bluuebunny/crossref_metadata_2025_split huggingface dataset:
On the Mode of Occurrence and Derivation of Beds of Drifted Coal near Corwen, North Wales
Authors: Mackintosh D. 
Published: October 2009

A
bout
four years ago the late Mr. Jones, of Angharad, directed my attention to the remarkable fact that beds of drifted coal are to be found in sand and gravel around Corwen, at a great distance from any
known
coal
in situ
. The belief that this coal was of
local
derivation had led to unsuccessful mining operations in the Wenlock rocks of the neighbourhood.

Positions occupied by the Drifted Coal.
-Around Corwen the lowest drift consist of yellowish (occasionally bluish) clay, irregularly alternating with beds of coarse gravel. Many large boulders are to near its summit. The former are often rounded and local; the latter subungular, or angular, and erratic (chiefly from the Arenig hills to the west). Above this drift there is a deposit of clean sand and fine gravel, which, in other parts of the Dee valley, often graduates into very coarse gravel with boulders. In many places around Corwen this deposit is covered by an irregular kind of brick clay. The coal is generally found in the sand and fine gravel. Immediately to the east of the mountain-limestone quarry (about a mile and a half to the west of Corwen), a roadside section shows fine gravel and sand with streaks of decomposed coal. In the Dee valley, some	distance east of Corwen, and not far from Carrog station, consideraqble quantities of coal may be found in
many
other places around Corwen; but the principal instance occurs to the north of the town, and near to where the Denbigh
On the Permians of the North-East of England (at their Southern Margin) and their Relations to the under- and overlying Formations
Authors: Wilson E. 
Published: October 2009

T
he
main object of the present communication is to bring under the notice of the Society a capital section (see figure), exposed by the Great Northern Company's Derbyshire Extension line, the peculiar interest of which is that it exhibits the whole series of the Permians of this district, and their relations to the under- and over-lying formations.

The section begins at the Hempshill cutting near Cinderhill, and ends at Kimberley West station. It bears, roughly speaking, north-west for a mile, and then gradually curves round and bears south-west, and throughout corresponds approximately in direction, with the dip of the red rocks exposed.
Going west we get the following succession of strata :—

Characteristic mottled and obliquely laminated
Lower Bunter
sandstone (ƒ
1
), about 30 feet exposed, including its lower brecciated portion. The breccia, which is alternately sandy, marly, and calcareous, expands near fault No. 1, to 5 feet, including sandy interstratifications, but locally disappears on the east, where it becomes very difficult to separate the Lower Bunter from the next underlying deposit.

The breccia contains semiangular green, blue, and purple slates, more or less rounded grits, quartzites, quartz-breccia, and numerous white and discoloured slabs and nodular ,balls of fossiliferous Carboniferous-Limestone chert. Seeing that the yellow chert-balls are the chief eentres of cementation, and are deeply indented by the adhering pebbles, it appears probable that their conversion into chert took place after being deposited in the breccia. Beneath the breccia comes a series of
comparatively
hard red-and-yellow-mottled and soft grey
sandstones
, becoming,
On the Relation of the Upper Carboniferous Strata of Shropshire and Denbighshire to Beds usually described as Permian
Authors: Davies D. C. 
Published: October 2009

The strata I am about to describe occur in the north-west corner of Shropshire and in the adjacent south-east corner of Denbighshire. They are cut through by the rivers Ceiriog and Dee; and a good section of a portion of them may be seen along the banks of the Dee, from the mouth of the Ceiriog downwards towards Erbistock.
I directed attention to these beds in the year 1873. Since that time I have been engaged constantly in colliery operations in the district and strata then referred to; and I propose in this communication to narrate the results of my observations during the interval, and also to inquire into the relative position of these strata with others which are usually described as Permian.
The order of the beds and their relation to the underlying Coal-measures will be understood by a reference to the horizontal section which accompanies this paper (Pl. I. B). This section extends from the Brynkinallt Colliery, near Chirk, on the west, past the new sinkings of the Ifton-Rhyn Collieries on the east. The line of the section was carefully surveyed by Mr. F. B. Henderson, F.G.S.; and the geological details are supplied by the section of the Brynkinallt Colliery on the west, the Hafod-y-bwch pit-section on the north, the recent sinkings and borings at Ifton on the east, taken together with the outcrops of the strata which are visible along the line of the section.
Section no. 11, of the Diagram of Sections (Pl. I.), gives in
On the Chesil Beach, Dorsetshire, and Cahore Shingle Beach, County Wexford
Authors: Kinahan G. Henry 
Published: October 2009

S
-beaches
are common around our coast lines; but none seem to have attracted so much attention as the Chesil Beach on the north-east margin of Lyme Bay, Dorsetshire. This is probably due to the circumstance of the beach being situated on a much resorted-to coast, its great length, and the peculiar assortment of the fragments composing the accumulation, these being arranged as if they had been passed through a series of sieves of gradually decreasing coarseness. This last particular has even attracted the attention of the fishermen, who say they can tell, on the darkest night, at what part of this beach they have landed, by the size of the pebbles at the place.

The latest published paper on the Chesil Beach is that of Prof. Prestwich, read before the Institution of Civil Engineers, February 2nd, 1875; and from the discussion at the reading of it it is evident that opinions still differ much on the subject. This has emboldened the writer of this paper to come forward, more especially as no previous writer seems to have taken into consideration the special effects that the “flow” of the tide, which is most accelerated at the nodal or hinge-line in the English Channel, must have on the east shore of Lyme Bay—also because he has specially studied Cahore shingle beach, co. Wexford, which in many points is analogous to the Chesil Beach.

Tides in the English Channel and Irish Sea.

At Portland Bill on the English Channel, and at Cahore Point
At Portland Bill on the English Channel, and at Cahore Point on
On the Echinodermata of the Australian Cainozoic (Tertiary) Deposits
Authors: Duncan P. Martin 
Published: October 2009

I.
Introduction
.

W
hen
the Cainozoic or so-called Tertiary deposits of Australia were found to be fossiliferous in some parts, great interest was excited respecting the possibility of the Echini being able to afford satisfactory evidence regarding the geological age of the strata in relation to the European types. It was hoped that the fossils of this great group would present some of the anomalies which characterize almost every class of organism found in the great distributional province; and it was thought to be probable that relics of very ancient forms would be discovered. But the number of species of Echini which were found in the marine deposits beneath the older basalt was small; and at the commencement of their study the amount of knowledge of the living Echinodermal fauna of the coasts and neighbouring seas was not great; consequently disappointment ensued. Year by year more specimens of the fossil Echini have been discovered, and careful collecting has produced many with their ornamentation wonderfully preserved; and, contemporaneously, the labours of Gray, Agassiz, and others, increased our knowledge of the recent Australian fauna.

Of necessity, therefore, the literature of the fossil Echini of Australia is scanty; and those palæontologists who have contributed to it have only paid attention to the relation of the forms to those of other geological ages, and neglected to consider the affinities with the existing fauna.
The principal contribution to the Echini of the Australian Tertiaries is that of Laube, “Ueber einige fossile Echiniden von den Murray cliffs
On the Ice-Fjords of North Greenland, and on the Formation of Fjords, Lakes, and Cirques in Norway and Greenland
Authors: Helland Amund 
Published: October 2009

The observations recorded in the following paper were made during two years of travel among the fjords and mountains of Norway, and during a visit to the ice-fjords of North Greenland in the summer of 1875. These travels were almost wholly undertaken with the view of seeing how far these countries confirmed tho views entertained by Prof. Ramsay and other English and American geologists as to the origin of fjords and lakes.
We will first examine the fjords of North Greenland, ascend to the Inland Ice which covers the whole country, so far as is known, then visit the glaciers which descend into the fjords, measure their rate of flow, and examine the other phenomena which they present. As these are, in many respects, of the greatest importance to geology in general, they shall be described more fully than is necessary for explaining the formation of fjords and lakes.
The tract over which I travelled in North Greenland extends from the colony of Egedesminde (60° 42′ 9″ N. lat., according to Nordenskjöld) to the fjord of Kangerdlugssuak (about 71° 15′ N. lat.) in the district of the Colony of Umanak.
Of ghe great ice-fjords which produce bergs of large dimensions, the following were visited, viz. those of Jakobakavn and Torsukatak; of the smaller, which produce only little bergs, those of Sarkardlek, of Alangordlek (in the district of Christianshaab), and of Kangerdlugssuak. The ice-filled valley of Ilartdlek, by Pakitsok, was traversed, and the Inland Ice here ascended. A large number of
Description of a new Species of
Araucarites
from the Coralline Oolite of Malton
Authors: Carruthers W. 
Published: October 2009

A
raucarites
H
udlestoni
, Carruthers, sp. nov.

Cone oblong-ovate, supported on a thick branch, which is clothed with leaves to the base of the cone. Scales numerous, supported on a thick axis. Scales small, wingless, with a well-marked lepidium or upper scale. Seed small, oval, borne at the base of the scale.
The two cones, found by Mr. Hudleston, are mature, and each scale, except those imperfectly developed at the apex and base of the cone, bears a seed. The cones are small, being 3¾ inches long by 2½ inches broad. The scales also are small in proportion to the thickness of the axis. The axis must have been the first part of the organism to decay, as the matrix in which the cones were imbedded was yet unsolidified, and has been pressed into the cavities left by the decayed axes. The scales, however, persisted until the rock became indurated; and when this decay took place, the cavities were filled in with crystalline calcite, which now represents the external form of the scales and seeds, often with singalar minuteness.
The fragment of branch which still adheres to one of the cones, exhibits the bases of the leaves, which were of considerable size and thickness, as is shown by the transverse section of the calcite cast.

The characters which I have described as found in the scales show that this
Araucaria
belonged to the
Colymbea
section of the genus, now represented by two species in
On certain Ancient Devitrified Pitchstones and Perlites from the Lower Silurian District of Shropshire
Authors: Allport S. 
Published: October 2009

T
he
principal object of the present communication is twofold:—in the first place, to bring under the notice of the Society the occurrence in Shropshire of an extremely interesting series of ancient vitreous and semivitreous lavas, with their associated agglomerates and ashes; and in the second, to show, from an examination of their structure and composition, that originally they were absolutely identical with some of the glassy volcanic rocks ejected during the most recent geological periods.

In a previous paper (published in vol. xxx. pp. 529-567, of the Quarterly Journal) I arrived at the same result as to the identity of ancient and recent volcanic products, from an investigation restricted to the basic group of rocks; and I am now enabled to show that those of the acid type afford equally strong evidence in the same direction.
The discovery of several highly characteristic varieties of glassy rocks and volcanic ashes of Palæozoic age is, I think, a matter of considerable interest from a petrological point of view, more especially as their mode of occurrence and their relations to the surrounding strata afford the clearest evidence that the geological structure of a part of the district in which they occur has hitherto been misunderstood.
On Sheet 61 of the Geological-Survey map a band of “greenstone” is represented as constituting the axis of the somewhat irregular narrow ridge of which Ercal Hill and the Wrekin form the greater portion. It commences half a mile south of Wellington, and extends in a south-westerly direction
On the Remains of
Hypsodon, Portheus
, and
Ichthyodectes
from British Cretaceous Strata, with Descriptions of new Species
Authors: Newton E. Tulley 
Published: October 2009

D
r. Mantell
in the year 1822, in his ‘Geology of Sussex,’ described and figured certain fossil bones, obtained from the Upper Chalk near Lewes, as the parts of an unknown fish (p. 241, pl. 42). These remains, which it appears were all obtained from one block of chalk, consisted of an upper jaw with teeth, including the maxilla and præmaxilla, with a vertebra and an indeterminable bone. The maxilla, which is there referred to as a lower jaw, is said to “contain twelve smooth pointed teeth. These are slightly convex, very brittle, and possess a glossy surface. The three anterior ones are gently curved; their fangs are hollow, and placed in sockets that extend almost to the base of the jaw. The nine posterior teeth are of a lanceolate form, and probably destitute of fangs, appearing as if attached to the jaw by anchylosis.”

The appearances which led Dr. Mantell to think the posterior teeth differed from the anterior ones, must, I think, have been due to the condition of the specimen, the teeth of which are somewhat obscured by the matrix; for, after a comparison with other specimens, I see no good reason for thinking that the teeth of this jaw differ otherwise than in size.
The præmaxilla, which has the remains of “five tusks or defences,” is broken away from the maxilla.

Prof. Agassiz, in the year 1843 (‘Poissons Fossiles’), without definitely characterizing his genus
Hypsodon
, alludes to Dr. Mantell's description, and then proceeds to describe the fossil
Remarks on the Coal-bearing Deposits near Erekli (the ancient Heraclea Pontica, Bithynia)
Authors: Spratt T. 
Published: October 2009

Towards the end of March 1854, after the combined fleets of England and France had entered the Black Sea, as coal was known to be procured by the Turkish Government from the south coast, near Erekli (the ancient Heraclea), I was ordered to proceed there, and examine and report upon its quality and fitness for the use of war-steamers; for although two or three cargoes of the coal were seen at Constantinople by some naval engineers, the quality appeared to be so inferior as coal (from being so mixed with slate and rubbish), that a general opinion prevailed that it was only a better quality of lignite than that procured from the Tertiary deposits of the Sea of Marmora and the Archipelago.
It was therefore of first importance to ascertain the age of the Erekli coal-beds, as well as the quantity that could be procured from them with sufficient economy and of sufficiently good quality for the use of our war-ships for steaming at high speeds.
I could obtain no fragment of a fossil from the coal at Constantinople that I examined, nor any information regarding the deposits associated with them; for, although M. Tchihatcheff had shown that rocks of the Devonian age existed, no mention was made of these coal-deposits or of any Carboniferous strata in the neighbourhood, in his valuable work on Asia Minor, published in 1853. I now find, however, that M. Schlehan had, in the ‘Zeitschrift der deutschen geologischen Gescllschaft’ for 1852, given a full description
On the Mammal-fauna of the Caves of Creswell Crags
Authors: Dawkins W. Boyd 
Published: October 2009

T
he
exploration of the caves of Creswell Crags carried on by the Rev. J. M. Mello, F.G.S., in 1875, and brought before the Society in that and the following year, was finally concluded last summer; and the results have been handed over to me, by the Committee, for description—a task of no little difficulty, from the vast numbers of the fossil remains which have been discovered. The results are of considerable importance, not merely because they confirm the conclusions which were arrived at from the previous explorations, but because they add new facts to the history of palæolithic man in Britain. In dealing with these the Robin-Hood Cave will be taken first; and then I shall check the evidence which it offers by that furnished by the cavern on the other side of the ravine of Creswell Crags known as the Church Hole. It must, however be remarked that the history of both these caverns is rendered imperfect from the promiscuous diggings carried on by unauthorized persons, the results of which have not been brought before the Committee.

II The Robin-Hood Cave.
A. Distribution of Species in the Lower and Middle Strata.
In the description of the remains from the Robin-Hood Cave in this Journal (August 1876, p. 245), attention was drawn to the fact that the cave was inhabited by hyaenas during the time of the deposition of the red sand below, the cave-earth, and the breccia above, and that no traces of man were found below the cave-earth.
On a new Area of Upper Cambrian Rocks in South Shropshire, with a Description of a new Fauna
Authors: Callaway Charles 
Published: October 2009

In March 1874 I communicated to this Society a paper entitled, “On a Tremadoc area near the Wrekin in South Shropshire, with description of a new Fauna,” which was published in abstract in the Society's Journal, vol. xxx. p. 196.

In that paper I described certain shales, commonly supposed to be Caradoc, which I had examined at Shineton, two miles S.S.W. of the Wrekin. In these shales I had found
Conocoryphe, Lingulella
, and other fossils of a Cambrian type; and from this and other evidence I had concluded the beds were of Tremadoc age. My views, however, were not accepted by the Fellows present at the reading of my paper, on account of the alleged imperfection of the fossil evidence; and, as I was at the time absent in America, I had no opportunity of defending my position. Since my return home I have collected more abundant and satisfactory evidence, both geological and palæontological, which I venture to think will establish my original conclusions. I have also made out some additional points of interest in the geology of the neighbourhood of the Wrekin.

Previous Information.
Sir R. Murchison has described the area under examination, from the Wrekin on the north-east to the May-Hill Sandstone at Kenley on the south-west, as composed of strata of Caradoc age, the Wrekin itself being an igneous outburst altering the Caradoc sandstone on its flanks into quartzite.
The Geological Survey has followed Murchison, but has included, under the name of “quartzite,” certain sandstones in which
Further Notes on the Diamond-fields of South Africa, with Observations on the Gold-fields and Cobalt-mine in the Transvaal
Authors: Dunn E. J. 
Published: October 2009

A
visit
made to the Diamond-fields in December 1874 enables me to make some additions to, and corrections of, my previous paper, read before the Geological Society in 1873.

At De Beer's, mining-operations have clearly established the fact that the “pipes” are more recent than the sheets of dolerite and other intrusive rocks surrounding them; for on the east side of the mine the rudely tabular dolerite, forming the wall of the “pipe,” is tilted at an angle of about 40°(fig. 7.) Included masses and nodules of dolerite occurring in all the pipes hitherto opened, help to confirm this view.
In no case are the “pipes” traversed by dykes of hard rock; and the only instance of dykes of any description intersecting the material forming the “pipes” is at De Beer's, where, at a depth of 100 feet from the surface, and at the east side of the mine, long, narrow, dyke-like masses, from 2 to 5 feet wide, vertically cut through the soft diamond-bearing rock; one having the latter width runs for about two hundred yards in a straight line. These dykes(?) are lighter in colour and somewhat harder than the bounding rock, but earthy in texture and so much altered that specimens sent to the British Museum were undeterminable, though evidently quite distinct from the surrounding soft rock. The general opinion of the miners who have these dykes(?) cutting through their claims, is that they contain no diamonds.
The wall of De Beer's Mine, except on the north
Notes on the Chemical Composition of some of the Rocks of the Lizard District
Authors: Hudleston W. H. 
Published: October 2009

These rocks may be roughly divided into four principal groups (without enumerating others of less importance), viz.:—

1.
The Serpentines.

2.
The “Greenstones” in the Serpentine.

3.
The Hornblende Schists.

4.
The Gabbros.

Features in common
.—In all specimens of the above rocks examined by me, alkalies are extremely scarce, if not altogether absent in most cases. They are all basic, rarely containing as much as 50 per cent. of silica.

Differences
.—Chemically they divide themselves into two groups:—Group A (poor in lime and alumina) includes the serpentines; Group B (rich in lime and alumina) includes the “greenstones,” hornblende schists and gabbros—rocks which, however much they may differ in appearance, have considerable resemblance in their fundamental constitution.

Some of the Rocks of the Lizard District.
Group A. The Serpentines.
These rocks, as usual, present an infinite variety as regards external appearance; but there is considerable resemblance in their chemical composition. A specimen has been selected for careful analysis.

Black Serpentine from “near Cadgwith.”
—Black to greenish black, opaque; fracture splintery; charged with numerous crystals of a highly cleavable mineral of a pale brass-eolour and metallic lustre. Sp. gr. of the mass 2·587. Freed as far as possible from the crystals, the black matrix yields a greenish-grey powder, which adheres in considerable quantity to the magnet. Composition:—

Two or three kinds of crystalline fragments are noticeable in the undecomposed residue; one is prebably enstatite.
As the amount undeeomposed is so small, the quantity of unaltered augite, diallage