bluuebunny/crossref_metadata_2025_split huggingface dataset:
On the Gold-diggings at Creswick Creek and Ballaarat
Authors: Redaway W. 
Published: October 2009

Abstract

M
r
. R
edaway
noticed first the “bluestone” or concretionary basaltic lava at Creswick Creek, which composes also the rough bouldered surface of the country to a great extent. In the plains formed of this volcanic rock, small lakes or water-holes, from 3 to 12 feet in diameter, are in some places frequent.
On the Gold-Diggings at Ballaarat
Authors: Rosales Henrique 
Published: October 2009

“B
y
the aid of machinery, and through the alteration of the mining-regulations granting extended claims, the old ground has been profitably re-worked: and, by the introduction of the frontage-system, which, according to the difficulties to be overcome, grants extensive claims on new ground, the present ‘leads,’ most of which are N.W. of the Gravel Pits, under the townships, are advantageously worked. The amalgamation of three or more claims is also allowed, the miners having then to put down only one shaft.

“The engines most in use are stationary, of from 15 to 20 horsepower, with winding and reversing gear. To the end of the winding-gear-shaft is attached the crank for the pump ; and the motion is also taken to drive a puddling machine, which is nothing but the arrastra working without mercury. The depth of sinking averages about 300 feet, of which in some instances there are as much as 200 of basalt to be cut through.
“"A t the junctions of the Frenchman's and White Horse Leads, in the Eldorado, the remains of a tree were found in an undisturbed position, with the roots fast in the wash-dirt.
On some Reptilian Fossils from South Africa
Authors: Owen  
Published: October 2009

T
his
subgenus is founded on four skulls, forming part of the collection transmitted to the British Museum in 1858, by His Excellency Governor Sir George Grey, K.C.B., from the sandstone rocks at the foot of the Rhenosterberg, S. Africa. These skulls belong, by their dentition, to the Dicynodont family, but present such strongly marked deviations from the type species of the genus (
Dicynodon lacerticeps
, Ow.) as to indicate a distinct subgeneric section; they were accordingly entered in the Museum list, and labelled in the cabinet where they are exposed to view, under the term
Ptychognathus
.

Dicynodon
(Ptychognathus) declivis, Ow. (Plate I. figs. 3, 4, 5.)

In this species, assuming the horizontality of the upper (fronto-parietal) plane of the cranium (P1. I. fig. 3 ll) as giving the natural position of the skull, the broad plane of the occiput meets the fronto-parietal plane at an acute angle, rising from the condyle upwards and backwards—a direction not hitherto observed in any reptile, and similar to that presented by the occiput in relation to the vertex in the feline and many other gyrencephalous mammals.
The fronto-parietal plane (ib. fig. 5) is bounded by an anterior ridge, 14, 15, extending from one superorbital process to the other, with a gentle convexity forward, including the interorbital space. From this ridge the facial part of the skull (fig. 3 15, 22) descends in a straight line in a direction nearly parallel with that of the occiput, but slightly diverging from that parallel as it cxtends downward
On the Ossiferous Grotta di Maccagnone, near Palermo
Authors: Falconer H. 
Published: October 2009

Abstract

D
r
. F
alconer
first described the physical geography of that portion of the north coast of Sicily in which the ossiferous caves abound, namely between Termini on the east and Trapani on the west. The geological structure of the tract had been ably investigated and mapped by Hoffmann. A great mass of Hippurite-limestone stretches from Termini to the eastern side of the Bay of Castellamare, which on the side towards Termini forms rugged precipitous or scarped cliffs skirting the sea-shore. From Cape Zaffarana to Capo di Gallo, a distance of about twenty miles, the coast-line is deeply indented by the Bay of Palermo; west of Capo di Gallo there is a smaller indentation, backed by Carini; and still further to the west there is the deep Gulf of Castellamare. At the bottom of these indentations the mountains of Hippurite-limestone recede from the coast, forming inland precipitous cliffs or rugged slopes, from the base of which stretch slightly inclined flats of marine Pliocene deposits, which disappear under the sea. These latter form nearly horizontal strata of a calcareo-argillaceous sandy breccia, full of marine shells and fragments of corals, &c. Philippi identified 209 species of Mollusca from this deposit in the neighbourhood of Palermo, the great majority being of living species. The ossiferous caves had been known from remote antiquity, and notices of them occur in Valguarnera, II Mongitore and other Sicilian historians. The botanist Cupani had figured and identified some of the bones. The author’s investigations had been directed to the caverns near Palermo and Carini. At Palermo the littoral pliocenc plain, celebrated for its richness as the “Concha d’Oro,” or shell of gold, is from a mile to one and one-half mile broad, and where it abuts against the Hippurite-rocks is from 180 to 200 feet above the level of the sea. The ancient Pliocene sea-margin is very distinctly seen at this elevation all round the bay, and the ossiferous caverns chiefly occur at from 30 to 50 feet above this level. Some of them, such as the “Grotta di Belliemi,” are at a higher level. The caves are studded all round the bay. The Hippurite-limestone hills skirting the coast are here from 1200 to 1800 feet above the sea; some of the heights more inland, such as Monte Griffone and Monte Cuccio, attain a height of upwards of 3000 feet.
On some Fossil Reptilian Eggs from the Great Oolite of Cirencester
Authors: Buckman J. 
Published: October 2009

T
he
fossils which form the subject of this notice, were obtained by one of my pupils (Mr. Dalton), from the Hare-Bushes Quarry, about one mile to the east of Cirencester.

This quarry, which is largely worked for the use of its freestone, offers a good section of the upper beds of the Great Oolite of Gloucestershire,—the alternations of their bands of stone and partings of clay marking that unsteadiness of character by which the Bradford Clay and the Forest-marble appear to have commenced their depositions, the Bradford Clay (that is, a marly bed containing the fossils originally observed at Bradford, such as the
Apiocrinus rotundus, Terebratula digona, T. coarctata
, and
T. cardium
) being only local, but still observable in many positions both to the east and west of the Hare-bushes—the most remarkable being at the Acman-street or Tetbury-road Station, about two miles to the west of the Royal Agricultural College, where the bed is about eight feet thick in its deepest part, and whence Mr. Woodward obtained no less than 127 species of fossils.

Where, however, the bluer clays set in, marking the true Forest-marble, these will be found to contain but few fossils; at the same time, their position is well marked by their always resting on the upper, obliquely laminated, bed of the Great or Bath Oolite, as shown in the following
The specimen containing the fossil eggs (see Figs. 1 and 2) was found in the stage marked 4, and consists of the characteristic stone. It is
On the Sinking at Shireoak Colliery, Worksop, to the “Top Hard Coal” or “Barnsley Coal”
Authors: Lancaster John , Wright Charles C. 
Published: October 2009

As the sinking at Shireoak to the “Top Hard or Barnsley Coal” is not only in a new district, but has also been carried through a considerable thickness of Permian rocks and Coal-measures which have not been proved elsewhere, we venture to think that our sections and some account of the strata passed through will be of interest to this Society.
In March 1854 Mr. Lancaster commenced sinking two pits for the Duke of Newcastle on the north-western side of his Worksop Manor Estate, where the Coal-measures are overlaid by a considerable thickness of Permian rocks. A bore-hole had been sunk some years previously on the same estate by Mr. John Woodhouse, to prove the minerals; and, though it was carried to a depth of more than 300 yards, no satisfactory results were obtained, no workable coal or ironstone being found.
The Permian beds are, we think, better developed here than at any colliery where they have been sunk through, though their total thickness is only 207 feet. The upper beds, as will be seen from the vertical section (p. 143), consist of thin and alternate layers of soft sandstones and red marls, which attain a total thickness of 60 feet. The Magnesian Limestone, however, forms the thicker portion. We found it divided into two principal beds; the Yellow, which was very hard and crystalline, 54 feet thick; and the Blue below it, containing bands of blue shale, 20 feet thick. Both together yielded 66 gallons of water a minute
On the Tertiary Deposits, associated with Trap-rock, in the East Indies
Authors: Hislop Stephen 
Published: October 2009

I
n
introducing the following descriptions of some fossils from Peninsular India, I shall confine my remarks to the rocks, volcanic and sedimentary, with which those fossils are connected. They have already been noticed in a memoir, which, in conjunction with my friend the Rev. R. Hunter, I submitted to the Society in 1854.

On that occasion I endeavoured to prove that there was no foundation “for the supposition that the great outpouring of basalt in India took place in the ocean,”—that the water of the lake in which it really was effused was in many places “so shallow as to allow the igneous rock to rise above its surface into the atmosphere,” and that therefore the flatness of the tops of trap-hills was not owing to superincumbent pressure, as is generally believed, but was “the effect of the well-known law by which the surface of liquid bodies is reduced to the same uniform level.” The age of the deposit formed at the bottom of the lake, before it was invaded by the volcanic eruption, I considered to be Lower Eocene; and, while inferring as a matter of course that the overlying trap was subsequent to it, I expressed the opinion that the similar rock which was frequently found underlying was more recent than both.
In opposition to this last view it is held, that the underlying trap must have been poured out first, and the freshwater deposit formed over it. This, I admit, would be the theory attended with the
On the Coal-formation at Auckland, New Zealand
Authors: Weekes Henry 
Published: October 2009

Abstract

T
he
district is formed of stratified sandy clays, of Tertiary age; they vary in colour from white to light-red. The white clays contain beds of lignite, varying from a few inches to several feet in thickness. Sections of these beds are exposed along the banks of most of the tidal inlets with which the district abounds. In some places, near the hills, the lignite is seen to rest on trap-rock; elsewhere a shelly gravel underlies it.

At Campbell’s farm a whitish sandstone lies on the lignite, and at the junction is hardened, and contains ironstone-nodules; these, when broken, yield remains of exogenous plants. A fossil resin is found abundantly in the lignite. On Farmer’s Land the lignite is 16 feet thick, including a little shale; at Campbell’s it is 7 feet thick, but thins away. There is some iron-pyrites in the lignite, but not sufficient to deteriorate its value as a coal. Similar coal has been found at Muddy Creek to the S.W.; at Mokau, about 100 miles to the south; and near New Plymouth.
The Tertiary beds of Auckland are everywhere broken through by extinct volcanos, varying from 200 to 800 feet in height. The craters are generally scoriaceous, in a perfect condition, with a depression of the rim usually to the north or east. There are also around the district other volcanic hills, rounded, scoriaceous, more fertile than the crateriform hills, and apparently of an older date.
Supplemental Observations on the Order of the Ancient Stratified Rocks of the North of Scotland, and their associated Eruptive Rocks
Authors: Murchison Roderick I. 
Published: October 2009

I may now revert to the main object of this memoir, the establishment of a clear order of succession among the oldest rocks of the North-western Highlands, And here I have the satisfaction to reiterate that not only Prof. Ramsay, who accompanied me, but also Prof. Harkness, who has since visited the north-western region to satisfy doubts in his own mind, have both come to the conclusion that my general views (as laid down in the map, Pl, XII. vol. xv.) are correct.
On a point of such great stratigraphical importance, I cannot avoid quoting the very words of Prof. Harkness, who, after visiting the west of Sutherland, wrote to me thus:—The gneiss which occupies the western portion of Sutherland is of a character so unlike that which forms the more eastern mountains of this country, that lithological characters alone would almost justify the conclusion that it appertains to a different geological epoch. Its strike is, as you have shown, at variance with that of the newer gneiss where this latter is in contact with the quartz-rocks and limestones forming the Lower Silurians.
“A t many localities where the surface allows of the relation of the upper gneiss and its immediately underlying deposits to be seen, there is undoubted evidence of a perfect sequence and conformity of the strata which appertain to the upper quartz-rock and limestone and the overlying flaggy gneiss; and this latter, in some districts remote from the quartzites and limestones, presents the same uniform dip with
On the Geology of a part of South Australia between Adelaide and the River Murray
Authors: Burr T. 
Published: October 2009

T
he
lowlands about Adelaide on the west and along the River Murray on the east consist of horizontal beds of limestone and calcareo-siliceous deposits, yellowish and reddish in colour, full of marine fossils, and of Tertiary age. Sometimes gypsum and ferruginous sand replace the limestone. These plains are arid—except where granite protrudes from the surface, presenting cavities in which rain-water collects. The author observed a similar Tertiary formation on Yorke’s Peninsula, at Port Lincoln, and to the S.E. to beyond Rivoli Bay; and it probably forms vast tracts in New South Wales and Western Australia. None of these Tertiary districts appear to exeecd an elevation of 300 feet above the sea.

In describing two volcanos in South Australia, Mount Gambler and Mount Sehanck, Mr. Burr remarked that, coming from the west or north-west, at about 20 miles from these hills a white ‘coral limestone’ [Bryozoan limestone] containing flint or chert takes the place of the limestones and calcareous sandstones with recent sand-formation previously passed over. This white limestone is remarkable for the numerous deep, well-like water-holes in it, within about twelve miles of the volcanic mountains, and about cast or west of them.
Mount Gambler has a height of 900 feet above the sea (600 feet above the plain), and has three craters lying nearly east and west and occupied with lakes of fresh water. Mount Schanck, at a distance of about nine miles magnetic south, is circular and has one large and two small lateral craters.
The author next
On the Discovery of some Fossil Remains near Bahia in South America
Authors: Allport S. 
Published: October 2009

O
n
referring to a map of Bahia, it will be seen that a line of hills runs from the Point of St. Antonio in a north-easterly direction. They form for some distance steep rocky cliffs, skirting the Bay, and continue in the same direction for several miles. They also form the seaward exposed edge of an elevated range of country, and present a steep slope to the N.W.; and are everywhere covered by red loam or sand, except where exposed to the action of the sea. These are gneissose rocks, usually exhibiting distinct lines of stratification or foliation, but not unfrequently passing into amorphous masses (see Map, fig. 1).

The direction of the general line of upheaval clearly coincides with that of the above range of hills, being N.E. and S.W.; the dip of the gneiss, where it can be well made out, being always to the N.W.
In Itapagipe Bay, near Cabrito, there is a white sandstone, interstratified with shale, the dip of which is also to the N.W. It forms a low hill, running nearly parallel with the gneiss hills, at a distance from the latter of three or four hundred yards in the direction of the dip (fig. 2). No organic remains have yet been discovered here; but this deposit has not been carefully examined.
At a distance of about two miles from the gneissose range, and running parallel with it, is the isolated hill of Montserrate (see Map, fig. 1), which extends for nearly a mile
Notice of some Sections of the Strata near Oxford
Authors: Phillips John 
Published: October 2009

I
n
England, unconformity between the Cretaceous and the Oolitic strata is discoverable at almost every part of the range of the junction of deposits, from the coast of Yorkshire to the cliffs of Dorsetshire. Everywhere evidence can be found of the wasting action of the sea on the Oolitic strata before the deposition of the superincumbent rocks, and sometimes evidence of the movement of the sea-bed (to which, perhaps, the watery agitation was due). In the country near Oxford, and from this point south-westward, the Portland Oolite has been thus greatly wasted, so as to remain in only a few detached masses. There seems reason to suppose that movements of the sea-bed of considerable extent followed the deposition of the Oxford Clay; for the Coralline Oolite fails, and the Kimmeridge Clay grows thin, and hardly traceable far from the Shotover Hills, in a direction towards the north-east.

The deposition of the Cretaceous series on the wasted Oolites was thus inevitably irregular; but in addition we have the varieties of littoral, estuary, and fluviatile deposits on the boundary-surface of the Oolites; great surface-waste, referable to the Postpliocene age; and faults which seem to be of great effect, but are not yet traced out.
Under these circumstances, it is at once a very interesting and a very perplexing problem of field-geology to trace out the detached, unconformed and wasted cappings of sand and ferruginous stone which, in several places, lie on the Kimmeridge Clay, and are not themselves covered by strata of
On some Arrow-heads and other Instruments found with Horns of
Cervus megaceros
in a Cavern in Languedoc
Authors: Lartet Mons. E. 
Published: October 2009

Abstract

I
n
a cavern of the limestone at Massat, near Tarascon in Languedoc (Department of the Ariège), examined by M. A. Fontan, the floor was found to consist of a blackish earth, with large rounded pebbles, among which were mixed, in great disorder, bones and horns of a Chamois,
Cervus pseudovirginianus, C. megaceros
, and
Bos
, together with implements of stone and bone, to which MM. Isidore Geoffroy Saint-Hilaire and E. Lartet have referred in the ‘Comptes Rendus’ of May 10, 1858.

M. E. Lartet, in his letter, has furnished drawings and descriptions of some barbed arrow-heads of bone, some having indented grooves, probably for the appliance of poison; also needles, and a flute-bevelled tool of bone, a splinter or knife of hard flint, and the horn of an Antelope hacked at the base, probably when the animal was flayed.
On the Sections of Strata exposed in the Excavations for the South High-Level Sewer at Dulwich; with Notices of the Fossils found there and at Peckham
Authors: Rickman Charles 
Published: October 2009

In the autumn of 1859, open cuttings were made at Peckham, in connexion with the “Effra branch of the Great South High-level Sewer,” for the “main drainage” of the metropolis south of the Thames; and in the following spring a tunnel (330 yards in length) was being constructed under the Five-fields at Dulwich. The beds exposed in both sections belong to the “Woolwich and Reading Series” of the Lower London Tertiaries (Prestwich).
Four shafts were sunk to facilitate the driving of the tunnel; and the following beds were exposed; but, as some of the beds are not persistent, but die out even within the extent of the tunnel, the several shafts differed as to the sections obtained from them.
On the Geology of Bolivia and Southern Peru
Authors: Forbes David 
Published: October 2009

In laying before the Society a statement of the observations made during an examination of Peru and Bolivia, in the years 1857, 1858, 1859, and 1860. I may observe that the present memoir is to be considered as the first part of a report of the results, obtained during my travels in South America during these years; and, consequently, it is believed that the conclusions here arrived at will have more weight when considered in conjunction with the observations on the geology and mineralogy of the neighbouring republics of Chile and the Argentine provinces, which subsequently I shall have the honour to lay before the Society,—more particularly as several of the geological formations not well developed or examined into in the district forming the subject of this memoir exhibit themselves much more characteristically further south.
Many points will be found not so elucidated or examined into as could be desired, and might appear to have been neglected; this, however, has not arisen from oversight, but is due to the great difficulties and frequently severe privations encountered in exploring a country in many parts entirely uninhabited or in next to a savage condition, and further by my having been limited as to time and pecuniary resources, and hampered by other occupations and by the political state of the country.
On the Position of the Beds of the Old Red Sandstone developed in the Counties of Forfar and Kincardine, Scotland
Authors: Mitchell Hugh 
Published: October 2009

The time has now come for us safely to pronounce, from palæontological evidence, upon the place of those fossiliferous flagstones, with their associated sandstones and conglomerates, which are spread over a large territory in the counties of Forfar and Kincardine, and which are referred to in a paper read by Prof. Harkness before the Geological Society on the 18th January of this present year.
The superficial area of country referred to in this paper is almost the same as that in the paper of Prof. Harkness, namely a district, comprehending all the lowland parts of the two counties, bounded on the north by the Grampian Mountains, impinging on the west on the County of Perth, and bounded on the south and east by the German Ocean. The objects of the papers are, however, very different. Prof. Harkness illustrated the stratigraphical arrangement of the rocks by numerous sections along the northern boundary-line, where they lean against the crystalline schists of the Grampians; our attention is now directed more to the beds as spread out and exhibited in the beautiful tract of country to the south-east of the mountains, and which have of late years begun to yield not a few characteristic and important fossils. It is now wished to state the palæontological data, collected by the writer in the course of several years, which lead to certain conclusions, in his opinion, sufficiently determining the position and the importance of these rocks in the geological scheme.
On the Gravel and Boulders of the Punjâb
Authors: Smithe J. D. 
Published: October 2009

In the Phimgota Valley (a continuation of the Great Kangra or Palum Valley) the Drift consists of sand and shingle with boulders of gneiss, schist, porphyry, and trap-rock, from 6 inches to 5 feet in diameter. Some of the boulders, having a red vitreous glaze, occur in irregular beds.
This moraine-like Drift lies on the Tertiary beds, which, here dipping gently towards the plains, gradually become vertical, and are succeeded by variegated compact sandstones, gradually inclining away from the plains; next come various slates, at a high angle; and gneissic rocks lie immediately over them.