bluuebunny/crossref_metadata_2025_split huggingface dataset:
On the New Red Sandstone of the Southern Portion of the Vale of the Nith
Authors: Harkness Robert 
Published: October 2009

Abstract

T
he
sandstone occurring in the southern portion of the Vale of the Nith forms the north-west extremity of the great triassic formation which, commencing south of Appleby in Westmoreland, passes northward, having the mountain limestone for its eastern boundary, until it reaches Dumfriesshire. Its western boundary is also mountain limestone until it comes in contact with the eastern extremity of the West Cumberland coal-field, from whence it turns westward, skirting the edge of this formation, until it reaches the sea near to the entrance of the Solway Firth, under which it passes and again reappears in the southern portion of Dumfriesshire.

The eastern/imit of the new red sandstone in Dumfriesshire is the parish of Canobie, where it is seen in the bed of the river Esk at Canobie Bridge. Its northern extremity in this parish is met with a little higher up the river at a place called Knottyholm, near to which the Canobie coal-field commences. The new red sandstone forms the southern portion of this parish ; from whence it ranges westward, and passing through the greater portion of the parish of Half Morton, is again seen and worked extensively in the adjoining parish of Kirkpatrick Fleming. The upper portion of this parish consists of mountain limestone, which forms the northern boundary of the sandstone, and this limestone extends for a considerable distance in a southwesterly direction, forming the northern extremity of the sandstone in the parishes of Annan and Cummertrees. The sandstone occupies the whole of the former parish except a small portion of its northern part, and in the latter it is confined to the southern end. Besides the parishes already mentioned, of which it constitutes a part, it occupies exclusively the parishes of Gretna and Dornock which lie upon the margin of the Solway Firth. The parish of Ruthwell, west of Cummertrees, and bordering the Firth, is composed principally of mountain limestone, and it is probable that near here the sandstone again passes raider the waters of the Solway before it reappears in Caerlaverock, west of Ruthwell ; and here commences that portion of the new red sandstone to which this account more immediately refers.
On the Geology of Spain
Authors: Ezquerra del Bayo Joaquin 
Published: October 2009

I
n
order to give a general idea of the geological constitution of our country, it may be considered as divided into three principal divisions, viz. the Crystalline or Gneissoid formations; the Transition formations; and the Secondary. The first predominate almost exclusively in the western portions (not including Portugal), in the whole of the ancient kingdom of Galicia, and extend through Astorga, Zamora, Salamanca, Placencia, Cáceres, Mérida, Lleréna, Aracéna, and Rio Tinto, to the north of Seville and to the neighbourhood of Italica, the birth-place of the Emperor Trajan, now called Sancti Ponce. It must however be observed, that as yet, for want of detailed observations, we have no definite lines to mark the limits of the three formations above mentioned. We can only say that the gneiss rocks occupy about a fifth of the surface of the soil, extending longitudinally from north to south, but throwing out, as it were, ramifications towards the east.

These gneiss rocks are probably secondary or primary formations, altered by the plutonic rocks which have penetrated them. These are generally ordinary granite, more or less coarse-grained, and sometimes traversed by veins or dykes of porphyritic granite. Only at the northern extremity, viz. between Aracéna and Lleréna, in the villages of Zufre and Santa Olalla, is a great syenitic outburst visible.
The most important of these granitic ramifications to the east is that which passes by the Sierra de Gridos, Sierra d’ Avila, and the Guadarrama, to Somo Sierra, in a direction from south-west to north-east
Notice of the Discovery of Reptilian Foot-tracks and Remains in the Old Red or Devonian Strata of Moray
Authors: Brickenden Lambart 
Published: October 2009

I beg to submit to the Geological Society a brief notice of a discovery of considerable interest, which I made during the last year, but was prevented from communicating before the close of the last Session; a delay which I do not now regret, since a recent fact has come to light which invests with additional importance that which it was my object to lay before the Society.
In 1850 I discovered in the quarry of Old Red at Cummingston near Elgin, a slab of sandstone bearing a beautiful and distinct series of quadrupedal foot-prints, of which a representation, one-sixth the size of the original, is given in the annexed sketch (Pl. III.).
The slab exhibits on the surface, in a very striking manner, thirty-four foot-prints of a quadruped, traced in an uninterrupted succession across the stone. The impressions of the right feet alternate with those of the left, from which they are separated laterally by an interval of three inches, the length of each stride or pace being about four inches. The imprints of the fore and those of the hind feet are nearly in contact, and bear a precisely similar relation throughout: the size of the foot-marks of the former in proportion to the latter is as three to four; the hinder being about one inch in diameter.
Description of the
Telerpeton Elginense
, a Fossil Reptile recently discovered in the Old Red Sandstone of Moray; with Observations on supposed Fossil Ova of Batrachians in the Lower Devonian Strata of Forfarshire.
Authors: Mantell Gideon Algernon 
Published: October 2009

THE highly interesting fossils from the Devonian rocks of Morayshire, which Mr. Patrick Duff of Elgin has with great courtesy allowed my friend Captain Brickenden to transmit to me, with a request that I would examine and describe them, and lay the results before the Geological Society of London, consist of the remains and impressions of nearly the entire skeleton of a
lacertian reptile, 4½ inches in length, in a block of crystalline sandstone broken into three pieces.
On the largest fragment, P1. IV. 9, the spinal column with the ribs, from near the occiput to the sacrum, is distinctly shown; the pelvis is but obscurely indicated; the caudal vertebræ with their apophyses, comprising apparently two-thirds of the entire tail, are manifest. There are no traces of the bones of the pectoral arch, nor of those of the feet. Of the left anterior extremity, impressions of the distal half of the humerus, and of the proximal portions of the radius and ulna are the only vestiges ; the right arm is indicated solely by a hollow left by the humerus. The forms of the bones of the hinder limbs are demonstrated by the deep imprints of the femora and tibiæ, and less distinct traces of the fibulæ
The piece of sandstone, P1. IV. 8, that has been broken from the upper part of the block, Pl. IV. 9, nearly parallel with the plane of the spine, displays the corresponding impressions of the vertebral column and ribs, pelvis, bones of the
On the Discovery of Gold in Australia
Authors: Clarke W. B. 
Published: October 2009

In April 1841, Mr. Clarke undertook his first journey of exploration from the east coast of Australia to the westward, in the parallel of Port Jackson. On that occasion he became first acquainted with the geological position of the Carboniferous series of New South Wales with respect to the older rocks composing the axis and western flank of the great chain called the Blue Mountains, which also, in consequence of their extension N. and S. through many degrees of latitude, have been appropriately denominated “the Australian Cordillera.”
Although, on the occasion alluded to, says the author, my observations were made without much precision, I nevertheless became aware that the axis consisted of elevated schists of various kinds parallel with the meridian, together with some limestones, and that granitic rocks of a younger epoch had intruded into them, and were accompanied by dykes of quartz. The presence also of greenstones, diorites, syenites, porphyries, basalt, and other igneous products was also detected. There was evidence also of the schists having undergone various transmuting influences, and of the granites having suffered from causes which had in places produced disintegration. The Carboniferous formation was exhibited as resting upon the older rocks, either reposing unconformably upon the tilted schists or granites, or passing into the ancient conglomerates derived from the latter.
On the Superficial Accumulations and Surface-markings of North Wales
Authors: Ramsay A. C. 
Published: October 2009

During several summers, while investigating the more solid geology of North Wales in connexion with the Geological Survey of Great Britain, my attention has been occasionally directed to the subject of the action of ancient glaciers in that country, which were first described by Dr. Buckland in 1841; and I have especially endeavoured to discover traces of a sequence of events characterizing the glacial epoch.
On both sides of the Menai Straits, the low ground of Anglesea and Caernarvonshire is often covered by a coating of “drift,” composed of beds of sand, gravel, and occasionally of clay, mingled with boulders, and sometimes bearing marine shells characteristic of the period.
On the Silurian Rocks of the South of Scotland, and on the Gold Districts of Wanlockhead and the Lead Hills
Authors: Harkness R. 
Published: October 2009

Mr. Harkness considers that the mineral axis of the system of Silurian rocks in the south of Scotland is the syenitic mass of Criffel. The rocks lying next to the syenite are in a highly metamorphic state, but wherever bedding can be traced, it is found that the strata on the south side dip to the south, and on the north side to the north; which last northerly dip (or to speak more correctly N.N.W. dip) continues with little exception to the northern margin of the Silurian rocks.
The lowest regularly stratified beds which can be observed on the north of Criffel are near Woodside Hill, in the parish of New Abbey, Kirkcudbrightshire, where the dip is N.E., but at no great distance to the west of this the usual N.N.W. dip obtains. By following these beds northward from Lochaber (where the syenite again occurs), an ascending section is procured for six miles, the dip exceeding 70°. The rocks consist of thick and thin greywacke sandstone (in contact with the igneous rock), frequently showing the laminæ of deposition, succeeded by thin-bedded flaggy greywacke, resembling flinty slate. Then follow in succession (at Longwood) greenish-grey, curved, laminated beds, intersected by calcspar veins,—a series of chloritic shales, interstratified with thin beds of fine-grained greywacke sandstone,— shales,—and lastly sandstone and flaggy beds, which form the hills up to the Nick of Bennerick.
On the Geology of some parts of Central India
Authors: Sankey R. H. 
Published: October 2009

Abstract

I
n
this paper the author gave a very general sketch of the distribution of the different classes of rocks and soils of Central and Southern India. The “red-soil” and calc-tuff(Kunkur) of the granitic districts, the “black-soil” of the basaltic districts, the “laterite” of the Konkun coast and other districts, called also locally “iron-clay” and “lithomarge,” and perhaps the diamond-breccia of Southern India, are superficial deposits.

The age of the immense basalt or trap formation of Central India is unknown. An extensive freshwater deposit (or series of deposits occurs in this trap-formation; and Lieut. Sankey observes that it is invariably found between two layers of trap. The author considers it probable that these freshwater beds are the remains of a lacustrine or fluviatile formation extending from Bombay to Rajamundry, or entirely across the peninsula from sea to sea, in one direction; and from Medcondah (in the centre of Hydrabad) to Saugor (towards the north of Bundelcund in the other direction); an extent of nearly 700 miles in length and 500 in breadth.
These freshwater beds in the trap have been especially observed at Nagpoor, Jubbulpoor, and in the Sichel Hills.
In the same district sandstone and limestone occur to a great extent—the former known as the diamond-stone; the latter characterized by fish-remains of Jurassic age. But the relations of these rocks with the basalt are not evident.

Lieut. Sankey makes especial reference to the late researches of the Rev. Messrs. Hislop and Hunter in the vicinity of Nagpoor¶, aud concludes by detailing the observations made by himself and Dr. Jerdon in the Kamptee, Oomrait, and Pachmurra districts, on the coal, coal-shale, and sandstone there met with. The coal occurs about five miles north of the village of Oomrait (which is in Lot. 22° 8′. Long. 78° 46′, and fifteen miles to the west of Chindwarra), on the bank of a stream at the village of Chota Burkoi, where it outcrops as a layer about 1 foot thick. The shale and sandstone with which the coal is associated have afforded numerous remains of plants, as
Pecopteris, Glossopteris, Sphenopteris, Phyllothecæ
, and
Vertebrariæ
, such as occur in the Burdwan coal of N.E. India.

On the north and west of Kamptee this fossiliferous sandstone forms a series of great thickness. Sandstone also makes its appearance ten miles south of Nagpoor.
In the Pachmurra Range the sandstone is calculated by the author to be at least 2700 feet thick, and he thinks it probable that it is continuous with the coal-fields of Jubbulpoor, &c. to the North, and to the N.W., with that beyond Baitool. Lieut. Sankey, together with Dr. Jerdon, traced the sandstone almost up to Hurdagur, twenty miles S.W. of Pachmurra ; and he does not doubt that, by its continuation under the trap.range of Muttoor, it is connected with the coal-bed of Oomrait.
On the Geology of Rainy Lake, South Hudson Bay
Authors: Bigsby J. J. 
Published: October 2009

G
eographical Position
, &c.—Rainy Lake, or Lake Lapluie, is placed on the great commercial route from Canada to Prince Rupert's Land and the north-west fur countries.

It is 225 miles west of Lake Superior, and 85 miles south-east of the Lake of the Woods, from the head of Rainy River; but at Nahcatchewonan River it is only 37 miles distant from that lake.
This lake, 50 miles long by 38½ miles broad, is 294 miles round by canoe-route. Its form, like that of most bodies of water resting on plutonic rocks, is extremely irregular, being in three great troughs (with deep lateral indents), one of these running easterly, and the other two in a northerly direction. See Map, Plate X.
The immediate shores are usually low, rarely cliffs or earthy banks; but they rise in shapeless masses of rock, often naked, with broad marshy intervals; or in ridges, which become hills 300-500 feet high at distances from the lake varying from half a mile to four miles.

The low grounds are well covered with small trees, such as are common in these regions, and the higher abound in
Vaccinecæ
and other useful fruit-bearing bushes.

Rainy Lake is 1160 feet above the level of the sea, according to Capt. Lefroy. Its water is pure and clear, bul seldom deep, and the spring-freshets rise to the height of from 3 to 5 feet. Its magnetic variation is 10°-12° E.
We counted 515 islands; but there are more. There are mostly small and marsy
On Pipes and Furrows in Calcareous and Non-Calcareous Strata
Authors: Trimmer Joshua 
Published: October 2009

I
propose
, in this communication, to give a brief summary of the evidence on which I rely for proof of the formation of those remarkable cavities in the chalk, known as pipes and sand-galls, by the mechanical action of water, before the matter which fills them was deposited. I shall describe the various forms which they assume, the different strata, besides the chalk, in which they are found, and the various deposits of the tertiary epoch with which they are filled.

1.

The Pipes are terminations of Furrows
.—In the first place, then, they are the termination of furrows, which widen and deepen as they approach the pipes. This becomes evident, when we have an opportunity of seeing a ground-plan of them, in consequence of the removal of the matter covering the chalk, without disturbance of the surface of the rock. Until I drew attention to this fact*, they had only been studied in sections; and when seen in section, they frequently present very deceptive appearances.

It was the connexion of these furrows with pipes and other cavities in the chalk which caused me to venture to dissent from the theory of their formation by acidulated water percolating the strata above them, as promulgated by Sir Charles Lyell, and adopted by some of our most eminent geologists.
Detailed descriptions of several such cleared surfaces of chalk in Kent and Norfolk, which I had watched from day to day, during several weeks and even months, while the clearing was
On the Physical Geology of the Himalaya
Authors: Strachey Richard 
Published: October 2009

Abstract

T
he
author having, in a previous communication to the Society*, described the geological structure of a part of the Himalaya mountains, in the present paper he proposed to complete that sketch, at the same time taking a rather larger field of view, offering some explanation of the manner in which the chain in general had been raised to its present position—first, with reference to the mechanical action of the forces in operation; and secondly, as to the epochs at which the upheavement took place.

Attention was first directed to some of the more prominent points of the physical structure of the great mountain mass, of which the Himalaya forms a portion. Among these were specially noticed :— 1st. The general form of the section of the mass, which shows that the Himalaya mountains are merely the southern slope of a great protuberance, the summit of which forms the table-land of Tibet, while the northern slope is a mountainous region, marked on our maps as the Koneulun, similar to the Himalaya, and terminating in the great plains of Central Asia. 2nd. The parallelism to one another, and to the outer edge of the mountain area, of the great ridges or lines of elevation; of the great valleys or lines of drainage, which are also lines of rupture; of the strike of the strata; of the lines of igneous action; and of the distribution of the various deposits, considered both in reference to their mineral character and geological age. 3rd. The arrangements of the drainage, in accordance to which the crests of the northern and southern slopes of the great mass form two main lines of water-shed, proposed to be termed the “Turkish and Indian Water-sheds,” to the north and south of which, respectively, the rivers flow off directly to the plains of Turkistan on the one side, and to those of Northern India on the other; while the waters of the summit of the table-land are collected into two streams alone, the Brahmaputra and the Indus, which are discharged from the mountains at two distant points, at opposite ends of the chain. 4th. The constancy maintained for great distances along the length of the chain, both in the geological structure, and in the elevations to which the mountains rise; which last character is particularly shown by the almost perfect horizontality of some of the most elevated stratified deposits, by the extremely small slope of the main drainage-channels of the Tibetan table-land, and by the general similarity of the altitudes even along the most rugged ridges.
On the Geology and Mineralogy of Mount Alexander, and the adjacent Country, lying between the Rivers London and Campaspe
Authors: Selwyn Alfred Richard Cecil 
Published: October 2009

T
he
whole of the above district is occupied by four different geological formations—

1.
Granite

2.
Metamorphosed palæozoic strata.

3.
Basalt

4.
Auriferous drift

The extent of country occupied by the first three of the above formations may be seen on referring to the accompanying map; [by which it is shown that Mount Alexander forms part of a granitic range, extending from the River Coliban, on the east, to the Loddon on the west, with a breadth varying from four to twelve miles, and describing an irregular semicircle, with its convexity to the north. The granite is bounded on all sides by metamorphic rocks, and at its eastern extremity it is overlaid by patches of basaltic lava, amongst which the Coliban runs. The basalt occurs also to the east of the Coliban in still greater extent, overlying the metamorphic rocks along the course of the Campaspe River. At the western limit of the granite also, similar basalt forms the lava-plains on the Loddon.] The fourth is more or less universally distributed over the area occupied by the second.
On the Geology of some parts of Madeira
Authors: Lyell Charles 
Published: October 2009

D
uring
a stay of two months in Madeira, Sir C. Lyell had an opportunity of examining a considerable portion of the island, and extracts from his letters to Mr. L. Horner, read at this evening's meeting, contained observations on the geological structure of Madeira and the neighbouring islands of Porto Santo and Baxo. In nearly all his excursions. Sir Charles was favoured by the company of Mr. Hartung, a German naturalist resident at Funchal, who proved a most active fellow-labourer.

Sir Charles agrees with Mr. Smith, of Jordan-hill, in attributing a subaërial origin to the great mass of the volcanic rocks of Madeira. Some of the earlier igneous formations were submarine, and are associated at San Vincente, in the northern part of the island, with deposits containing corals and sea-shells. These marine strata are elevated at least 1200 feet above the sea.
A long and complicated series of volcanic eruptions, for the most part subsequent in date to the above, and which took place in the open alr, built up the island. They have given rise to a mountain-chain about thirty miles in length, running east and west. This chain in its middle and loftiest portion rises to the height of 5000, and in some peaks to more than 6000 feet. Its composition is displayed in the precipitous sides of valleys more than 3000 feet deep, and is seen to consist entirely of scoriae, lapilli, breccias with angular fragments of volcanic rocks, tuft, scoriaceous lava, and some beds of solid
On the May-Hill Sandstone, and the Palæozoic System of the British Isles
Authors: Sedgwick  
Published: October 2009

Abstract
In a former commurncation† the author and Professor M'Coy had shown that the sandstone of May-Hill contains a group of fossils of the true Wenlock type, and that it must therefore he cut off from the Caradoc sandstone, and arranged with the base of the Wenlock group; also that on the western flank of the Malverns, the upper portion of what had been called Caradoc sandstone is the equivalent of the May-Hill sandstone. In the present paper Professor Sedgwick treated of the Mathyrafal and Glyn Ceiriog sections, on the east side of the Berwyns, and sections on the western side, together with the sections of the Pentamerus limestone of Norbury and Linley, on the flanks of the Longmynd, the sections of Horderley, the Onny, and of Caer Caradoc; and lastly, the sections of Builth, Llandovery, and Llandeilo.
From the examination and considera6on of these sections, and of their fossil evidences, the author concludes that in those great physical regions there is not so much as one continuous unbroken section throughout which we can ascend in the way of passage from the Cambrian to the overlying Silurian groups ;--that there is a physical break between them exactly on the horizon oi'the May-Hill sandstone ; —and that, in exact co-ordination with that break (often distinctly marked by a discordancy in the position of the beds), there is a great change in the fossil species ;—thus pointing out the true physical and palæontological base of a Silurian system. Professor Sedgwick appended a corrected tabular arrangement of the Palmozoic rocks*, in accordance with the above ; and concluded with some remarks on the nomenclature of British geology.