bluuebunny/crossref_metadata_2025_split huggingface dataset:
A Comparison of the Permian Breccias of the Midlands with the Upper Carboniferous Glacial Deposits of India and Australia
Authors: Oldham R. D. 
Published: October 2009

I.
Introduction

In 1855 the late Sir Andrew Ramsay read before this Society a paper on the Permian breccias of Enville and of the Clent, Abberley, and Malvern Hills, in which he gave his reasons for believing that they were deposits of glacial origin. This was followed in 1875 by a paper of the late Mr. H. F. Blanford, in which the suggestion was made that the Talehir boulder-beds of India, whose glacial origin had been recognized in 1856, might have been formed during that glacial period the traces of which had been preserved in the Permian breccias of England.
The glacial origin of these breccias has frequently been disputed, and the doubts cast on them have been to a certain extent reflected on the Indian deposits to which a similar origin has been ascribed. No actual comparison of the two by any observer acquainted with both had, however, been made, and I determined to take an opportunity of visiting some of the exposures with a view of comparing the English and Indian rocks. The opportunity came last Easter, and I have to express my obligations to Mr. Wickham ing, F.G.S., who has made a special study of the deposits, and was good enough to guide me to the principal localities and the best exposures.

II.
The Permian Breccias of England

The grounds on which the late Sir Andrew Ramsay based his beliefs in the glacial origin of the beds were, stated briefly, (1) the distance from which the included
Contributions to the Geology of British East Africa.—Part I. The Glacial Geology of Mount Kenya
Authors: Gregory J. W. 
Published: October 2009

In the discussion as to the respective merits of the rival theories concerning the causes of former glaciation, few lines of work seem likely to yield better results than the study of the originally greater extension of glaciers in tropical regions. When therefore, on emerging from the dense forests of the lower slopes of Mount Kenya, I came upon a series of old moraines, not 10 miles from the Equator and far below the level of the existing glaciers, my interest was at once aroused in the additional problems presented for solution.
Mount Kenya is situated in long. 37° 20′ E. and lat. 0° 6′ S.; it rises to the height of approximately 19,500 feet, and covers an area of about 700 square miles. It consists in its lower part of a huge pile of volcanic ash and débris, with a low gradient, rising from 7200 to 10,200 feet, densely covered with forest and bamboo-jungle. Above this frown steep craggy slopes of coarse agglomerates, ash, and lava, while the whole is surmounted by a rugged pyramidal peak which is part of the central core of the old volcano.
The central peak is of such excessive steepness that the snow is scattered irregularly over it, instead of forming a ‘calotte’ or snow-cap, similar to those on Kibo (the higher summit of Kilima Njaro) and Chimborazo. The snow accumulates in the hollows and on the slopes with lower gradients; from these snow-fields a series of glaciers flow down into the valleys.
The
Notes on the Geology of South-eastern Africa
Authors: Draper David 
Published: October 2009

I. I
ntroduction
: P
hysical
F
eatures

I purpose, in the following pages, to give a brief description of the principal physical and geological features of that portion of South Africa which is situated between the 26th and 31st degrees of south latitude and the 29th and 31st degrees of east longitude
This area includes the Colony of Natal, the native States of Zululand and Swaziland, the south-eastern portion of the South African Republic (Transvaal), and the eastern portion of the Orange Free State and of Basutoland
(1) The Drakensberg Range
This range of mountains is the continuation of the main range, which runs roughly parallel with the coast-line of Cape Colony, from west to east, and turns rather suddenly northward at the Natal boundary. It is known under various names in Cape Colony, and as the ‘Drakensberg’ where it forms the boundary of East Griqualand and the Colony of Natal
The Drakensberg forms the watershed of the south-eastern portion of the continent; it divides the waters flowing westward into the Atlantic from those flowing eastward into the Indian Ocean. The rivers flowing westward, viz. the Orange and the Vaal, drain the inland portion of South Africa. Those flowing eastward, the principal of which are the Tugela, the Usuto, and the Pongolo, drain the coastal portion. These latter small in comparison with the Vaal and Orange rivers
the Drakensberg range consists of three distinct portions, differing greatly in aspect.

The
Mountain portion
, extending northward to the ‘Montaux-Sources,’ forming a bold and rugged mountain-chain
On the Relations of some of the Older Fragmental Rocks in North-western Caernarvonshire
Authors: Bonney T. G. , Raisin Catherine A. 
Published: October 2009

In a recent paper published in the Quarterly Journal of the Geological Society, a new and revolutionary hypothesis is put forward as to the age and position of certain well-known conglomerates and associated beds in North-western Caernavonshire. The new explanation presents at once some difficulties, but these have been increased in number and gravity by a fresh study of the district. We selected those portions of it examined by Mr. Blake, in which the more critical sections occur, and tested with the microscope the questions raised by work in the field. The one or the other author was already in possession of a fair number of slides from a district in dispute, and nearly fifty additional specimens have been expressly prepared for the present paper
According to the new hypothesis, the strata previously mapped and described from near Llyn Padarn and from neighbouring districts can be distinguished into two groups separated by a strongly marked unconformity. While the one part is held by Mr. Blake to be of early Cambrian age, the other is ‘post-Llanberis.’ A question at once suggests itself, namely, to what epoch (from the Menevian onwards) do these so-called ‘post-Llanberis’ sediments belong, and where in adjacent districts may we find beds that can be correlated with them? Of this problem Mr. Blake has not succeeded in offering a solution, but he evidently perceives that it is one which claims consideration
The new hypothesis, however, would involve two consequences of far-reaching import. The unformity is described as being
The Formation of Oolite
Authors: Wethered E. B. 
Published: October 2009

If a thin section of oolite be mounted in Canada balsam and examined under a microscope, it is seen to be made up of a number of granules associated with fragmental remains of calcareous organisms, and the interstitial spaces are filled in with calcite.
Looked at with a 2-inch object-glass these oolitic granules show, for the most part, a series of concentric strata or laminæ of calcium carbonate around a nucleus. There are also other secondary structures, the principal of which are dark striæ and patches, the former placed more or less at right angles to the nucleus.
At the Bath meeting of the British Association in 1888 Prof. H. G. Seeley read a paper ‘On the Origin of Oolitic Texture in Limestone Rocks.’ In this communication the author stated that he ‘believed that oolitic texture might originate in many ways……’ He also drew attention to the ‘close resemblance of the internodal grains of the nullipores to grains of oolite as furnishing a further explanation of oolitic texture. These grains show a concentric structure as well as a radiated tubular structure, which would favour the recrystallization such as commonly occurs.’
Generally speaking, up to the year 1889 the concentric layers were supposed to be chemically deposited calcium carbonate. Thus Dr. Sorby, F.R.S., in his most able and memorable address to the Geological Society in 1879, describes the formation of normal Jurassic oolitic grains in the following words : They are ‘ composed of more or less well-defined layers of small
Notes on the Genus
Murchisonia
and its Allies; with a Revision of the British Carboniferous Species, and Descriptions of some New Forms
Authors: Donald Jane 
Published: October 2009

I. T
he
S
ubdivision of the
G
enus
M
urchisonia
and its A
llies

17 a previous paper 1 I gave an account of the establishment of the genus
Murchisonia
by D'Archiac and De Yerneuil, and described its characteristics. Since that date several new subdivisions of the genus have been made by pal~eontologists, and however reluctant we may be to introduce new terms, we cannot well avoid doing so, for many of the
Murchisoniæ
vary considerably from the type. Palmontologists differ both in the divisions that they adopt and also in the value that they attach to them. While some merely consider these as sections, others regard them as subgenera, or even distinct genera. Before proceeding to examine these divisions it may be well to enumerate the generic characters of
Murchisonia
as now defined :—

Shell elongated, turreted, composed of more than six gradually increasing whorls. Whorls more or less angular, variously ornamented or smooth. Mouth oblong, oblique, terminated at the base by a very short or truncated canal. Columella arched. In the outer lip there is a narrow and more or less deep slit with parallel edges, the successive filling-up of which during the growth of the shell produces a continuous band throughout the whole length of the spire. This band is distinctly defined, and composed of either a single or double keel. Umbilicus open or closed.
Though D'Archiae and De u do not indicate any particular species as type, the first mentioned on the list that they give has generally been accepted
An Experiment to Illustrate the Mode of Flow of a Viscous Fluid
Authors: Sollas W. J. 
Published: October 2009

Now that the theory of glacier-movement propounded by James Forbes stands alone, undisturbed by conflicting hypotheses, we more readily perceive its simplicity and beauty; and we cannot refuse a tribute of admiration to the clarity of thought, no less to the skill in observation, which led that distinguished investigator to success in the treatment of a problem which his famous contemporaries had found so baffling.
Whatever may be the ultimate explanation, there can be no question of the fact, that the ice of glaciers behaves precisely like a plastic solid or highly viscous liquid; and it is consequently by enquiries into the laws of viscous flow that we may justly seek to extend our knowledge of the movements of flowing ice.
No substance is probably better suited for experiments in this direction than solid pitch, or that substance commonly known as ‘cobbler's wax,’ in which it occurs as the chief constituent. Under a sudden pull or pressure this material behaves like the most brittle solid, but when stress is slowly applied it yields continuously to deformation. A small fragment kneaded between the finger and thumb may be slowly drawn out into a thread of indefinite length, but if suddenly pulled it snaps across with a clean fracture; it may be readily impressed with the finger-nail, but a smart tap with the point of a needle shivers it into angular fragments.
While it thus essentially resembles ice in the manner in which it reacts against deforming forces, it possesses the advantage
The Bajocian of the Mid-Cotteswolds
Authors: Buckman S. S. 
Published: October 2009

Summary and Conclusions

The following are the facts and conclusions advanced in this paper:—

1.
A record of the stratigraphical sequence of the ‘intervening beds’ between Stroud and Leckhampton

2.

The correlation of the Gryphite- and Lower
Trigonia
-grits respectively.

3.
A demonstration of how the stratigraphical sequence has been affected by the ‘Bajocian denudation’

4.
The discovery of the importance of the Cold Comfort section, and the position of its beds.

5.
The discovery of a new ammonitiferous horizon in the Cotteswolds.

6.
The bearing of this discovery on Jurassic chronology.

7.

Correlation of the ‘intervening beds’ with Dorset strata, and the necessity of dividing the ‘
Witchelliæ
hemera’ into this and ‘
Sonniniæ
hemera.’

8.

The geographical extent of the ‘intervening beds’; and a demonstration that the strata of the
Witchelliæ
hemera only cover about 1½ square miles in the Mid-Cotteswolds.

9.
Records of the chronological sequence of brachiopoda; with special reference to their value in stratigraphical correlation.

10.
Description of certain new brachiopoda, particularly noticeable for their value as indicators of horizons.

11.
Notes on the development of certain brachiopoda, to show the importance to nomenclature of exactness in recording horizons, and the importance to correlation of having a nomenclature in accordance with development, by avoiding a confusion of heterogenetic forms.
Notes on the Glacial Geology of Arctic Europe and its Islands. Part I.: Kolguev Island
Authors: Feilden H. W. 
Published: October 2009

During the month of July 1895, after two ineffectual attempts to reach Novaya Zemlya, owing to the great accumulation of ice in Barents Sea, we ran down the dge of the ice-pack, which extended intact from Novaya Zemlya to the northern end of the Island of Kolguev. We were fortunate enough to meet with a day so fine and a sea so smooth that our party of five persons landed without difficulty at the mouth of the Gobista River, on the southwestern side of Kolguev. Our yacht was sent back to Vardö for coal, and we reminded on Kolguev for ten days, encountering very inclement weather. A most opportune break in an almost continuous series of gales and fogs enabled us to leave Kolguev on the return to our vessel, without difficulty or danger.
The Island of Kolguev lies in Barents Sea, distant some 50 miles from the manland of Arctic Russia, and about 130 miles southwest from the nearest part of Novaya Zemlya. Its greatest breadth is about 50 miles, and its extreme length 40 miles; the general shape is oval. The superficial area may be roughly estimated at 2000 square miles. As a familiar comparison, we might liken it in extent to our East Anglian country of Norfolk.
The soundings between Kolguev and the mainland of Europe do not exceed 30 fathoms, while, in all probability, 70 fathoms is the extreme depth between it and Novaya Zemlya. Kolguev, however, differs completely in geological structure from the mountainous islands
Evidences of Glacial Action in Australia in Permo-Carboniferous Time
Authors: David T. W. Edgeworth 
Published: October 2009

The subject of which this paper treats has already been traversed by the author in his Presidential address to the Geological Section of the Australasian Association for the Advancement of Science, at its meeting at Brisbane in January 1895.
The author hopes, however, that the presentation to this Society of a summary of these previous records,—with the addition of his subsequent field–work in 1895,—will be justified by the opportunity now given of a discussion which will be of immense benefit in furthering an important and interesting branch of geological investigation.
The personal observations recorded in this paper are the result of 13 years‚, more or less constant, field-work in Australia.
I. Work done by previous observers. The first actual record of evidence of ice–action in Australia is probably that made by Dr. A. R. C. Selwyn in 1859. The statement is as follows :— At one point in the bed of the, Inman I observed a smooth, Striated, and grooved rock–surface, presenting every indication of glacial action. The bank of the creek showed a Section of clay and coarse gravel; or drift, composed of fragments of all sizes irregularly interbedded through the clay. The direction of the grooves and scratches is E. and W. in parallel lines; and though they follow the course of the stream, I do not think they could have been produced by the action of water forcing pebbles and boulders detached from the drift along the bed of the stream. This is the first and only
On Transported Boulder Clay
Authors: Hill Edwin 
Published: October 2009

I wish to put on record some facts lately observed respecting two groups of Boulder–Clay masses which appear to have been transported from their original positions.
One group occurs in the cliffs south of Great Yarmouth. The sands of the cliffs which extend from Lowestoft to Yarmouth are usually described as ‘ Mid–Glacial.‘ On them lies Chalky Boulder Clay as seen at Corton and northwards, while below them are seen at several spots a perfectly different stony clay, the sands called Pebbly Sands or westleton Beds, and the well–known Rootlet Bed. The Chalky Boulder Clay extends continuously above the Mid–Glacial sands, from Corton for about ¾ mile northwards ; farther on, one or two disconnected strips also lie on the top of the cliffs. But, besides these, several masses of the same material occur embedded in the sands. I first noticed them while examining the coast in 1893, and in the spring of 1895 I again made a careful inspection, this time in company with Prof. Bonney.Two lie one on either side of the depression called League Hole, and others were seen respectively about 1/2 mile, 1 mile, and 11/2 mile north, towards Gorleston. The writer of the Survey Memoir (Mr. J. H. Blake) had his attention attracted to these or similar masses, and remarks that ‘ at times they looked as if they were lenticular patches of Boulder Clay in the Glacial Sands ‘ (p. 56, Geology of Country near Yarmouth and Lowestoft).He decided, however, that‘ they were all
Notes concerning certain Linear Marks in a Sedimentary Rock
Authors: Talmage J. E. 
Published: October 2009

Abstract
The marks described in the paper occur in a fine–grained argillaceous sandstone referred by the U.S. Geological Survey to the Triassic or Jura–Trias period, which is found on a low tableland within 2 miles of the bluffs overlooking Glen Canyon. The marks commonly appear as straight lines intersecting at right angles, but some have a pinnate distribution, suggesting engravings of frost–flowers. A description of the markings is given, and various experiments made in the laboratory to illustrate the effects of formation of crystals formed over sediment are described. (See a paper by the same Author in the Utah University Quarterly for December 1895.)
The Eocene Deposits of Dorset
Authors: Reid Clement 
Published: October 2009

The new survey of the western end of the Hampshire Basin having necessitated certain modifications in the geological map, it may be useful to lay the principal results before the Society. If the alterations were mere matters of detail, this would scarcely be worth while; but the more accurate mapping has led to the discovery of a sudden westerly change in the character of the Lower Bagshot Sands, and of a well-marked overlap at their base. The mapping of the Tertiary strata proves also that there is evidence of other periods of earth-movement in southern England, besides those already known, and that we are dealing with one of those regions where folding affects the same area again and again.
When the Eocene strata are followed westward through Sussex and Hampshire into Dorset, one finds constant local changes in the lithological character of the deposits, though these changes seem all to tend in the same direction. Marine beds become less conspicuous, coarser, more estuarine, and estuarine deposits become truly fluviatile. Thus the London Clay, which exceeds 300 feet in thickness to the east, dwindles to less than 100 feet in Dorset, and becomes more sandy and pebbly, though still apparently of marine origin. The Woolwich and Reading Series—fluvio-marine at Newhaven and Portslade, and slightly so at Lancing— becomes more fluviatile westward, lenticular patches of subangular gravel appearing in it west of Wareham. To what extent the Reading Series rests unconformably upon the Chalk is difficult to say, though overlap is clearly
On the Distribution in Space of the Accessory Shocks of the Great Japanese Earthquake of 1891
Authors: Davison Charles 
Published: October 2009

I. Introduction.
The complete history of the Mino-Owari, or great Japanese, earthquake of 1891 has yet to be written; but several important contributions to it have already been made. Prof. Koto, in an admirable memoir, has traced the course of the extraordinary fault-scarp and discussed the origin of the earthquake; Prof. Ōmori, with equal care and thoroughness, has investigated the unrivalled record of after-shocks; and Prof. Milne, in his invaluable catalogues of Japanese earthquakes, has provided the materials for detailed analyses from many points of view.
My object in this paper is to consider the geographical distribution of the numerous shocks which preceded and followed the great earthquake. Prof. Ōmori has discussed the distribution of the after-shocks of this and other Japanese earthquakes, chiefly with regard to time; but, in an interesting section of his memoir, he studies the distribution in space of the after-shocks of the Mine-Owari earthquake. In order to show the difference between Prof. Ōmori's method of treatment and that adopted in the present paper, I will first give a brief summary of this part of his work, though it is difficult to do justice to it without reproducing his maps.
II. Methods of representing the distribution of the Shocks.

2. The great earthquake occurred on October 28th at 6
h
38
m
a.m. (mean time of 135° E.) and duringthe first few days the aftershocks were so numerous and were separated by intervals of time so short that the identification of many of those observed at different places
Note on Volcanic Bombs in the Schalsteins of Nassau
Authors: Kayser E. 
Published: October 2009

The origin of the schalsteins of Nassau, the Harz, and other districts has remained hitherto an unsolved enigma for geologists. This, however, is not surprising, considering the very variable nature of the rocks. Generally of greyish-green colour, with highly-developed slaty cleavage, and with a large admixture of calcareous and chloritic matter, the schalsteins are sometimes earthy, sometimes coarse-grained to conglomeratic and brecciated—and in this latter case they contain frequently fragments of foreign rocks of extremely diverse derivation, such as diabase, porphyry, limestone, slate, etc. The schalsteins are, moreover, sometimes fossiliferous and distinctly bedded, and sometimes unfossiliferous, with as little evidence of stratification as an eruptive rock.
Some geologists consider the schalsteins as originating from a mixture of disintegrated diabases and ordinary argillaceous mud; others see in them a product of metamorphic processes; while most observers look upon them as volcanic tuffs, but greatly changed in consequence of their great age. That this last opinion is the only correct one seems clearly proved by the bombs which I have discovered.
These bombs are found in great numbers in two localities in the neighbourhood of Oberscheld, near Dillenburg: firstly in the vicinity of the village of Bicken (well known to the paæontologist on account of the occurrence there of Hercynian and Upper Devonian fossils), in a fine, earthly schalstein, very well stratified; and secondly, close to Oberscheld, in a slaty rock, less clearly strafied.