bluuebunny/crossref_metadata_2025_split huggingface dataset:
The Geology of the Country around Fishguard, Pembrokeshire
Authors: Reed F. R. Cowper 
Published: October 2009

On the northern coast of Pembrokeshire there lies a district of considerable area which has not been geologically investigated since the completion of the Government Survey under De la Beche in South Wales. The region adjoining that to be described in this paper has been made known to us in detail by the labours of Dr. Henry Hicks and others during the last few decades; and we may therefore claim a fairly complete acquaintance with the Archæan, Cambrian, and Ordovician rocks of South-west Pembrokeshire. North-east of a line running from Penclegyr Point on the coast inland to St. Elvis in the south, we have had, however, to confess comparative ignorance. The Geological Survey memoir on South Wales pays scant attention to this district, and relatively little information of importance can be obtained from any subsequent geological literature.
My object in visiting this tract of country was to determine the age of the volcanic series indicated on the Survey map near the coast, and to investigate the characters of both the contemporaneous and intrusive igneous rocks in the field and laboratory. To petrological questions, therefore, special attention has been paid.
The area with which this communication deals extends from Newport in the east to the western side of Strumble Head in the west, and lies north of a line drawn from Pwll Crochan to Cilgwyn, and passing through St. Nicholas and Llanllawer. This narrow strip of country, it will be noted, approximately coincides with the strike of the beds. (See Map,
Notes on the Chemical Composition of some Oceanic Deposits
Authors: Harrison J. B. , Jukes-Browne A. J. 
Published: October 2009

When describing in this Journal the raised and consolidated deep-sea oozes which occur in the island of Barbados, we experienced great difficulty in comparing our analyses of these deposits with those made by Dr. Brazier of the corresponding recent oozes. This was especially the case with the ‘red clays’ and, in a less degree, with the other deposits. In the paper above referred to we remarked that ‘if the Challenger samples of red clay which contained only small amounts of calcium carbonate and the samples of the Barbados argillaceous earths had been analysed by similar methods, a close resemblance in composition would have been found in them; and the differences would have been such only as would arise from the action of percolating water containing organic acids upon the Barbados deposits, from which the calcium carbonate and the iron peroxide present in a limonitic form would be leached out.’
We know that the analyses published in the ‘Challenger’ Report on Deep-Sea Deposits were made before Dr. Murray was placed in charge of the ‘Challenger’ Office and that he was fully aware of their shortcomings, as testified by his discussions of them in different parts of the Report. It is especially to be regretted that the analyses of the ‘red clays’ were not made on a more satisfactory plan, for the method employed by Dr. Brazier was not calculated to bring out the real mineralogical composition of these deposits.
Dr. Murray very kindly placed at our disposal a typical sample of
Notes on some Railway-cuttings near Keswick
Authors: Postlethwaite J. 
Published: October 2009

Several cuttings have recently been made on the Cockermouth, Keswick, and Penrith Railway, chiefly through drift, though some occur in the Skiddaw Slates, and in one case a diabase dyke (much decomposed) was met with. It is similar in character to a rock exposed about ¼ mile west of Troutbeck.
The Author describes the drifts as blue clay beneath, and brown clay above, and considers that these two clays were produced during two separate periods of glaciation, with no long interval between. In some places near Keswick water-borne gravel may be seen surmounted by blue clay; this gravel is considered by the Author to be of fluviatile origin. A section at Keswick Station is described; it is 130 yards in length, with a slight break in it, 50 yards of the western end being cut back 9 feet to the north. At the point where the break occurs, and for 17 yards eastward, some beds of current-borne materials take the place of the lower part of the blue clay. There is a bed of a very fine brown sediment 1 foot thick; above it is 2 feet of fine sand, and above that a bed of coarse gravel and pebbles, which is succeeded by blue clay of the usual type. The whole of these beds dip south-west, at an angle of about 9°.
The Author has searched both blue and brown clays diligently for shells, but hitherto without success.
The Chalky Clay of the Fenland and its Borders: its Constitution, Origin, Distribution, and Age
Authors: Howorth Henry H. 
Published: October 2009

The distribution of the Clay (so often termed Chalky Boulder Clay) is noticed, and it is stated that it is surrounded on all sides by country occupied by different deposits, being mainly separated from the sea on the east and north-east by sandy and pebbly materials, while on every other side it is clearly and sharply defined. The paucity of foreign stones is noted as compared with natives, and the similarity of the matrix of the Chalky Clay to the material of the older deposits of the neighbourhood. The Author maintains that the contents of the Clay indicate movement of material from west to east in some places, as shown by Jurassic fossils in the East Anglian Chalky Clay, and from east to west in others: in fact, that movement took place in sporadic lines diverging from the Wash and the Fens. He appeals to the amount of disintegration that has taken place to furnish the material for the Clay, the shape of the stones in the Clay, and the distribution of the Clay itself, as evidence against the action of land-ice or icebergs, maintaining that there is no evidence of submergence at the time the Clay was formed; and criticizes the attempts made to explain the formation of the Clay by water produced by the melting of ice.
The Author believes that the denudation of the Fen country which produced the great mass of the Chalky Clay with most of its boulders was coincident with and caused by the
On the Alteration of certain Basic Eruptive Rocks from Brent Tor, Devon
Authors: Rutley Frank 
Published: October 2009

Two microscopic sections of rocks occurring on the north side of Brent Tor were examined, and a cursory glance suggested at once the idea that they might originally have consisted to a greater or less extent of extremely vesicular basalt-glass. No unaltered vitreous matter, except perhaps mere traces, can now be detected in these specimens, the interest of which lies in the assemblage of alteration-products which they contain. A third section cut from a small chip collected at the southern side of the base of the Tor consists of a highly vesicular lava of a hyalopilitic character, which may be regarded as an amygdaloidal glassy basalt.
The Author gives a detailed account of the microscopic characters of the three sections, and discusses the history of the rocks, comparing them with Tertiary basic glass, and with the Devonian rocks of Cant Hill, which he described previously. He brings forward evidence in favour of the view that the original alteration of both the Brent Tor and Cant Hill rocks was palagonitic, and that while in the Brent Tor rocks the subsequent alteration of the palagonite into felsitic matter, magnetite, secondary felspar, epidote, and probably kaolin, and some serpentine and chlorite was complete, it was only partial in the case of the Cant Hill rocks. We may therefore assume that palagonite is not the ultimate phase of alteration in basic igneous rocks.
Discussion.
Gen. McMahoN enquired whether the Author had worked out in detail the chemical changes involved in the conversion of palagonite
A Delimitation of the Cenomanian:—being a Comparison of the Corresponding Beds in South-western England and Western France
Authors: Jukes-Browne A. J. , Hill William 
Published: October 2009

1. Historical Introduction.
The object of this paper is to compare the beds which form the lower part of the Upper Cretaceous series in those parts of Western France and Western England , which are nearest to one another. In England these beds are known by the names of Gault, Upper Greensand, and Lower Chalk; in France they are classed under d‘Orbigny‘s ‘Albien’ and ‘Cénomanien’ stages. It is well known that in both countries the deposits referable to these groups change their lithological character so greatly, in passing towards the west and south-west, that different observers have formed different opinions in their attempts to correlate one area with another. Further, no geologist has yet endeavoured to make a careful comparison of the French and English types; but it is only by such a comparison that the true stratigraphical position of d‘Orbigny‘s, Cénomanien stage can be determined, and that the limits of this stage in areas outside the typical Cénomanien district can be fixed.

The name ‘Cénomanien’ was introduced by d‘Orbigny in 1847 to designate the lower part of the series which he had previously called ‘Turonien,’ when he found that this lower portion contained a fauna, essentially distinct from that of the upper part. He then proposed to retain the name ‘Turonien’ for the upper part, and to adopt the name ‘Cénomanien’ for the lower part, taking the name from Le Mans, in the Sarthe, the
Cenomanum
of the Romans,and regarding that district as the typical area of his new
The British Silurian Species of
Acidaspis
Authors: Lake Philip 
Published: October 2009

The genus
Acidaspis
has been a peculiarly unfortunate one in Britain. Several of the specific names which are in common use are manuscript terms, or but little better; and the species to which they are applied have never been described. It is impossible, therefore, without access to standard collections, to determine to what forms the names refer. Even the species which have been described have in many cases been imperfectly figured, and the result is endless confusion. The common English trilobite,
A. coronata
, has received abroad no less than three names, all of them different from ours; while in England, on the other hand, the foreign name
A. crenata
is often applied to a species which is quite distinct from the original
A. crenata
, and which in fact has never yet been found out of Britain.

The disorder is worst among the Silurian forms, although these are much the most perfect. The Ordovician species are usually fragmentary, but the fragments have been fully described.
It is the object of the present paper to attempt to reduce the specific terminology to some sort of order, and to rescue the common manuscript names from the obscurity in which such terms tend to become involved after a lapse of time. Only the Silurian forms are here described; the Ordovician species have been left in the hope that better material may be forthcoming in the future.

Even the name of the genus itself is matter of controversy. Murchison employed the term
Acidaspis
in 1839
On the Llandovery and Associated Rocks of Conway (North Wales)
Authors: Elles G. L. , Wood E. M. R. 
Published: October 2009

I.
Introduction, and Description of Area
.

The Geological Survey Map (Sheet 78 N.E.) of the district lying immediately south of the town of Conway reveals an outcrop of Tarannon Shales, which is curious as regards its relation to the associated formations, since the Tarannon Shales are represented as being both underlain and overlain by rocks of Wenlock age. This circumstance led us to examine this special area; and our attention having already been directed to the occurrence of graptolitic shales below the Tarannons in other parts of Wales, we thought it' possible that they might also be present in the Conway district.
Our observations in that district have extended over a fairly wide region, including the greater part of the valley of the Afon Gyflin between Conway and Y–Ro; but the only area which we have mapped in anything like detail lies immediately south of the town of Conway itself, and occupies the hill opposite Conway Castle and the railway. This area is bounded on the east by the River Conway, and on the west by a fault (‘ boundary–fault,‚ as we term it in the following pages) which brings a calcareous grit of Bala age against Silurian beds.The northern limit of the area is formed by the Afon Gyffn, a‚ tributary stream of the River Conway, which it joins just below the Castle. The southern limit has been taken, for convenience, at the beginning of the dense woods belonging to Benarth Asylum. In other places higher up the valley,
The Tertiary Basalt–plateaux of North–western Europe
Authors: Geikie Archibald 
Published: October 2009

Introduction. Since the publication, seven years ago, of my memoir on ‘The History of Volcanic Action during the Tertiary Period in the British Isles’, I have continued the investigation of this subject. My researches in this interval have included a re-examination of various tracts in Mull, Rum, Reassay, and Skye; and numerous traverses in the last-named island, especially over areas which had not been previously described by any geologist; a detailed survey of Canna and its adjacent islets; an exploration of the Shiant Isles and other insular outliers of the Tertiary sills, and a visit St. Kilda for the purpose of accurately determining the relations of its two great, groups of igneous rocks. In two successive years I have prolonged my excursions into the Faroe Islands, where the phenomena of of our basaltic plateaux are reproduced on a colossal scale, and where the numerous fjords and sounds have laid bare the most stupendous range of geological sections. This extended series observations, while entirely confirming the main conclusions announced in my former memoir, has furnished many fresh and important illustrations of phenomena already described, and some new interesting additions to our knowledge of the volcanic history of Tertiary time over the North-west of Europe. I now lay before the Society an outline of the chief results which have thus been obtained.
As the literature of the subject was fully summarized in my former memoir, it need not be further referred to here. Such more recent papers as bear on any of
The Gypsum Deposits of Nottinghamshire and Derbyshire
Authors: Metcalfe A. T. 
Published: October 2009

Abstract
The gypsum deposits of these counties occur in the Upper Marls of the Keuper division of the Triassic system. The author describes their occurrence in thick nodular irregular beds, large spheroidal masses, and lenticular intercalations, and their association with satinspar, alabaster, selenite, and anhydrite.
On submerged Land-surfaces at Barry, Glamorganshire
Authors: Strahan A. 
Published: October 2009

Barry Island lies off the northern coast of the Bristol Channel, about 7 miles south-west of Cardiff. Until the year 1884 it was separated from the mainland by the tidal estuary of the Cadoxton River on its northern side, and on the east by a tract covered at high water, but in which the solid rock cropped up through the tidal' deposits at frequent intervals, the most conspicuous prominences being known as the Coston, Mark, Bendrick, and Black Rocks.
In the absence of evidence to the contrary we may assume that the course followed by the river at this time was its original course, for it falls into the general south-westerly direction of the rest of the valley. The numerous outcrops of rock, moreover, in the tidal area east of the island make it unlikely that there was an outlet here of sufficient depth to drain the marshes behind it.This tidal area seems to have been one of three low cots in the water-parting on the southern side of the Cadoxton Valley.One of these would separate the western part, or the Little Island, from the main part of Barry Island were it not for a ridge of blown sand; another occurs east of Hayes Farm, where, as shown by the Ordnance level 19 given on the map facing this page, the alluvial marsh of the Cadoxton River closely approaches the present coast. The third, presumably a trifle lower than either of the others, was submerged during thesubsidence of the land
Discovery of Mammalian Remains in the Old River-gravels of the Derwent near Derby.— Part II.
Authors: Deeley R. M. 
Published: October 2009

The deposits in and beneath which the mammalian remains were found occur on the inside edge of a gravel–terrace which covers a large area on the right side of the Derwent Valley below Derby. Its south–western boundary is more or less obscured by a variable thickness of unstratified, yellow, sandy clay containing pebbles. Masses of this pebbly deposit frequently penetrate 6 or 8 feet into the gravel, much as does the ‘trail’ of Southern England. At its inner edge the gravel terminates against rising ground, composed of Keuper Marl capped in places by Boulder Clay. The line of junction between the gravel and the Keuper commences on the south side of the breach made in the Derwent Valley escarpment by the Kedleston Brook. From here it skirts the lower portion of the Royal Infirmary grounds, crosses the railway near Osmaston Road, passes a few yards to the south–west of the section at Allenton, and then skirts the base of Chellaston Hill until the river–escarpment of the Trent, a mile north of Aston–on–Trent, is reached. Its north–eastern boundary is a continuous and steep escarpment about 18 feet above the modern alluvial plain of the Derwent.
This escarpment, starting near the Kedleston Brook breach, passes through the Midland Railway–station, and keeping on the north side of the London road, passes through Alvaston, Elvaston, and Aston, when it joins the corresponding escarpment of the Trent Valley.
This portion of the ground I have contoured, so as to show the exact relationship between the
The Geology of the Eastern Corner of Anglesey
Authors: Greenly Edward 
Published: October 2009

I. Introduction. The observations recorded in this paper were made during a detailed survey on the 6-inch scale, by myself, of a small portion of Anglesey. It is my intention to continue the mapping of the island on the same scale.
I should like to express my thanks to former workers upon Anglesey, all those with whom I have come into communication having expressed the warmest sympathy with my undertaking; and in particular to my former chief, Sir Archibald Geikie, and to Prof. Bonney, who have aided me very substantially by generous loans of slides and specimens. My friend and late colleague, Mr. Peach, has also, with his wonted goodness, looked over the graptolites and other fossils for me. Dr. G. J. Hinde and Prof. T. Rupert Jones have been so kind as to determine certain small organisms; and to Mr. G. J. Williams I am indebted for the photograph of the slates at Careg Onen.
II. Careg Onen Slates. The Carboniferous Limestone and Ordovician shales form the greater part of the cliffs about the cove of Careg Onen 2 (fig. 1), but near the western end of the beach we find, emerging from beneath the latter, a series of hard, greenish, fissile rocks dipping apparently- at very high angles (figs. 1, 2, 3). Careful examination, however, reveals indistinct planes of bedding, crossing the conspicuous divisional planes—which are really planes of cleavage—at various angles, and evidently much folded (fig. 4, p. 620). There are some lines of dark nodules following
Seismic Phenomena in the British Empire
Authors: de Montessus de Ballore M. F. 
Published: October 2009

I. Introductory. Without pretending to have discovered the primary cause of earthquakes, the author is firmly convinced that the plan which he has been elaborating for some years -will reduce the present chaos of seismological study to some sort of order, and will enable others to go farther than he has done. This plan is made up of four parts, and the present paper, which deals with the British Empire, is a section of the third part now approaching completion.These four parts, three of which will be briefly outlined in the following pages, are :—

1.
Formation of an Earthquake Catalogue.

2.
Refutation of the empirical laws previously enunciated.

3.
Description of the globe from the seismic point of view.

4.
Study of seismic phenomena in the United Kingdom and the British Colonies.
II. Formation of an Earthquake Catalogue. More than 100,000 observations of earthquakes have been brought together, 6175 of which have been made use of in the present work. These observations vary much in value ; when they are the result of isolated narratives, gathered from documents of all kinds (but the object of none of which is the special study of earthquakes), we get so-called I historical series,' generally of little account. If, on the other hand, scientific men have especially busied themselves with these phenomena in any particular country, and have taken careful note of the earthquakes felt by them or reported to them, we
Notes on the Glacial Geology of Arctic Europe and its Islands.—Part II. Arctic Norway, Russian Lapland, Novaya Zemlya, and Spitsbergen.
Authors: Feilden H. W. 
Published: October 2009

So much has been written about the glacial geology of Northern Norway by, great authorities that I should have refrained from discussing the subject had I not recently heard a paper' read at a Meeting of this Society, in which the author suggested that the terraces in the transverse fiords of North-western Norway would be perfectly explained by the formation of ice-dammed lakes. The author, however, admitted that the authenticated occurrence of marine organisms in these raised beaches would be a conclusive argument against his views.I have never made any special study of the phenomena connected with the secular upheaval of Arctic Norway, for I had always been under the impression that few geological facts were more generally accepted -as well established than the recent elevation o,f land in Arctic latitudes, including Northern Norway. My observations are consequently somewhat cursory, but I do not remember landing on any of the more considerable islands north of the Arctic Circle, that form the ‘ Skjergaard' of Norway, without noticing traces of recent elevation and deposits containing abundantly shells of molluscs of the same species as those that now inhabit the adjacent sea. The same holds good of the ‘ westeraalen,’ and I observed last summer a well-defined raised beach near the settlement of Rissohavn, on the island of Andd, full of the shells of recent molluscs; this beach was overiain by 4 feet of peaty soil, in which grew birch-trees.
The lofty chain of the Lofoten Islands has not been buried under