bluuebunny/crossref_metadata_2025_split huggingface dataset:
On Burrows and Tracks of Invertebrate Animals in Palæozoic Rocks, and other Markings
Authors: Dawson J. William 
Published: October 2009

§Introduction

The present paper is intended to contribute some recently acquired facts to the solution of questions connected with these often problematical markings; and it will consist rather of short notes, illustrated by photographs, than of a connected discussion of the subject. I propose to notice the nature of certain markings sometimes referred to plants, under the name of
Bilobites
, —to the true nature of the
Scolithus canadensis
of the Potsdam Sandstone,—to certain tubes similar to those of modern
Sabellæ
, —to cylindrical concretions resembling trunks of trees, —and to imitative markings, and peculiar trails of doubtful origin.

§ II. Bilobites, Rusichnites, Protichnites, and Climactichnites.
(Fig. 1 to 6.)

The name
Bilobites
, proposed by Dekay in 1823, was as Newberry has shown, originally applied not to objects of this kind, but to casts of certain bivalv shells. It was therefore dropped in America; but it has been revived and has gained currency in Europe†, as a term including various forms of markings referred to different genera. The dominant characters are a band, or an oval mass, with a median longitudinal furrow or ridge, and marked with transverse or oblique furrows or strim, and with or without a marginal ridge. The writer was enabled to show in 1864 that one of the most remarkable of these impressions, Rusophycus grenvillensis of Billings, and Gruziana-like markings associated with it, were really burrows and tracks of marine animals, probably Crustaceans. He arrived at this conclusion by a careful study of the impressions made by the recent
On some Water-worn and Pebble-worn Stones taken from the Apron of the Holt-Fleet Weir on the River Severn
Authors: Marten Henry John 
Published: October 2009

In the year 1844 a weir was constructed by the Severn Commissioners across the River Severn at a place called Holt Fleet, about eight miles above the city of Worcester, with the object of impounding the water above it, for navigation purposes, to a height of 5 feet 4 inches above previous low summer-level.
The weir, a plan and section of which accompany this paper (figs. 7 & 8), is a dam of solid masonry across the river, without any sluices in it; so that the whole of the water passing down the river at that point flows over the crest of the weir and down the slope, or face of the apron, on its lower side.
The crest of the weir is 300 feet in length, and the drainage from 1870 square miles (nearly 1,200,000 acres) of country above it, extending to the Plinlimmon range, is discharged over it.
The stones of which the weir is constructed were taken from an adjoining quarry at Holt Fleet, and consist of a soft red sandstone of the Upper New-Red-Sandstone Formation, marked F. 5 on the one-inch map of the Geological Ordnance Survey.
In the year 1887, or 43 years after the stones were placed on the apron of the weir, an examination was made of them, as some of the stones had become displaced and others showed signs of decay.
The examination brought to light the fact that a large proportion of the stones on the Island side of the central
On the Unconformities between the Rock-systems underlying the Cambrian Quartzite in Shropshire
Authors: Callaway Ch. 
Published: October 2009

I
ntroduction

A
bout
twelve years ago I devoted some attention to the Archæan rocks of Shropshire, and a commnnication on the subject appeared in the Quarterly Journal (1879, vol. xxxv. p. 643). Additional results were published in the numbers for May, 1882 (vol. xxxviii. p. 119), and November, 1886 (vol. xlii. p. 481). Some details, however, remained for settlement. Of these the most important is the relation between the great volcanic system (Uriconian) and the vast series of sediments which takes its name from the Longmynd. Ten years' additional experience amongst the Archæan rocks has given me some advantage in reviewing my old evidence, and recent criticisms by Prof. Blake call for some notice.

The following is a summary of my published conclusions, with Prof. Blake's objections:—

i.
The volcanic rocks (Uriconian) of the Wrekin and Caer Caradoc are older than the Longmyndian. Prof. Blake admits that they are older than the upper part of the Longmyndian, but contends that they are not older than the lower part of that series. He accordingly separates the Longmyndian into an upper member (Cambrian) and a lower member (Monian). He furthermore expresses the belief that in one locality (Pontesbury) the felsites regarded by me as pre-Longmyndian are really intrusive in rocks which he considers Cambrian.

ii.
The granitic and gneissic rocks (Malvernian) of the Wrekin and other Salopian localities are older than the Uriconian, since they furnish rounded fragments to Uriconian conglomerates. Prof. Blake, on the other hand, holds
On the Age, Formation, and Successive Drift-Stages of the Valley of the Darent ; with Remarks on the Palæolithic Implements of the District, and on the Origin of its Chalk Escarpment
Authors: Prestwich Joseph 
Published: October 2009

§1. G
eneral
C
haracter
and
A
ge
of the D
arent
V
alley
.

I
n
former papers t I have touched incidentally upon the drift phenomena of this district, and on the occurrence of a peculiar group of flint implements found on the adjacent Chalk plateau. I now purpose to limit my observations to the circumscribed valley of the Darent, which I have had more special opportunities of studying since my residence at Shoreham.

This valley, including the district surrounding it, is of peculiar interest, from the circumstance that its geological history, beginning with pre-Glacial times, may, with few breaks, be traced to Neolithic times; as also from the light it throws upon the age of some of the Thames-Valley drifts, and from its distinctive groups of Palæolithic implements. It is moreover free from the complication produced in the valleys north of the Thames by the presence of foreign-drift elements, for here the drift is restricted to débris derived from its own drainage-area.
The Darent Valley is one of the few which run through the Chalk escarpment into the so-called Wealden area §, though it does not pass beyond the first outworks, being shut out by the range of the Lower Greensand from the central Weald. To the south of the Chalk range, the valley branches westward in the line of the main stream to near Limpsfield, and eastward to near Ightham in directions parallel with the ranges of the Lower Greensand aud the Chalk, and is terminated by watersheds which separate it in the
On Nepheline Rocks in Brazil.—Part II. The Tingua Mass
Authors: Derby Orville A. 
Published: October 2009

In a former paper under the above general title (Quart. Journ. Geol. Soc. vol. xliii. 1887, pp. 457
et seq
.), the distribution, so far as it is at present known, of the nepheline-bearing rocks in Brazil was given, together with a somewhat detailed description of the Pocos de Caldas locality. Since that time three important petrographical papers relating to this group of rocks have appeared, one of which is accompanied by a detailed geological description of the insular, and presumably later, eruptive mass of Fernando de Noronha.

In this and subsequent papers, it is proposed to treat of the other continental localities, with special reference to the geological relations and mode of occurrence of this interesting group. One of the localities enumerated in that paper—the Serra de Bocaina—should be eliminated from the list, as a recent examination shows it to be composed exclusively of gneiss and granite. The specimens reported to have come from this locality are probably from the neighbouring mass of the Serra de Itatiaia.
The peak of Tingua is one of the two prominent masses that break the somewhat monotonous, approximately even-topped out-line of the Serra do Mar, as seen from Rio de Janeiro; the other being the well-known Serra dos Orgões. Of the two, the former, although of less elevation (1600 as compared with 2232 metres), is, to the geological eye at least, the most striking, since its topographical features, and more particularly its conical form and apparent distinctness from the range to which it belongs,
On Wells in West Suffolk Boulder-clay
Authors: Hill Edwin 
Published: October 2009

On taking up my residence in the heart of the Suffolk Boulder-clay, I at once began to enquire the depths of wells, in order to learn the thickness of its mass. The nature of the answers was unexpected. The depths at which water is obtained appeared altogether irregular and capricious ; ulitmately it seemed necessary to conclude that in some cases, possibly in many, the water is met with not below but in the interior of the Clay itself.
Here is an instance. A well in an outhouse of this Rectory (Cockfield, seven miles S.S.E. of Bury St. Edmund's) gives water at a depth of 35 feet. Another, outside its grounds, 120 yards W., obtained till this depth was reached. But another, the same distance N.N.W. of the first, is only some 8 or 10 feet in depth. Boulder-clay forms the subsoil to within a few inches of the surface, which in the case of each of these wells is about 300 feet above Ordnance datum.
Other wells have the following depths, the distances and directions being measured from the Rectory :—One half a mile N.N.E. (surface about 290 feet) 50 feet ; another a quarter of a mile N. (300 feet) 70 feet. In the opposite direction, at Cockfield New Hall, three quarters of a mile S.W. (255 feet), water was found at various depths down to 35 feet, but at the New Barn, a quarter of a mile farther S.W. (aboutt 280 feet), the depth was 126 feet.
On the Inverness Earthquakes of November 15 to December 14, 1890
Authors: Davison Charles 
Published: October 2009

I. I
ntroduction
.

The earthquakes felt towards the close of last year in the district round Inverness form an interesting chapter in the recent physical history of Great Britain. Fortunately, the first undoubted shock was the most severe one, and this drew the attention of numerous observers to the slighter, but not less important, earthquakes which succeeded it. In some respects the evidence is incomplete, owing to the early house at which many of the shocks occurred ; but it is on the whole full enough to indicate in outline the succession of events and their relation to the geological structure of the district.
In studying these earthquakes the accounts given in the local newspapers have been found of some service, but I have chiefly relied on records sent to me in reply to a series of questions which were circulated as widely as possible throughout and near the disturbed area. At the end of this paper I have acknowledged in detail the help thus received ; but I wish here to offer my hearty thanks to those who have assisted me—first, for the valuable information which they have placed at my disposal, without which this paper could not have been attempted, but not less for the unfailing courtesy and kindness with which my enquiries have been received.
During the period mentioned at least eleven undoubted shocks were felt. Besides these, there were nine others, each depending on the evidence of one witness only, but they were noticed and recorded by
The Geology of Barbados. Part II. The Oceanic Deposits
Authors: Jukes-Browne A. J. , Harrison J. B. 
Published: October 2009

In a former paper we described the raised coral-reefs of Barbados; we now offer an account of the important series of raised oceanic deposits which form part of the solid framework of the island, beneath its comparatively superficial coating of coral-limestone.
1. General Descriptions of the Deposits.
(a) Geological Position.-The Oceanic Deposits form a group or series of beds which is clearly marked off from the Scotland Series below and the Coral Limestones above. They do not, however, appear as a continuous band between the other two formations, because the elevation of the island from oceanic depths was accompanied by a considerable amount of faulting, and tracts of the Oceanic Deposits were dropped down between blocks of the older Scotland Series. Waves and currents then formed a surface of erosion across the faulted mass before the corals began to grow, and consequently the reefs rest, not only on various parts of the Oceanic Series, but in many places directly on the Scotland Beds.
The unconformity between the Oceanic Deposits and the Scotland Series on which they rest is as clear as the lithological contrast between the two formations is great. The older series has been thrown into a succession of folds and flexures which in many places amount to plications and contortions, and all this compression was accomplished before the formation of the Oceanic Deposits, which often rest on the edges of highly-inclined or vertical strata. In respect of colour and lithological composition there could hardly be a greater contrast
The
Olenellus
Zone in the North-west Highlands of Scotland
Authors: Peach B. N. , Horne J. 
Published: October 2009

While tracing the various subdivisions of the Durness Series of quartzites and limestones from Sutherland southwards into Rossshire, careful attention has been paid to any indications of fossiliferous zones which might throw additional light on the age of the strata. During last season's campaign, certain sections in the Dundonnell Forest happily furnished the evidence which has been eagerly sought after.
Physical Features of the Dundonnell Forest.
Between Little Loeir Broom and Loeh Maree the members of this series traverse one of the wildest tracts in the west of Ross-shire. The Dundonnell Forest lies mainly to the south of the head of Little Loch Broom, stretching southwards by An Teallach (3483 ft.) to Loch an Nid and Creag Rainich (2646 ft.). The southern portion of the Forest is drained by the Loch an Nid river, which, finding its source in the loeh of that name, flows northwards for about three miles towards the shooting-lodge of Achneigie. The river is bounded on the east for part of this distance by a precipitous crag (1000 ft. high), and on the west by the long dip-slopes of quartzite and Torridon Sandstone of Sgurr Ban (3194 ft.) and Ben a Chlaidheimh. Near Achneigie the river bends towards the north-west, soon pouring its waters into Loch na Sheallag. From this loch issues the Gruinard river, discharging into Gruinard Bay.

The sections from which the fragments of
Olenelluz
were obtained occur along the eastern slope of the valley drained by the Loch an Nid river, between Loch
On the Basalts and Andesites of Devonshire, known as ‘Felspathic Traps’
Authors: Hobson Bernard 
Published: October 2009

I. Previous Literature. 1797. W. G. Maton. Observations relative chiefly to the Natural History, Picturesque Scenery, and Antiquities of the Western Counties of England. Salisbury, vol. i. pp. 95-97 (describes the Thorverton stone).
1811. J.F. Berger. Observations on the Physical Structure of Devonshire and Cornwall. Trans. Geol. Soc. vol. i. pp. 100-102 (describes the amygdaloid of Poucham [probably Pocombe], Upton Pyne, 1 and Thorverton).
1821. Rev. J. J. Conybeare. On the Geology of the neighbourhood of Okehampton, Devon (" memoranda on the Red Marle" at end); Annals of Philosophy, new series, vol. ii. pp. 165, 166 (describes the amygdaloid of Thorverton, Silverton, and Radden [Raddon Court] quarries).
1835. Sir H. T. De la Beche. " Note on the Trappean Rocks associated with the (New)Red Sandstone of Devonshire," Prec. Geol. Soc. vol. ii. (1833-8) pp. 196-8 (mentions the trappean rocks "near Tiverton, Thorverton, Silverton, Kellerton Park, Crediton, and Exeter," and gives the geological history of those at Washfield, near Tiverton.
1839. Sir H. T. De la Beche. Report on the Geology of Cornwall, Devon, and West Somerset (Geol. Survey Memoir)pp. 199-204, 211, 212, 215, 216, 489.
1839 ? (no date). One-inch Geological Survey Maps, Sheets 21, 22, 24, 26 (almost all the important exposures are included in Sheets 21 and 22).
1865. W. Vicary, F.G.S. On the Feldspathic Traps of Devonshire. Trans. Devon. Assoc. vol. i. pt. iv. pp. 43--49 (gives additional localities and fuller details of the macroscopical characters of the rocks).
1890. R. N. Worth, F.G.S. The Igneous Constituents
Notes on the Geology of the Northern Etbai
Authors: Floyer Ernest A. 
Published: October 2009

By the scientific expedition despatched by H.H. the Khedive in the beginning of the year 1891 the whole country between the Red Sea and the Nile, and between Kos and Kosair on the north and Assuan and Berenice on the south, was examined and mapped out. Close attention was paid to the geology, for a study of which special preparation had been made, and the simplicity with which the formations are arranged enables a fairly correct picture to be drawn of an area of 2300 square miles, although the time given to its examination extended but little over three months.
The Map which accompanies the present abridgment shows the principal places mentioned in the text, and may be useful to any one who may have time and opportunity to visit the country.
Kina-Kosair-Berenice
The principal feature is a long ridge of igneous rock running N.N.W. and S.S.E. In this ridge, porphyry at times rises up into lofty peaks. These are at Jebel Dukhan, where are the quarries of the ‘imperial red porphyry’ now worked by Mr. Brindley, F.G.S. Next southwards come the porphyry peaks of Hullus, and south again the peaks of Jebel Ferayeg, the πεντεδάκτυλον őρος of Ptolemy. Between these peaks the ridge is lower, granites and metamorphic rocks alone appearing. The ridge runs near the sea, and the valleys on the east are short, frequent, and deeply eroded, both from the more frequent rains consequent on the sea-moisture, and from the slopes being steeper on the eastern than
The Gold-quartz Deposits of Pahang (Malay Peninsula)
Authors: Becher H. M. 
Published: October 2009

The Gold–quartz formation of Pahang traverses an extensive series of sedimentary rocks, of which the low hill-country lying on the eastern side of the granitic mountain-axis chiefly consists. These rocks, probably of Palæozoic age, are for the most part thinly-bedded slates, with some sandstones, and fewer dark-coloured, impure limestone-beds. Locally they are more or less metamorphosed and contorted; quartzites, and micaceous and other schists, often intervening between the slate-series proper and the greater igneous rock-masses.
Generally the strata are regularly and evenly bedded, with a prevailing strike approximately north-and-south; they dip at steep angles, mostly eastwards, from which it would appear that they have been subjected to an upheaval, due to intrusion of the central granite. Other upheavals are traceable to syenitic intrusions, which form lesser hill-ranges between the backbone-chain and the eastern coast; while numerous dykes of trappean rock have caused minor local disturbances. There are not, to my knowledge, any indications of eruptive volcanic action in Pahang, or in any other part of the Malay Peninsula.
Besides the extensive slate-formation, the only sedimentary rock noticeable is a peculiar crystalline limestone, which apparently over-lies the first-named unconformably, and is found in isolated hill-patches, characterized by abrupt vertical cliffs and numerous caves.
All the alluvial formations appear to be of quite recent origin, and to have been undisturbed since the commencement of their deposition.
Although the Gold-quartz formation in Pahang is most frequently associated with certain characteristic dark-grey and black slate-rocks, it is not confined to these, but it is
On the Stratigraphical, Lithological, and Palæontological Features of the Gosau Beds of the Gosau District, in the Austrian Salzkammergut
Authors: Kynaston Herbert 
Published: October 2009

I. Introduction
During the latter part of the summer of 892, I was enabled by means of a grant from the Worts Fund (Cambridge University) to do some geological work in the Eastern Alps. My observations during the seven weeks or so that I spent on the Continent were confined to the Upper Triassic and Upper Cretaceous rocks of the neighbourhood of Aussee, Altausse, Hallstatt, and Gosau, in the Austrial Salzkammergut, and more especially to the Cretaceous rocks of Gosau; and it is the remarkable formation here developed that I proose to deal with in this paper.
I am aware that the subject of the Gosan Beds is by no means a new one, and that many eminent stratigraphists and palæontologists, whose researches have brought forth a copious literature and much discussion, have been before me in the same field. With the exception, however, of the remarkable researches of Murchison and Sedgwick, little, if any, detailed work has been done on these beds by English geologists. Furthermore, although the formation at Gosau and other places in the Eastern Alps has been known for a long time, yet its isolated position, peculiar stratigraphical relations, and unique fauna have always been subjects of much discussion amongst European geologists, and the question of the exact geological horizon of the beds and their palæontological relations cannot even yet be said to have been definitely settled.
It is proposed, therefore, in the following pages to give a summary of the results of the principal previous
On the Origin of Certain Novaculites and Quartzites
Authors: Rutley Frank 
Published: October 2009

A
lthough
various explanations have been offered regarding the origin of certain novaculites it seems that more may yet be said upon this subject. A useful
résumé
of the opinions held by different authors is given in the ‘Annual Report of the Geological Sarvey of Arkansas for 1890,’ by Mr. L. S. Griswold. Before attempting to explain my own views it seems desirable that I should allude briefly to the specimens upon which those views are based, and especially to the Arkansas novaculites, since Mr. Griswold's intimate acquaintance with these rocks, both in the field and in the laboratory, lends great weight to his opinions. Indeed, it may seem presumptuous on my part to question them, since I have no knowledge of the ground with which he is so familiar, and also because the material at my disposal consisted of two small specimens, while he has had mountain-ranges to work upon.

The specimen of Arkansas stone which I have examined is a bluish-white rock with a faint yellowish tinge, translucent in moderately thick splinters, breaking with a conchoidal to splintery fracture and bearing a general resemblance to chalcedony. The structure is cryptocrystalline, and it shows under the microscope the outlines of what were once cavities of rhombohedral form, now occupied by siliceous deposits of secondary origin. The specimen of Ouachita stone resembles a faintly yellowish-white or cream-coloured biscuit-porcelain, except that it exhibits barely a trace of translucency on thin edges.
Under the microscope this rock is also seen to possess a