Upper Lias in Central and Western Somerset, taking, in the course of my examination, upwards of seventy sections. The results of this exploration, so far as relates to the Rhætic beds and the White Lias, are embodied in the following paper.
The suites of fossils collected, and numbered on the spot, have been examined by my friend Mr. Etheridge, F.G.S., without whose able assistance and corrections I should have felt diffident in my own determination of the Invertebrata.
On the Carboniferous Rocks of the Valley of Kashmere
Authors: Godwin-Austen H. 
Published: October 2009

The district or Pergunah of Vihi is situated on the right bank of the Jhelum, above Srinagar, and is bounded on the N.W. by Zebanwan (8813 feet), on the S.E. by Wasterwan.
The rough panoramic sketch (fig. 2) of the hills which surround this valley, as seen from the line of the river looking east, indicate the positions of the several places at which the following sections were taken. The distance from Zéwan to Reshpur is about 8 miles. The level plain consists of the lacustrine and alluvial deposits of the Kashmere valley, through which the streams from the hills have cut deep courses. The Jhelum flows between high banks of the same formation.
Everywhere, both in Kashmere and Thibet, a Palæozoic series underlies the Mesozoic formations. The age of the Palæozoic rocks is that of the Carboniferous series of Europe, but as yet fossils have not occurred to enable me to distinguish any formations of older date. As, however, Lower Silurian fossils from the Khyber Hills were found by Dr. Falconer in the gravel of the Cabul River, as also by Colonel Strachey on the Niti Pass, the great masses of slaty and metamorphosed rocks, which in this part of the Himalayan chain underlie the Carboniferous beds, may be referred to a Lower Palæozoic series.
The Carboniferous formation may be traced all along the range of mountains on the north side of the Kashmere valley, where, in conjunction with Dr. Vercher, I met with its characteristic fossils in great
On the so-called “Eozoonal Rock”
Authors: King William , Rowney T. H. 
Published: October 2009

Summary
Although zealous advocates at one time for the organic origin of “eozoonal” Ophite, we now, after a prolonged investigation, and after, as we believe, leaving no point unnoticed, feel ourselves under the necessity of totally relinquishing that opinion.

It has been seen (1) that the “chamber-casts” or granules of serpentine are more or less simulated by chondrodite, coccolite, pargasite, &c., also by the botryoidal configurations common in Permian Magnesian Limestone; (2) that the “intermediate skeleton” is closely represented, both in chemical composition and other conditions, by the matrix of the above and other minerals; (3) that the “proper wall” is structurally identical with the asbestiform layer which frequently invests the grains of chondrodite—that, instead of belonging to the skeleton, as must be the case on the eozoonal view, it is altogether independent of that part, and forms, on the contrary, an integral portion of the serpentine constituting the “chamber-casts,” under the allomorphic form of chrysotile—and that perfectly genuine specimens of it, completely simulating
casts
of separated nummuline tubules, occur in true fissures of the serpentine-granules; (4) that the “canal-system” is analogous to the imbedded crystallizations of native silver and other similarly conditioned minerals, also to the coralloids imbedded in Permian Magnesian Limestone—that its typical Grenville form occurs as metaxite, a chemically identical mineral imbedded in saccharoidal calcite; (5) that the type examples of “casts of stolon-passages” are isolated crystals apparently of pyrosclerite. Furthermore, considering that there has been a complete failure to explain the characters of the so-called internal casts of the “pseudopodial tubules” and other “passages” on the hypothesis of ordinary mechanical or chemical infiltration, also bearing in mind the significant fact that the “intermediate skeleton,” in Irish and other varieties of “eozoonal rock,” contains modified examples of the “definite shapes” more or less resembling the crystalline aggregations and prismatic lumps in primary saccharoidal marbles—that “eozoonal” structure is only found in metamorphic rocks belonging to widely separated geological systems, never in their unaltered sedimentary deposits,—taking all these points into consideration, also the arguments and other evidences contained in the present memoir, we feel the conclusion to be fully established, that every one of the specialities which have been diagnosed for “
Eozoon Canadense
” is solely and purely of crystalline origin: in short, we hold, without the least reservation, that, from every available standing point—foraminiferal, mineralogical, chemical, and geological—the opposite view has been shown to be utterly untenable.
Remarks on the Copper-mines of the State of Michigan
Authors: Bauerman Hilary 
Published: October 2009

The remarks contained in the following pages are the results of a general examination of the mines of Keweenau Point, made during the summer of 1865; and although the subject is not a new one, having been elaborately treated by Professor Whitney in two different works, and having received subsequent notices from Messrs. Rivot, Borie, and others, still the progress of mining enterprise has opened up some new features which have not as yet received any notice, and may be of interest to the Society.
The copper-mining district of Michigan is situated in the upper peninsula, or north-western portion of that State, forming a narrow belt of country about 140 miles in length, extending in a north-easterly and easterly direction, from the boundary of the State of Wisconsin to the end of Keweenau Point, the promontory of which projects into Lake Superior on the southern shore, about midway between Fond du Lac and the outlet of the lake at Sault S. Marie.
2. Structure of the District.—The rocks of the district consist of coarse sandstones and conglomerates, occupying either shore, with a central mass of trappean rocks, which forms the mineral range proper. The sandstones on the eastern side have a south-easterly dip, while the traps, which axe well stratified, and include several conformable beds of conglomerate, together with the overlying sandstones and conglomerates of the western and northern shores of Keweenau Point, dip towards the north and north-west, or generally at right angles to the trend of the land.
On the Metamorphic and Fossiliferous Rocks of the county of Galway
Authors: Harkness R. 
Published: October 2009

The portion of the county of Galway which lies between Killery Harbour on the north and Galway Bay on the south, includes Connemara and Joyce's country, one of the wildest and most mountainous districts of Ireland.
A section of the geology of this district is given in Sir Richard Griffith's Geological Map of Ireland; and the rocks of the country have been generally alluded to by Sir Roderick I. Murchison in the last edition of ‘Siluria.’
The rugged Connemara district is for the most part made up of metamorphic rocks, among which patches of granite occur; and this latter rock is found occupying a considerable area on the south of the metamorphic series, and extending to the northern boundary of Galway Bay. It also constitutes the rocky and moory country known as Moycullen, which lies on the west side of Lough Corrib.
The metamorphic rocks, as they are seen on the northern margin of the granitic area, consist of gneissose strata, which strike east and west, and which, although much contorted, have a prevailing southerly dip, or incline towards the granitic area. On their northernside rocks occurs a band of hmestone, which can be traced westwards from a few miles west of Oughterard, on the shores of Lough Corrib, for a considerable distance, as quarries of it are seen near the road leading from Oughterard to Clifden. One of these appears near where the Maame Road leaves the Clifden Road, at a spot called Butler's Lodge; and here the limestone
A Description of some remarkable “Heaves” or Throws in Penhalls Mine
Authors: Pike J. W. 
Published: October 2009

This mine is situated in the parish of St. Agnes, in the county of Cornwall, and stands on the sea-coast, three or four hundred yards from the edge of a bold precipitous cliff rising to a height of 300 feet above the sea-level.
Pryce, in his valuable old book ‘Mineralogia Cornubiensis,’ and Carne and Hawkins in papers read some forty years ago before the Royal Cornwall Geological Society, together with many other writers, refer to the heaves of the celebrated Pink lode, which is now a part of Penhalls Mine.
A paper was also read in 1815 before this Society, by Mr. John Williams, entitled “Account of some Remarkable Disturbances in the Veins of the Mine called Huel Peever,” the appearance of the lodes in which mine present the nearest approach to the dislocations in the Penhalls district.
The nature of the ground or “country” is a light-grey, distinctly stratified “killas” (the clay-slate of many geological writers, though not a cleaved rock) with a pretty regular dip towards the north of from 20° to 25°.
In the.immediate neighbourhood of the workings the ground is traversed by:—
1. Four or five tin-lodes, varying from 4 feet to a few inches in width, dipping north at about the same angle as the killas, and composed of the oxide of tin, with a little iron and copper pyrites in the middle,—the walls or outsides, locally called eapel, being a hard grey killas with quartz and schorl. The only distinction between the different lodes
On some Flint Implements lately found in the Valley of the Little Ouse River, near Thetford
Authors: Flower J. W. 
Published: October 2009

Abstract
The sands and flint-gravel on the right bank of the river Ouse at Thetford form a terrace 8 to 10 yards above the river, and about 40 yards distant from it. At a spot called Red Hill a large number of flint implements have lately been obtained from this gravel, at from 12 to 15 feet below the surface, and within a foot or less of the chalk on which the gravel rests; and some were found in the same gravel filling pot-holes in the chalk.
The author pointed out the exact correspondence, as regards geological position and relations, between the Thetford gravels and the flint-implement-bearing beds of Amiens, Abbeville, Fisherton, Icklingham, Hoxne, &c. He further noticed the close resemblance which these implements and some others discovered in England bear to those of the valley of the Somme; and concluded by expressing his dissent from Mr. Prestwich's conclusions, and stating his own views on their mode of accumulation, remarking that, in his opinion, these implements were manufactured prior to the severance of this island from the continent.
On the Discovery of new Gold-deposits in the District of Esmeraldas, Ecuador
Authors: Neale Edward St. John 
Published: October 2009

Within the last few weeks unworked and hitherto unknown gold-deposits have been discovered in the district of Esmeraldas; and I am informed by the President, who has received specimens of the gold of a very pure quality, that it is the intention of the Government to send a scientific Commission, at the head of which will be Dr. Jameson, a British subject who has been many years in Quito, to report upon the probable yield of the gold-district.
Should this survey prove satisfactory, as anticipated, I am informed that the Government of this Republic will be prepared to enter into engagements with foreign speculators and capitalists.
On the Glacial and Postglacial Structure of Lincolnshire and South-East Yorkshire
Authors: Wood S. V. , Rome J. L. 
Published: October 2009

Abstract
The features of Yorkshire and North-east Lincolnshire having distinctive characters from those of Central and South Lincolnshire, the authors describe the two areas separately. In the former, their coast-sections exhibit the Glacial clay separated into two portions: of these the lower, which they identify with the ordinary (or upper) Glacial clay of the South, contains abundant chalk débris; but the upper or purple portion (which was in places divided from the lower by sand and gravel beds) contains no chalk in the upper, and but little in the lower part of it, the place of the chalk being taken by fragments of Palæozoic rocks. The latter of these clays alone extends over the Wold-top at Speeton, and alone occupies the valley along the northern Wold-foot, and so away northwards to Scarborough and the Tees-mouth, from which the authors infer that the north of England did not subside beneath the glacial sea until after the south had been submerged. The so-called Bridlington “Crag” is shown to be an intercalated bed in this purple clay. Both these clays are shown to be denuded, and their denuded edges to be everywhere covered by a much thinner Boulder-clay, that of Hessle, which wraps Holderness like a cloth, extending to altitudes of 150 feet, and running down the east of Lincolnshire to the Fen-border. This Postglacial Boulder-clay of Hessle is again cut through, and in those places covered by posterior beds of gravel, one of which (at Hornsea) contains fluviatile shells. At Hull this clay supports a forest, which is now submerged 33 feet below the Humber,—the same submerged forest also occurring at Grimsby. The authors regard the position of the sea during the Postglacial period as having been principally on the west of the Yorkshire and North Lincolnshire Wold until the formation of the gravel-troughs cutting through the Hessle clay, and that its present position was connected with a recent westerly elevation and easterly depression.
The Glacial clay of Central and South Lincolnshire belongs to the chalky portion, from which all the superior or purple part of the formation has been denuded; and the valleys of Central Lincolnshire are shown to be cut out of the Cretaceous series and Glacial clay as a common bed, the hills formed of the clay rising to elevations equal to the Wold in that part.
The Glacial clay of both areas is shown to be denuded westwards, and the denuded edges occupied with sands and gravels termed by the authors denudation-beds.
Notice of the Hessle Drift, as it appeared in Sections above Forty Years since
Authors: Phillips John 
Published: October 2009

T
he
progress of modern research has brought before us, on a great scale and under various aspects, a subject which, until the series of strata began to be studied by W. Smith, had literally no place in British geology. By that observer, first of all men, the “superficial deposits,” as they were called, were separated from the “regular strata,” and referred to a different and more tumultuous origin. Dr. Buckland popularized this idea, and, under the title of “diluvial” deposits, presented a great number of important observations relating to the final operations on our land of the waters of the sea, followed by river-floods and ordinary atmospheric action*.

Modern research has convinced us that, instead of that diluvial accumulation being the work of one transitory and confused disturbance of the level of sea and land, there were successions of drifted deposits, under different conditions, having unequal distributions, and peculiar local directions. We have not merely translated the antique “diluvial” into the modern “drift;” the abnormal cataclysm has become an intelligible series of local sea-actions and limited displacements of land; the crisis has become a period: Preglacial and Postglacial eras are marked in time, and characterized by successive races of animal and vegetable residents.
Those who, like myself, had to struggle with the Boulder-clays and northern drift more than forty years ago, without the aid of glaciers and icebergs, and with no clear theory of the changes of level of land or sea, were apt to leave out of our local