bluuebunny/crossref_metadata_2025_split huggingface dataset:
On some Devonian and Silurian Ostracoda from North America, France, and the Bosphorus
Authors: Jones T. Rupert 
Published: October 2009

§I. D
evonian
S
pecies
.

§I. As stated at page 14 of the Quart. Journ. Geol. Soc. for February last, Mr. J. M. Clarke, of Albany, N. Y., sent me some Devonian
Ostracoda
, collected by him in Ontario Co., N. Y., and some from Clarke Co., Indiana. These are now illustrated and described herewith.

1.

1. The first-mentioned occur in the buff-coloured, earthy portion of a decomposing siliceous rock, known as “the Chert of the Coraiferous Limestone,” and cavernous with casts (internal and external) of Polyzoa, Ostracoda, remains of Trilobites, and other organisms, comprising some interesting specimens of
Beyrichia
and allied genera. There are six species, and these are illustrated in P1. XX. figs. 4, 9- –13, and PI. XXI. fig. 1

2.
2. Two species, collected also by Mr. J. M. Clarke, from the Hamilton Group, Clarke Co., Indiana, U. S., P1. XX. figs. 6 & 7.

§ II. Among the additional Ostracoda, collected by Dr. Hinde, F.G.S., as mentioned at page 28, Feb. No., Q. J. G. S., are some Devonian Ostracoda from the Hamilton Group at Thedford, Ontario, Canada, and from the same formation at Eighteen-mile Creek, Lake Erie, N.Y. Four of these, being new species, are here described and figured (P1. XX. figs. 5 & 8; and woodcuts, figs. 1 & 2).

§ III. The Devonian
Beyrichia
collected some years ago by M. Dumont at the Bosphorus, and noticed by Dr. Ferd. Römer in the ‘Neues Jahrbuch,’ &c. for 1863, having been kindly lent by M. Dewalque for examination, is here
The Variolitic Diabase of the Fichtelgebirge
Authors: Gregory J. Walter 
Published: October 2009

I. I
ntroduction
.

A
mong
the many interesting rocks described in 1874 by Prof. von Gümbel in his ‘Die paläolithischen Eruptivgesteine des Fichtelgebirges’ was a variety of diabase crowded with small round, apparently felspathic bodies. As these stood out on weathered surfaces like peas or pearls, he suggested for it the name of “Perldiabas.” Seeing that this peculiar modification occurred around the margins of the diabase masses, close to the contact with the sedimentary rocks into which they were intruded, Prof. von Gümbel regarded these pearl-like spheroids or “Knollchen” as fragments of the neighbouring beds caught up by the igneous rock, rounded by the rolling and the fusion of the sharp angles, and baked till they acquired the porcellanitic appearance that they now present. In the following year, Profi von Zirkel, in his well-known paper “Die Structur der Variolite”, described the microscopic structure of this rock, and, recognizing that the rounded spheroids are merely ordinary spherules, he identified it as variolite, and compared it with the typical varieties; he objected alike to von Gümbel's name and theory.

Prof. von Zirkel's conclusions were confirmed by Prof. Rosenbusch in his detailed microscopic examination of the rock, and he, in accordance with the view taken by the French geologists of the origin of the Savoy variolites, regarded these also as ordinary “endomorphen Contactformen der Diabase” on the selvage of intrusive dykes.
Prof. von Gümbel's faith in his own theory stood firm against these criticisms and this new evidence; and in 1879, in the third volume
Notes on Rock-specimens collected by W. Gowland, Esq., A.R.S.M., F.I.C., F.C.S., in Korea
Authors: Holland Thos. H. 
Published: October 2009

I. L
iterature
.

1704. A Collection of Voyages and Travels. London. Vol. iv. pp. 623-632.

1818. Account of a Voyage of Discovery to the West Coast of Corea and the Great Loo-Choo Island. Captain Basil Hall.London. Pp. 1-57. Appendix, p. cxxi
et seq.

1819. Voyage of H.M.S. ‘Alceste.’ John McLeod, M.D. Third Edition. London.

1834. Journal of Three Voyages along the Coast of China. Rev. Charles Gut~aff. Third Edition. London. Pp. 227-249.

1873-74. China-Sea Directory.

1881. “Notes on the Geology of the Corean Archipelago,” Nature, vol. xxiii, p. 417,

1886. “Geologisehe Skizze yon Korea.” Dr. C. Got~che. Sitzungs-berichte k. Akad. Wissensch. Berlin, vol. xxxvi, p. 857.

1886. “Beiträge zur Petrographie yon Korea.” Prof. J. Roth.
ibid
. p. 875.

II. I
ntroduction

Although his visit in 1884 was primarily intended for purposes of archaeological research, Mr. Gowland has succeeded, under considerable difficulties from the ill-concealed hostility of the natives, in collecting numerous specimens, and in making important observations on the geological structure of the interior of Korea.
Mr. Gowland traversed the country from Söul, the capital, to Fusan, on the south-east coast—the route thus roughly following up the basin of the Hart River to the watershed (which forms a natural line of boundary between the provinces of Chhung-chhöng and Kyöng-sang), and then from the pass year Mungyong, following the course of the Naktong River
On a Labyrinthodont Skull from the Kilkenny Coal-measures
Authors: Lydekker R. 
Published: October 2009

In going through the collection of Labyrinthodont remains from the Coal-measures of Jarrow Colliery, Co. Kilkenny, preserved in the Science and Art Museum, Dublin, I noticed a fragment of shale showing the lower jaw of a Labyrinthodont, which appeared to indicate a species different from any of those hitherto described from these beds. The slab in which the specimen is contained is of a slaty nature, without any of the pyritous matter which is so frequently fatal to the permanent preservation of the Jarrow fossils. On. examination it appeared that by splitting the fragment the upper surface of the skull might also be revealed; and this operation fortunately proved successful. Whereas, however, the external sculptured layer of the bones of the lower jaw is exposed, in the case of the cranium the line of fission has traversed a film of shale overlying the bones, and it has only been practicable to remove this film so as to expose the sculptured surface in the left postorbital region.
As is the case with all the Jarrow fossils, the specimen has been completely flattened by pressure; but, although the width of the cranium has been doubtless thus slightly increased, the general contour is fairly well exhibited. The outline of the right side of the cranium is, indeed, in great part destroyed, owing to the reflection of its maxillary border on to the inferior surface of the slab. On the left side of the cranium the contour is, however, entire. The extremity of the
Manod and the Moelwyns
Authors: Jennings A. Vaughan , Williams Griffith J. 
Published: October 2009

On the north and west of the great mass of Harlech Grit which forms the centre of the Merioneth anticlinal, the Lingula and Tremadoc strata dip under the mountains of the Moelwyns and Manods, and are there overlain hy the Arenig ashes and slates. The beds exposed on the southern slopes of these mountains have therefore the same general stratigraphical age as those cropping out on the northern slopes of Cader Idris and on the western aspect of Arenig and the Arans.
The general relations of the rock-masses of this difficult district have been admirably elucidated by the officers of the Geological Survey, and the results of their work published in Sir A. Kamsay's invaluable memoir on the Geology of North Wales.
In the present paper, which is the result of observations carried on interruptedly for several years, our objects are :—
To offer conclusive evidence as to the intrusive nature of the great crystalline mass known as the Syenite of Tan-y-grisiau.
To correct what seems to us an inaccuracy of some importance in the correlation of beds in different parts of the range, as interpreted in the map and memoir of the Geological Survey.
To trace with greater completeness the position and constancy of the beds of slate in the Arenig series ; a subject of considerable local and practical importance, when we remember that those who are engaged in slate-quarrying have so far had to rely mainly on their personal and unaided observation.
In order to make the
On the Igneous Rocks of the South of the Isle of Man
Authors: Hobson Bernard 
Published: October 2009

I. P
revious
L
iterature
.

T
hough
the igneous rocks of the Isle of Man have been cursorily described by Berger, Henslow, and Macculloch, the most satisfactory account of them is contained in the work of the Rev. J. G. Cumming § and in the paper by Mr. Horne ∥. The Rev. J. Clifton Ward ¶ has also given an interesting sketch of their geology.

I n the “Journal of the Liverpool Geolo~cal Association,” vol. ix. (1888-89) pp. 41-47, is a paper entitled “Notes on some Manx Lavas,” by Isaac E. George, but it hardly contains much information.
In the “Proceedings of the Liverpool Geological Society,” vol. vi. pt. i. (1888-9) pp. 123-131, is a paper on “An Examination of some Volcanic Rocks of the Isle of Man,” by Messrs. Dickson and Holland, containing analyses of 5 specimens, and a description by Mr. Rutley of 10 specimens.

II. M
ain
F
eatures
of the G
eology
of the D
istrict
.

The greater part of the Isle of :Man consists of slates, which are usually held t~ be of Lower Silurian age, but in the south of the island Carboniferous rocks occur. They occupy an area of about 7 square miles and overlie the slates unconformably, extending from Cass-ny-Hawin on the east coast to near Athol Bridge over the Silverburn on the north-west, thence, bounded on the west by a fault which throws them down against the slates, to Strandhall. Bounded on the south by the sea, they extend eastwards from Strand-hall to the peninsula of Langness, where
On a Spherulitic and Perlitic Obsidian from Pilas, Jalisco, Mexico
Authors: Rutley Frank 
Published: October 2009

The specimen upon which the following observations were made is a greyish-green or leek-green obsidian with a waxy lustre, containing numerous deep brownish-red sphrulites, ranging from the size of peas to smaller dimension. It was collected by Dr. A. E. Foote, to whose kindness I am indebted for it.
Under the microscope the thin section shows banded and perilitic structures, the former being delicate and even, while the latter is developed with a perfection which I have never seen equalled. Each perlitic area, as a rule, includes several centres, sometimes five or six, or more, around which perlitic structure has been developed (Pl. XVIII. fig. 1). A similar complex perlitic structure has alredy been noted in certain dacites by Prof. Judd. The glass of the obsidian contains numerous globulites and longulites, which are densely crowded together along the fluxion-banding.
The perhtic fissures appear in all cases to have been filled tip with siliceous matter, showing, in some instances, minute crystalline rods or fibres, passing from the walls towards the middle of the fissure, where a distinct line of arrest parallel to the walls may be seen. This secondary crystalline matter exhibits double refraction, so that the perlitic structure appears brightly illuminated and in strong relief against the glass of the obsidian, when viewed between crossed nicols (Pl. XVIII. fig. 2).
I t is only here and there, however, that these somewhat regular growths from opposite walls of the cracks are to be seen. At times the minute crystalline rods or
On the Gravels south of the Thames from Guildford to Newbury
Authors: Monckton Horace W. 
Published: October 2009

The greater part of the hill-gravel in the district to which the following communication refers belongs to the Southern Drift of Prof. Prestwich, and a very large portion of the valley-gravels consist of materials mainly derived from the Southern Drift. It is only on the hills between Cookham and Twyford, and at Tilehurst near Reading, that we get the Westleton Shingle of that author or the Glacial Gravel.
The distinctive features of the Southern Drift are given at length by Prof. Prestwich. Briefly it may be said to consist of materials derived from the Wealden area of Kent and Surrey, the Chalk country to the north and west of the Weald, Eocene formations of the neighbourhood and older gravels, or possibly older clay with flints and surface-debris. It is, I believe, the gravel of old rivers which had little or no relation to our present river-system, whilst the gravels of the valleys, terraces, and minor plateaux are the work of rivers having some, though often a distant, relation to those now in existence.
The Southern Drift of the district under consideration may conveniently be divided into three classes. The first includes certain patches on very high ground along the margin of the Wealden area, obviously the oldest gravels in the district. The second consists of material largely derived from the Lower Greensand of the Wealden area and extends as far west as Strathfieldsaye; while in the third, which lies west of that place,there is an absence of such material. It
The Subterranean Erosion of the Glacial Drift, a Probable Cause of Submerged Peat- and Forest-beds
Authors: Shone Wm. 
Published: October 2009

The Drift of the N.W., N.E., and Central England covers a large area of the Triassic Series, composed of interstratified hard and soft rocks, giving rise to very unequal denudation of the various members of the series. The Triassic area is consequently of an undulating character, and the Drift which covers it like a mantle partakes of the undulating nature of the rocks it overspreads. The Drift upon the sides of the valleys has, at short intervals, been cut into minor valleys by the rain coursing down their slopes. The minor valleys
cut out of the Drift
should be carefully distinguished from the larger valleys
covered with Drift
, for the latter appear to follow the contour of the pre-Glacial land surface.

Every minor valley has its small streamlet, which in dry weather is most frequently a very insignificant watercourse; during heavy falls of rain, however, such tiny rivulets become swollen into large and rapidly-flowing brooks, charged with densely turbid water derived from the clays, sands, and gravels of the Drift.
The section (fig. 1) is across two such minor valleys. At the S.S.E. end is situated the sandpit, with a face of the pit at right angles to the line of section. Under the surface-soil the pit has a covering of Upper Boulder Clay (varying from 2 to 6 feet in thickness) resting upon Middle Sands and Gravels. About 6 feet beneath the base of the Upper Boulder Clay there was a band of clay a few inches thick in
On the Rocks mapped as Cambrian in Caernarvonshire
Authors: Blake J. F. 
Published: October 2009

Conclusions
The above observations prove that there is a definite succession in the Cambrian series, which is the same in the isolated portion east and south of Bangor as in the main mass. Whether we see the base or not depends on the age assigned to the Dinorwig felsite. If that be Cambrian there might be beds of the same system below it, but there probably are none, since we certainly see the base at Beaumaris. Whether we see the top or not depends on whether the Bronllwyd Grit, which belongs to the overlying group, is conformable or not, and there is no evidence tat it is. In any case, no intervening beds above the Purple and Pale Slates are known in North Wales.
It is also proved that the rocks to the west of the felsite belong to the lower part of the series, and those to the east to the upper, both being determined in areas where the felsite is absent, and hence it appears probable that the felsite mass is a volcanic complex belonging to the middle of the Cambrian period.
Thus my former conclusions, though somewhat modified, are shown to be substantially correct.
The New Railway from Grays Thurrock to Romford: Sections between Upminster and Romford
Authors: Holmes T. V. 
Published: October 2009

This railway, which has been in process of construction during the last two or three years and is still incomplete, diverges, from the London and Tilbury line about a mile west of Grays Thurrock station. Thence its range is either northerly or north-westerly. It crosses the Mardyke about half a mile west of Stiffbrd, and its course lies westward of the villages of North and South Ockendon and eastward of Stubbers and Cranham Hall. From Cranham Hall to Romford its direction is more westerly. At Upminster it joins the railway from Barking to Langdon Hills and Pitsea, and then, leaving it again close to Upminster station, keeps on the northern side of the road between Upminster and Hornchurch, and crosses that ranging northward from the last-named village at Butts Green. Then, passing close to, but southward of, the farmhouse called Great Gardens, it joins the Great Eastern Railway about half a mile east of Romford station. The portion of the line south of Upminster is in a more advanced state than that between Upminster and Romford, the mile nearest Romford being at present (Feb. 1892) in the most backward condition.
Having described elsewhere the sections seen between West Thurrock and the Mardyke, I will only remark with respect to that part of the line that the junction of the Chalk with the Thanet Sands was once visible where Back Lane crosses the railway. Thence, to the end of the cutting north of Back Lane, Thanet Sands (below gravel) appeared. The
On the Microscopic Structure and Residues Insoluble in Hydrochloric Acid in the Devonian Limestones of South Devon
Authors: Wethered Edw. 
Published: October 2009

The complicated nature of Devonian Geology in South Devon is well known. In this paper I shall confine my remarks to the microscopic examination of the limestones, and shall not enter on the stratigraphical and palæontological problems which have been worked out by such geologists as De la Beche, Jukes, Godwin-Austen, Holl, Champernowne, Etheridge, Ussher, Davidson, Whidborne, H. B. Woodward, and others.
For the purpose of collecting specimens of limestone to be examined I spent a mouth in South Devon during the summer of 1890, and I desire to express my thanks to Mr. W. A. E. Ussher, of H.M. Geological Survey, for the very ready assistance and friendly advice which he gave me.
2. Detailed Examination of the Organic Structure

(a)
Hope's Nose Limestones
.—At Hope's Nose, near Torquay, there is a quarry opened in limestone of varying light and dark colour, and this is capped by a shaly limestone, which Mr. Ussher regards as belonging to the Calceolen Kalk, “apparently completely inverted upon massive bedded limestone containing
Heliolites porosus
.”

Commencing with the
Calceola
Beds, as representative of the basement limestones, thin sections, seen through a microscope, show a light grey, finely-crystalline groundmass traversed by fissures filled with calcite. In the groundmass are ferruginous patches and minute rhombohedral crystals, apparently of dolomite.

Passing to the limestones below—which, it must be remembered, are assumed to be above the
Calceola
Beds when in their normal position—thin sections of the lowest beds exposed show them to be composed of broken calcareous fragments, the structure
The Rise and Fall of Lake Tanganyika
Authors: Carson Alexander 
Published: October 2009

After alluding to certain observations of Cameron, Livingstone, and Stanley on the changes of level of Lake Tanganyika, the writer states that the most interesting point in connexion with the rise and fall of the lake is the question:—How is it possible for a great lake to rise 30 feet above its normal level by the blocking up of its outlet?
This is to a large extent accounted for by Cameron. He says: “On going down the river [Lukuga] we found that it was blocked by vegetation similar to that on which we had crossed the Sindi, and also to that over which we had had to pass to reach the shore from our boats at the southern end of Lake Tanganyika, and which I afterwards found existed on Lakes Kassali and Mohrya. The presence of this mass of vegetation is easily accounted for. Every day that there is a gale of wind, and the consequent sea on the lake, blocks of this peculiar growth are detached, and such as survive the passage to the outlet getting jammed together commence to grow, and form a sort of porous stopper in the neck of the outlet.” He then quotes Sir Samuel Baker's experience on the Nile when the whole channel “was blocked up and the expedition to Gondokoro impeded for a year, the country above the stoppage having been converted into a series of swamps and shallow lakes, while Egypt was suffering from all the evils of a low Nile.”
Only
Note on the Nufenenstock (Lepontine Alps)
Authors: Bonney T. G. 
Published: October 2009

A Change for the worse in the weather, as mentioned in my paper en ‘Crystalline Schists and their relation to Mesozoic rocks in the Lepontine Alps,’ prevented :Mr. J. Eccles and myself from completely examining the Nufenen Pass. In the summer of 1891 we were enabled to make an excursion thither from Ulrichen in the Rhone Valley. Though our visit was necessarily a brief one, for even to the top of the pass it is nearly three hours’ steady walking and an ascent of over 3600 feet from Ulrichen, yet, as the present paper does something to finish off an obviously ‘ragged edge’ in my former communication, I venture to bring the results before the Society.
The upper part of the Nufenen Pass (8006 feet) is a nearly level ‘corridor,’ north of the Nufenenstock (9400 feet), the highest point being at the western end, though the eastern one, above the ascent from the Val Bedretto, is not many feet lower. We were obliged on the former occasion to give up work soon after entering the ‘corridor’ from the latter end. On our second visit we found that the rain had begun at a very inconvenient moment, for another hour of fine weather would have sufficed for clearing up our principal difficulties.
On the northern side of this ‘corridor,’ as stated in the above-mentioned paper, is a gneiss, south of which is a little rauchwacke. This can be traced some distance westward down the slopes. It contains rather numerous fragments of
On some Schistose ‘Greenstones’ and allied Hornblendic Schists from the Pennine Alps, as illustrative of the Effects of Pressure-metamorphism
Authors: Bonney T. G. 
Published: October 2009

That a rock originally augitic may become hornblendic is well known, but the cause of the change is less certain. Some authors seem disposed to attribute it, almost as a matter of course, to the direct effects of pressure; that it is so in some cases can hardly be doubted, but that this explanation universally applies must not be hastily assumed. It may, for instance, be demonstrated, as in the classic case of the Scourie Dyke, that a dolerite has been converted into a hornblende-schist, but the question of the efficient cause may still remain open. At the Lizard, as the present author has endeavoured deavoured to show, augite is replaced by hornblende, as in certain of the gabbros, under circumstances which make it highly improbable that pressure has been operative to any appreciable extent. Hence, although schistose ‘greenstones’ have already attracted considerable attention, it may be worth while to describe certain cases in which pressure must have been an important agent of change, in the hope of ascertaining some mineral or structural characteristics which may help us in recognizing metamorphism due mainly to mechanical causes.
The first group of specimens to be noticed in the present paper was obtained in the summer of 1891, when Mr. J. Eccles and myself spent some time at Saas Fee, in the Vispthal. The structure of the great mountain-mass drained by the two branches of the Visp is rather complicated. The rocks are almost wholly crystalline; gneisses appear to occupy the lowest position