bluuebunny/crossref_metadata_2025 huggingface dataset:
On the Physical Conditions of the Mediterranean Basin which have resulted in a Community of some Species of Freshwater Fishes in the Nile and the Jordan Waters
Authors: Hull E.
Published: October 2009

The Author summarizes the evidence in favour of the existence of barriers in post-Miocene times, separating the Mediterranean area into a chain of basins. He brings forward arguments in support of his contention that the waters of the eastern (Levantine) basin became fresh during a period when the area of evaporation was smaller, and the supply of river-water greater, than at present. Into this freshwater lake the waters of the Nile would flow directly. He has elsewhere given reasons for believing that the Jordan Valley from Lake Huleh to Arabah was the bed of a lake over 200 miles long, and at least 1300 feet above the present level of the Dead Sea. He suggests that the waters of this lake escaped into the Levantine basin through the plain of Esdraelon. With such physical conditions existing, the fauna of the Levantine basin would have a means of spreading throughout the whole system of waterways connected with it.

In conclusion the Author adds some observations on the changes which occurred in the Mediterranean area subsequent to the post-Miocene epoch of earth-movement.
On some Phases of the Structure and Peculiarities of the Iron Ores of the Lake Superior Region
Authors: Gresley W. S.
Published: October 2009

The Author has been studying heaps of ore brought from the region lying south-west of Lake Superior since 1890. He describes certain structural features of the ore-fragments, and discusses the evidences of mechanical movements and chemical alteration exhibited by these fragments.
On the Mean Radial Variation of the Globe
Authors: Lobley J. Logan
Published: October 2009

The Author submits considerations (chiefly derived from the characters of the earlier sediments) which lead him to suppose that crust-folds have not been produced by continuous contraction of the Earth, and that the planetary heat and mean radius of the Earth have been practically invariable during the period which has elapsed since Cambrian times.
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,
Contributions to the Palæontology and Physical Geology of the West Indies
Authors: Gregory J. W.
Published: October 2009

S
hortly
after Mr. Jukes-Browne's return from Barbados in 1889, he asked me to identify a collection of fossil corals which he had made on that island. A very cursory examination showed that the synonymy of the coral fauna of the West Indies was in such confusion that it would be impossible properly to execute this task, and work out the relations of these Barbadian fossils, with the material then available to me. The causes of the difficulty were as follows:—In the West Indies there are two coral faunas, one recent and the other fossil. The former has been described by the neontologists, the latter by the palæontologists; and neither school has devoted adequate attention to the work of the other. If the two faunas had been wholly distinct, this would not have mattered so much; but unfortunately they overlap, and thus the same species have been twice described. The extent to which this has been carried has been greatly increased by the fact that many late Pleistocene species have been mixed in collections with those of the older Kainozoic deposits. The synonymy has been still further complicated by the imperfection of the original figures and descriptions upon which most of the species are based. The West Indian corals were favourite objects in the collections of the early naturalists, and thus the great majority of the species date back to the works of the museographers of the last century. The illustrations given by these authors show the mode of growth and
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
Supplementary Notes on the Systematic Position of the Trilobites
Authors: Bernard Henry M.
Published: October 2009

S
ince
I had the honour of reading a paper on this subject before the Geological Society (printed in this Journal, vol. 1. 1894, p. 411) two other papers have appeared in America, giving further details as to the appendages and structure of
Triarthrus
. Both papers are by Dr. C. E. Beecher. The earlier, describing the pygidial limbs, appeared in time to be briefly mentioned in a footnote in my own paper just referred to. The more recent has but now appeared, and gives an account of the ventral structure of
Triarthrus
. These two papers seem to me to contain matter of perhaps even greater morphological interest than the discovery of the antennæ.

The Metastoma.
—Taking the new evidence, not in the order of its appearance, but in the order of the parts referred to, the rectastoma, ‘ now revealed for the first time,’ is described and figured by Dr. Beecher as a small, convex, arcuate plate just posterior to the extremity of the hypestema. A small arcuate plate projecting backwards, as shown in Dr. Beecher's figures, is the exact form that the labium or lower border of the mouth must have assumed, when the segment of the hypothetical annelid ancestor bent round so that the mouth opened post, riorly for the new method of feeding. But such a metastoma, as I have already argued, would be a disadvantage: it would form a barrier in the way of food being pushed into the mouth by the ‘gathobases.’ In
Apus
we accordingly find
On Fluvio-Glacial and Interglacial Deposits in Switzerland
Authors: Du Riche Preller C. S.
Published: October 2009

I. I
ntroduction.

I
n
a paper published in the Geological Magazine for January 1894, I showed that the Swiss Alps had been visited not only by two, but by three general glaciations, of which the first may be referred to Pliocene, the second to Middle Pleistocene, and the third to Upper Pleistocene times. The evidence consists chiefly in a number of glacial and so-called fluvio-glaciM deposits which I had examined in the Swiss lowlands, and notably in the vicinity of the Lake of Zürieh, where, perhaps more than in any other part of Switzerland, such deposits are laid open within a comparatively small and easily accessible area.

The first suggestion of certain gravel-beds at the foot of the Italian Alps being older than the two Pleistocene glaciations then generally accepted may be said to have emanated from Stoppani, Desor, and notably from Renevier, as early as 1875. In 1882, Prof. Penck succeeded in showing, on the evidence of Deckensehotter or plateau-gravel, that the Bavarian and Austrian Alps had been visited by three different glaciations; but as regards the Swiss Alps, even such distinguished glacial geologists as Prof. Helm hesitated to adopt that view until quite recently, namely in 1891 Dr. Léon Du Pasquier, of Neuehhtel, showed in a valuable memoir that the fluvio-glacial gravels deposited in the valleys of the principal river-systems in the North of Switzerland admit of being classed in three distinct categories, to wit, Cavernous Nagelfluh (the Swiss equivalent for Deckenschotter),Upper Terrace-, and Lower Terrace-gravels. Dr. Du Pasquier
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 a Human Skull and Limb-bones found in the Palæolithic Terrace-gravel at Galley Hill, Kent
Authors: Newton E. T.
Published: October 2009

I. I
ntroduction
.

At a time when so much attention is being directed to the implements made by Palæolithic Man, the discovery of a human skeleton in the Palæolithic gravels of this country cannot but awaken much interest. The remains which form the subject of the present communication have been submitted to me for description by Mr. Robert Elliott, of Camberwell, whose enthusiasm as a collector of flint-implements and other antiquities is well known to many of us, as is also the fine collection of these relics which he has with much labour brought together. It was in the year 1888, on one of his journeys in search of ‘implements,’ that Mr. Elliott discovered parts of a human skeleton in the gravel yielding Palæolithic implements, which, at a height of about 90 feet above the Thames, overlies the Chalk at Galley Hill, Northfleet. The particulars of this discovery are given in a letter from Mr. Elliott, which will be found at p. 518. The interest of the discovery has seemed to me sufficient to justify a full account of it being placed on record, so that all attendant circumstances may be known, and everyone interested in the matter placed in a position to draw his own conclusions as to the age of these human remains.

II. D
escription of the
R
emains

The portions of the skeleton which have been recovered area large part of the skull, wanting the facial bones ; the right half of the lower jaw still retaining the grinding
On Overthrusts of Tertiary Date in Dorset
Authors: Strahan A.
Published: October 2009

I. I
ntroduction

The intensity of the earth-movements which have thrown on end and inverted the Secondary rocks of Dorset, and the magnificent dissection of the structures in the sea-cliffs, have attracted attention for many years past. The first to give an accurate account, and to speculate on the causes of the position of the strata, was Webster in 1816; though admirable in his description and in his pictorial representation of the facts, he failed in his endeavour to explain them, and was in this respect improved upon by Conybeare and Phillips in 1822, and by W. B. Clarke in 1837. In 1830 Buckland and De la Beche read their paper on the Geology of Weymouth, etc., and gave an account of the principal faults, but did not correctly distinguish those that were formed before the deposition of the Gault from others that were produced at a later date. In 1848 a cutting made for the Dorchester and Weymouth railway revealed unsuspected complications in the great Ridgeway disturbance, which were described with great accuracy by Weston in 1848 and 1852, while additional light was thrown upon the subject by the publication in 1850 of the Geological Survey map, Sheet 17, in the preparation of which Bristow received great assistance from the Rev. O. Fisher. Further speculations on the age of some of the disturbances were made by Prof. Prestwich in 1875, and the existence of two distinct sets of movements was pointed out by Mr. Hudleston in 1881 and 1889. In
The Geology of Mount Ruwenzori and some Adjoining Regions of Equatorial Africa
Authors: Elliot G. F. Scott , Gregory J. W.
Published: October 2009

I. I
ntroduction
.

R
uwenzori
is a mountain-ridge on the right bank of the Semliki branch of the Nile, between the two lakes Mwutan and Lutan Nzige (the Albert and Albert Edward Nyanzas). It ranks as the third snow-capped mountain in Africa, both in height and date of discovery. Kilimanjaro was first seen in 1848 and Kenya in 1849, and Ruwenzori only narrowly escaped detection a few years later. Speke and Grant passed near it in 1862, but its existence was not reported to them, though the natives whom they met must have known of it. Sir Samuel Baker, in 1864, approached it from the north, and reached a locality from which the mountain ought to have been visible; but he did not see the snow, and though his ‘Blue Mountain’ seems to have been Ruwenzori, he covered the whole site of the mountain with a lake. Gessi Pasha circumnavigated the Albert Nyanza in 1876 and went nearer to the mountain than the point from which it was subsequently discovered; but he also missed it. Mason Bey, in 1877, followed the same course, and though he stayed for some time for astronomical purposes within sight of Ruwenzori, he never saw it. It was reserved for Mr. Stanley, in 1888, to recognize that the white patches that appeared among the clouds for brief and at distant intervals were a snow-capped ridge.

The late Capt. W. G. Stairs made an effort to ascend the mountain in 1889, and reached a level determined by aneroid
The ‘Schistes lustrés’ of Mont Jovet (Savoy)
Authors: Gregory J. W.
Published: October 2009

The controversy as to the age and origin of the ’ Schisted lustrés’ of the Western Alps has passed through three distinct stages. At beginning of the century these schists were included among the primitive rocks. Even in the first decade, however, this idea was refuted in a paper by Brochant, which may still be read with interest, owing to its excellent description of the physical features of the Tarentaise. In this work, all the rocks of which Mont Jovet is composed, with the exception only of the gypsum, were referred to a series of ‘terrains promitifs’ within still narrower limits, Bakewell then showed that the English Coal Measures, he included the limestones in the Mezoic. A second stage in the controversy was entered upon eith Elie de Beaumont's epoch–making discovery of belemnites in the limestones of Petit–Cœur, a hamlet 5 miles north west of Mont Jovet. In consequence of this, Fournet, in his map, marked the whole of the rocks of the mountain as Jurassic; while, later on, Lory, who knew the locality well, identified the schists and limestones of the summits as altered Trias. In spite of the protests of the Italian geologists, who referred the ‘ Schistes lustrés’ either to the early Palœozoic or to the Archœan crystalline series, the weight of Lory's influence gained general acceptance for his view. It was not till 1887 and 1889 that Zaceagna and Bonney carried the controversy into the third phase by the independent description of some sections across 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 Structure of the Plesiosauria Skull
Authors: Andrews Charles W.
Published: October 2009

The structure of the skull of the Liassic Plesiosauria has been discussed by many writers, but the various accounts that have been given of it are incomplete, and often differ one from the other in important particulars, doubtless owing to the fact that in most cases the specimens examined are much crushed, and are embedded in the matrix, so that only one aspect is visible. In the National Collection there is, however, a fine skull of
Plesiosaurus macrocephalus
, which has lately been almost completely cleared from the matrix, so that it exhibits both the upper and under surfaces; this specimen, though it has been subjected to a slight vertical compression which has caused some fractures and dislocations, gives a fairly clear idea of the general arrangement of the constituent bones, and, since it throws light on some obscure points, seemed worthy of the following brief notice. Certain other specimens, which are of assistance in some difficulties, will also be referred to.

In 1838 Owen figured and described the upper and lateral regions of the skull of
P. macrocephalus
, and in 1881 Sollas described under the name
P. brachycephalus
some portions of the head of a specimen probably referable to the same species. Neither of these writers had an opportunity of examining the palate, and it is this region, therefore, that is more particularly considered here; while, in the structure of the rest of the skull, only such points are noticed as seem to add to, or to be at variance
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

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
On the Geology of the Neighbourhood of Carmarthen
Authors: Crosfield Margaret C. , Skeat Ethel G.
Published: October 2009

I. Introduction and Bibliography.

The area described in this communication has Carmarthen for its centre, and lies approximately within a 4–mile radius of that town, as indicated in the accompanying sketch–map (Pl. XXV.). Our object in examining this district was to trace the continuation of the complex anticline which was discovered by the late Mr. T. Roberts, about 10 miles west of Carmarthen. In the map illustrating his paper the anticline is shown to be narrowing rapidly in the neighborhood of Mydrim, the
Didymograptus
–beds seem to wrap round the older
Tetraptus
series, and apparently the anticline is dying out.

An examination of the beds round Carmarthen has enabled us to establish this conclusion, ans to show that in our own district we have a new anticline, the northern limb of which continues in the same direction as that of the anticline farther west, but with a core consisting of older rocks, which er correlate with the Tremadoc Slates. The southern limb of the new anticline is buried under Old Red Sandstone (which here encroaches farther north than at St. Clears), but in the northern limb we have a regularly ascending series from Tremadoc Slates to
Dicranograptus
–shales. To the east this regular succession of beds is disturbed by the presence of an extensive series of alternating grits and sandstones, with some shales, the last containing Bala fossils. The beds in question abut on those of Arenig age, but whether their appearance in this locality is due to faulting or to an
Extrusive and Intrusive Igneous Rocks as Products of Magmatic Differentiation
Authors: Iddings J. P.
Published: October 2009

Prof. W. G. Brögger, in dedicating to me his recent work on ‘Die Eruptionsfolge der triadischen Eruptivgesteine bei Predazzo in Südtyrol,’ 1 has not only honoured me by this token of his friendship, which I prize highly, but also by associating my name with a work which commands my admiration, and with which I am in the most hearty accord. His treatment of the igneous rocks in the region of Predazzo as a generic series intermediate in composition between a granite-diorite-gabbro series and a granite-syenite (elaeolite-syenite) series is fully justified by their chemical and mineral composition and by their geological association ; and for the order in which these rocks have been erupted he has given ample evidence. The intrusive character of the granular rocks is clearly established, and the fantastic theory of Reyer abundantly disproved. So also the discussion of Kjerulf and Michel-Lévy’s hypotheses, regarding the melting and assimilation of overlying rocks by molten granitic magmas, leaves nothing to be said in further refutation of these suggestions, so far as they relate to the intrusion of igneous magmas that come within the range of our investigation. To suppose that such a process may have been active in the earliest period of the cooling globe is quite reasonable. It implies a very highly-heated magma, and shifting temperature or convection-currents. As applied by Suess to account for the great craters of the moon, it appears highly probable. But there is no evidence that such a melting has taken place in 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
Appendix. Report on Specimens collected by Col. H. W. Feilden in Arctic Norway, etc.
Authors: Bonney T. G.
Published: October 2009

In the following notes the specimens collected by Col. Feilden are grouped according to localities and arranged in the order of the dates on the labels.

(i) From Rock in place, Stor Tamsö, Porsanger Fiord, Norway.

(28.) A fine–grained, faintly speckled, light grey rock, apparently either a quartzose gneiss or quartz–schist, without strongly marked foliation. On examining a slice, quartz proves to be the dominant mineral. It occurs in rather. elongated irregularly–outlined grains, with borders of a different tint (with crossed nicols).A dark olive–brown biotite is present in both fair–sized flakes and tiny flakelets, with some felspar, but much less than one would expect from the macroscopic aspect of the rock; there are also a few small garnets, a little iron-oxide, and zircon. Macroscopically and microscopically the rock reminds me of some quartz–schists which I have collected near Braemar, Aberdeenshire, and in the neighbourhood of Clifden, Connemara.

Prof. T. G. Bonney on Specimens Collected by Nov. 1896,

(ii) Boulders from tundara in the neighbourhood of sviatoi nos, kola penisula.

(29.) A fine–grained reddish granite, rather rich in felspar and poor in mica (biotite and a little muscovite). Examination of the powder shows that some of the felspar is ferrite-stained, that microcline is present, and that the iron oxide probably is haematite.

(19, at Sviatoi Nos.) A moderately coarse, rather felspathic, reddish–coloured gneissoid granite; the biotite (not very abundant) exhibits a slightly linear arrangement. .A good deal of muscovite is seen on close examination with a lens; this also is found
On
Cycadeoidea gigantea
, a new Cycadean Stem from the Purbeck Beds of Portland
Authors: Seward A. C.
Published: October 2009

The Isle of Portland has long been famous for the silicified Coniferous and Cycadean plants which occur in the surface-soils of Purbeck age. Buckland, Carruthers, and others have described the manner of occurrence and structure of the plant-remains from this horizon, and the fossil “crows' nests,” or short, thick stems of Cycads, have long been familiar to geologists. The plant which forms the subject of the following description was acquired by Dr. Woodward in 1895, and is now one of the most remarkable specimens in the Fossil Plant Gallery of the British Museum. It is probably the largest fossil Cycad hitherto recorded, and although the internal structure has been for the most part very imperfectly preserved, the cast of the stem is in some respects unusually complete. The specimen was found lying in a horizontal position in a bed of shaly clay, 2 feet thick, and about 17 feet higher in the Purbeck series than the Great Dirt-bed, from which most of the Portland plants have been obtained.

The position of the fossil is shown in fig. 1; the section is drawn from a photograph of the rock-face in one of Mr. Barnes's quarries close to St. George's Church on the west side of the old Portland Wide Street.

In Pl. I. the stem is represented about ⅛ natural size; it measures 1 metre 18·5 cm. At the base it is somewhat narrower and thinner, and the surface-features are less clearly shown than in the other
Geological and Petrographical Studies of the Sudbury Nickel District (Canada)
Authors: Walker T. L.
Published: October 2009

I. Introduction.

The town of Sudbury is situated in Northern Ontario, 442 miles from Montreal on the transcontinental line of the Canadian Pacific Railway. When this railway was constructed some eight or ten years ago, the name Sudbury was given to a small station which was afterwards selected for the eastern terminus of the branch railway that follows the northern shore of Lake Huron and crosses the St. Mary River at Sault Ste. Marie. It is about 40 miles from the north-eastern shore of Lake Huron.

Shortly after the construction of the railway, considerable deposits of chalcopyrite were discovered in the neighbourhood, and an American company was organized to work them. Thus it was thatCopper Fliff Mine was opened up for copper, although along with the chalcopyrite large quantities of nickeliferous pyrrhotite occurred. The pyrrhotite was considered worthless, as it was not known to contain nickel till the mine had been in operation for some little time, and sales had been made of the products. After the accidental discovery of the value of the pyrrhotite as a nickel ore, there was much prospecting in the district for nickel-deposits. This continued till 1891, by which time scores of nickel-deposits had been located. At that time the world'sannual consumption of metallic nickel was not more than 1500 tons, and hence it was a more difficult task to dispose of nickel properties at remunerative prices than it was to discover them. for this reason, prospecting for nickel was abandoned in this region, though
The Raised Beaches and Glacial Deposits of the Varanger Fiord
Authors: Strahan Aubrey
Published: October 2009

The raised beaches of the Varanger Fiord have frequently been noticed. Though readily recognized all round Northern Norway, they are particularly well developed on the less precipitous coasts formed by the Gaisa rocks. In the immediate neighbourhood of Vadsö, the long slopes leading up to the moorlands of the interior can be seen from the sea to be diversified by a succession of terraces, too numerous to count, and lying one above the other up to a height of nearly 300 feet above the present shore. On closer examination these terraces are found to consist of shingle and sand, piled up here and there into characteristic beach-ridges, and enclosing behind them a number of shallow lakes or peat-bogs. Where the form of the ground permits they extend a considerable distance inland, and change the character of a large tract of country.

Though in every locality that I visited some of the intermediate beaches were more pronounced than others, I was not able to trace on such banks for more than a short distance, or to show that they occurred at the same level in different parts of the fiord. They seem rather to have been due to wave-action having been more energetic first in one place, then in another, as the form of the coast varied with the change of level. On the other hand, the upper limit of the
series of beaches could be traced without difficulty, and, so far as I saw, contoured the hills
around the fiord