bluuebunny/crossref_metadata_2025_split huggingface dataset:
On Supposed Casts of Footprints in the Wealden
Authors: Beckles S. H. 
Published: October 2009

Abstract

C
ertain
large trifid bodies, presenting a resemblance to the casts of the impressions of birds′ feet, are rather numerous in the cliffs to the east and west of Hastings (from the latter locality Mr. Beckles has obtained eight specimens), in a limestone containing
Cyrencæ
, remains of
Lepidotus
, &c., and Dr. Mantell has discovered a specimen in the Wealden of the Isle of Wight.

Several specimens, detached from the cliffs, have been taken from the beach; but at about four miles east of Hastings, where the cliffs are about 200 feet high, the casts occur at about 40 feet above the sea-level. They were found in a stratum of rock, overlying a bed of clay; which latter having been removed by rain and weather, the casts appeared in relief on the under-surface of the rock, just as if they were hanging from the ceiling of a room.
One detached block obtained at this place bears four of these trifid bodies in relief; they are arranged with the toes pointing in a uniform direction, so as to mark out a nearly perfect square. A distance of 2 ft. 7 in. separates the two in front, and 2 ft. 5 in. the hinder two: between the two on the right, from the toe of the hinder one to the heel of the foremost, there is a space of 2 ft. 3 in.; and between the other two the distance is less by nearly 2 inches.
The largest specimen found has a length of 21 inches.
The general uniformity of position and of character,—the constant presence of a middle or heel-like prominence and of three “toes,” the central one being always the longest, together with other uniform peculiarities,—have reference apparently to the connection of the origin of these trifid bodies with the foot-prints of birds or other animals.
Some specimens, as for instance that of which a model was presented to the Society by Mr. Taggart in 1846†, have narrower “toes” than others.
On the Till of Caithness
Authors: Cleghorn John 
Published: October 2009

Abstract

T
he
Till generally occupies the low districts of Caithness. At Lybster, however, fourteen miles south of Wick, it reaches 212 feet above the sea, with an unascertained depth below low-water mark. In the harbour it has been bored twenty feet, and it is the anchorage ground of the bay. The author finds that at Lybster and at Wick the deposit is in a trough of rock, more than a mile broad and many miles long, of the shape seen at
a, b, c
, in the annexed woodcut. At Lybster the deposit is cut through by the Burn of Reisgill, which empties itself into the harbour, and at Wick by the river of Wick; at both places the clay is found on each side of the watercourses, rising in high banks, as shown at
a, d
, and
e, c
, in the accompanying diagram.

From observations Mr. Cleghorn has had the opportunity of making, he believes the Till to be laminated, as represented in the accompanying section, and that the troughs at Lybster and Wick, previously to the denuding action of the Burn and the River, were filled up as represented in the figure.

From the position of the Till in Caithness, its lamination, and broken shells, from the occurrence of smoothed and scratched boulders in the Till similar to such as are found in the watercourses near Wick, and from the apparent elevation of the Caithness coastline, as proved by the occurrence of rocks perforated by lithodomous molluscs at various elevations above the present level*, the author infers that the Till is the wastings of coasts and the sedimentary matter of rivers deposited in the valleys of a deep sea, inhabited by the
Anarrhicas lupus
*.
On the Kelloway Rock of the Yorkshire Coast
Authors: Leckenby John 
Published: October 2009

Among the more interesting features in the geology of the east coast of Yorkshire is the Kelloway Rock, whether compared, in its extraordinary development, or in the great variety of its fossils, with its Wiltshire prototype.
The Kelloway Rock is first seen in the cliff a short distance to the south of Gristhorp Bay, and here, but for its position below the Oxford Clay, and the presence of some characteristic fossils, there is little about the thin band of calcareous pisolite in which these fossils occur to identify it with the ochreous and arenaceous deposits as it usually appears. This band, which immediately underlies the Oxford Clay, never exceeds 5 inches in thickness, and after a course of 50 yards, thins out into a bed containing much decomposed lignite, and which at this point forms a passage into the Oxford Clay above. The great mass below, presenting a thickness of nearly 30 feet, is entirely unfossiliferous. The thin deposit at the top, and the passage into beds of lignite, seem to indicate the gradual filling up of some shallow sea of that period.
From the southern extremity of Gristhorp Bay, the Kelloway Rock is seen on the cliff, from the base to a height of fifteen to twenty feet, presenting, by its laminated markings and longitudinal fissures, an appearance of artificial masonry. It gradually ascends northward (the fossiliferous band having disappeared), until, about midway in the bay, it passes inland.
The underlying Cornbrash is well developed about halfway up the
On the Extraneous Fossils of the Red Crag
Authors: Wood S. V. 
Published: October 2009

The Deposit called the Red Crag indicates the action of strong reversible or tidal currents, and is more disturbed and littoral in its character than any portion of a formation at present known; and, for its limited area, it contains a larger percentage of foreign† organic remains than any of which we have as yet a record. I know of no locality that appears to me more to resemble what was probably the local condition of the Sea of the Red Crag during the accumulation of the material herein enumerated than the conditions under which the Bay of Christchurch at present exists; and I believe that in the conflicting streams that now wash the shores of that neighbourhood may be found a cause sufficient to produce all the effects visible in the Red Crag,—only reversing the direction of the land, the sea of that period opening to the northward.
To ascertain the age of the Red Crag by the “percentage test,” could only be effected by the exclusion of a large portion of its contents; and, when we have got rid of those fossils which we know to belong to some remote anterior period, we should then have to contend against the doubtful admission of many species that may have been introduced from the deposits immediately antecedent. A large number of the shells have in all probability, as suggested by Sir Charles Lyell, been washed into the Red Crag Sea by an underwater abrasion of the older beds; and the
On a Fossil Fruit found in the upper part of the Wealden Deposits in Swanage Bay, Isle of Purbeck
Authors: Phillips John 
Published: October 2009

But few of the numerous fossil remains of Plants in the Wealden and Purbeck deposits of the British Isles have as yet been completely described. Ferns,
Equisetaceæ
, Monocotyledonous plants,
Coniferæ,
Cycadaceæ
, and Characeæ have been recognized by their leaves and stems. But fruits are uncommon. One of these is cycadaceous—
Zamiostrobus
, and there are two undetermined
Carpolithi
*.

To this short catalogue I am now able to offer one addition, taken from a nodule of ironstone in the upper part of the Wealden beds, in Swanage Bay, at the close of 1857.
The general section of the strata near Swanage, on a line from north to south, shows, in succession, the Portland rock, the Purbeck deposits, the Wealden, and the Cretaceous beds. For the purpose of this notice, only Wealden groups require attention.
The upper part of the Wealden, as seen very completely in the Northern Cliffs of Swanage Bay, exposes about 700 feet of clays frequently red or purple, less frequently blue, greenish, or very pale, alternating with sandstones of different tints, mostly soft and fine- grained, but sometimes hardened by irony impregnation, or modified by admixture of pebbles. One band contains much lignite.
In the upper part of this series, above every red or purple bed, are alternations of sandstone and pale shale. In one of the shale-beds is a course of small nodules of pyritous ironstone, one of which yielded, on fracture, the fruit in question. It is a mass of bisulphuret of iron, which threatened to fall to
On some Vegetable Remains from Madeira
Authors: Bunbury Charles J. F. 
Published: October 2009

The vegetable remains procured by Sir Charles Lyell and M. Hartung from the leaf-bed which they discovered* in the ravine of S. Jorge, in the Island of Madeira, were entrusted to me for examination; and I propose now to lay before the Geological Society the observations I have been able to make upon them. I have examined 140 specimens, by far the greatest part of them in a very imperfect state, mostly small fragments, often quite undeterminable, and, even when most perfect, no more than single detached leaves, of which, however, the veins and margin are often very well displayed. Dicotyledonous leaves predominate, but are intermixed with numerous remains of Ferns, always, however, in small fragments, insufficient to give any idea of the general form of the frond. The very fragmentary and incomplete condition of the remains of Ferns in this bed ia indeed striking. Something of it is attributable to the nature of the stone, which is by no moans fissile, but breaks quite irregularly; but something also would seem to be owing to the original conditions of the deposit. The circumstance is unfortunate, because Ferns are so variable, and show such differences even in different parts of the same frond, that great uncertainty attends the determination of them from such small fragments.
Of the Dicotyledonous leaves, a large proportion, as I have said, are too imperfect to be even described. Of those that are preserved, a few kinds may, with a certain degree of confidence, be referred to
On the Jointings in the Carboniferous and Devonian Rocks in the District around Cork; and on the Dolomites of the same District
Authors: Harkness Robert 
Published: October 2009

Jointings in the “Brownstone” and “Yellow Sandstone.”
—The country around Cork is well marked by peculiar features, which have resulted from the nature of the sedimentary rock occupying this area, and from the nature of the sedimentary rock occupying this area, and from certain physical changes which have operated on these rocks subsequent to their deposition.

The contour of the district exhibits a series of low hills generally ranging in nearly an east and west direction; and these hills are composed of Devonian sandstone. Separating the east and west ranges of hills are valleys; and in many of them Carboniferous limestones are seen, and other rocks appertaining to the lower portion of this formation,—the areas of Carboniferous rocks being the remains of much larger masses which have been removed by denudation.
The physical features of this district have originated from a succession of rolls, which have affected the strata after the deposition of the Carboniferous series.
In the deposits which here form both the Devonian and the Carboniferous formations there are seen well-developed series of jointings; these, however, are more extensive, and occur in greater variety, in the limestones of the Carboniferous group. In the Devonian rocks (which consist of fine-grained dark-coloured sandstones, well marked by cleavage, and locally “brownstones” in the lower portion which is here developed, and light-coloured sandstones, the “yellow sandstones” of the Irish geologists, in their higher parts) the jointings in general only manifest one direction, which is nearly N. and S.; and these N. and S.
On some Points in the History and Formation of Etna
Authors: Abich H. 
Published: October 2009

Your questions about Etna have carried me back to the pleasant time when I made repeated studies of that remarkable mountain, not having a presentiment of the occasion which I much later had of verifying and recognizing in another land the truth of those beautiful laws of nature, written so clearly in the configuration of the Val di Bove, and especially in the structure of the very body of Etna, visible on the slopes and steep declivities of that enormous chasm of subsidence, the Val di Bove. For, that it is indeed such, nobody will deny who has been enabled, by comparative researches in the whole circumference of the elliptical valley, to prove that idea of its formation,—an idea indeed which immediately suggests itself to the observer from the elevated edge of the Val di Bove on the border of the Piano del Lago or Schiena dell'Asino.
You are struck by some particulars in my figure of the mountain in Pl. 8 of my ‘Views of Etna*,’ and you desire to know how far those lines pointed out in your copy of it are based upon direct observation? In general, I have to confess that, when tracing those dotted lines, I may have fogotten that it was not the right place, in a profile constructed by hypsometrical measurements only, to hint at theoretical views, and that it would have been better to suppress not only the dotted line, but also those lines indicating a stratification, and intended to express a
On the Black Mica of the Granite of Leinster and Donegal; and its probable identity with Lepidomelane
Authors: Haughton Samuel 
Published: October 2009

We owe our knowledge of Lepidomelane to a single analysis, made by Soltmann, of a specimen from Petersberg, Wermland. He describes it as occurring in an aggregate of minute black scales, in small six-sided tables, with perfect basal cleavage—either hexagonal or trimetric, easily dissolved in muriatic or nitric acid, leaving a skeleton of silica.
Its composition is as follows—
This analysis gives very nearly, in atoms—
Soltmann does not appear to have ascertained whether his mica were uniaxial or biaxal, as he is in doubt whether it is trimetric or hexagonal.
In my first paper* on the Granites of Leinster, I have mentioned the black mica which is found accompanying the white margarodite of the Leinster granite, in small flakes, and noticed the curious fact that these flakes are sometimes physically imbedded in the plates of white mica, without injuring their fissility or lustre, but always effecting a reduction of about 20° in the angle between the optic axes of the latter.
Since the publication of that paper, I have ascertained the existence, in large quantities, of a similar black mica in the Co. Donegal, both in granite and gneiss; and also, through the kindness of Mr. Cotton, C.E., obtained specimens of the black mica of the Leinster granite, found in large crystals in the cuttings of the Bagenalstown and Wexford Railway, at Ballyellin, in the Co. Carlow.
The black mica of Ballyellin is found in crystalline plates, 2 in. by ½ in.; it is not only associated with, but
On the Occurence of some Tertiary Fossils at Grove Ferry, near Canterbury, Kent
Authors: Brown John , Sowerby G.B. 
Published: October 2009

My friend Mr. Prestwicn having kindly informed me of an interesting fossiliferous deposit at Wear Farm, in the parish of Chislet, I was endeavouring to find the spot in 1854, when accidentally I heard of a little sand-pit in a garden near Grove Ferry, also in the parish of Chislet (about a mile and a half from Wear Farm), on the left-hand side of a lane leading from the railway-station to the little village of Up Street, nearly a mile from the village of Chislet. Up Street is on the high road from Canterbury to Ramsgate, and six miles from the former. The pit was rather more than halfway up the side of the hill, and within about thirty feet of its top. The surface of the ground slopes down to the River Stour. Gravel caps the hill; and the Lower Tertiary sands are seen in a section, at its foot, near the railway-station, and also at a farm about half a mile to the east.
The fossil shells which I found in the little sand-pit were mostly very fragile, but in considerable abundance. They occurred both in sand and in dark red clay§ and some were nearly white, whilst others were tinted rusty red. Those which belong to Crag species appeared especially to be of a reddish colour.
The beds forming the central portion of this hill above Grove Ferry would appear, according to Mr. Prestwich's sections¶ of the Lower Tertiaries of that neighbourhood, to belong to the “Basement-bed of the London Clay,”
On the Fossil Crustacean found in the Magnesian Limestone of Durham by Mr. J. Kirkby, and on a New Species of Amphipod
Authors: Bate C. Spence 
Published: October 2009

In January, 1857, a paper by Mr. Kirkby was read before the Geological Society*, on “some Permian Fossils from Durham,” in which a few fragments were described as the remains of an extinct Crustacean. Some drawings of these were kindly submitted to me previously to their publication. One series I regarded† as being probably from the anterior portion of an Isopod; and the remainder I considered as not belonging to the same animal, but as parts of an Amphipod.

I have recently (since the reading of this paper) been allowed, through the kindness of Mr. Kirkby (to whom I applied in accordance with a suggestion from the Council of the Geological Society), the advantage of examining the original specimens of
Prosoponiscus problematicus
, together with others that have been discovered since the publication of his paper.

Having thus a favourable opportunity of reconsidering an opinion which was given from an examination of drawings only, I have been enabled to make out some points not portrayed in the drawings, which enable me to arrive at a more satisfactory conclusion. The specimens are the anterior and middle parts of an Amphipod; and none belong to an Isopod, as I at first informed Mr. Kirkby‡.
To show with any amount of certainty the correctness of this hypothesis, it is necessary that I should demonstrate, in recent Crustacea, an approximation of structure to that of the fossil. Assuming that, if certain known parts of an unknown animal agree in character with those homologically the sae
On some Points in the Geology of South Africa
Authors: Rubidge R. N. 
Published: October 2009

Abstract

T
he
author had observed in Namaqualand the occurrence of horizontal siliceous beds, covering other siliceous inclined beds, the silicification of the latter being apparently due to the infiltration of silica from the upper quartzose beds into the inclined beds below. In this communication Dr. Rubidge details the evidences that he observed of such a process having taken place, and points out how the observations on some of the Namaqualand rocks by Mr. Bain, Mr. Bell, and Dr. Atherstone, respectively, tend to support his views on this point. The inclined beds of this district are gneissic, and, in the instances referred to, very quartzose.

The horizontal sandstones of this district he correlates with the Table Mountain sandstones*; he has found in them a few obscure traces of fucoidal or other plants†.
The author then passes on to the Cape district; and, first offering his testimony to the industry and general exactitude of Mr. Bain as a geologist, he proceeds to compare Mr. Bain’s section of Mitchell’s Pass‡ with a section which he lately made for himself on two hasty journeys.
Mr. Bain figures the indurated sandstone or quartzite of Mitchell’s Pass as being at first horizontal, and then suddenly dipping at a strong angle northward, so as to underlie the Devonian schists of the Bokkeveld, at Ceres, and to divide them from the slates of the Cape district. Dr. Rubidge points out the apparent difficulty of explaining such an inclination of the quartzite, the slates underlying both the inclined and horizontal portions not presenting any evidence of a difference in dip; and he suggests that the inclined beds of quartzite have nothing to do with the horizontal quartzite, except that, being immediately beneath the horizontal siliceous beds, they have by some means been silicified from above, and thus rendered in appearance identical.
On the Relations of the different parts of the Old Red Sandstone in which Organic Remains have recently been discovered, in the Counties of Moray, Nairn, Banff, and Inverness
Authors: Malcolmson J. G. 
Published: October 2009

Conclusion

From the facts above detailed, we may conclude—

1st.
That the primary stratified rocks of the southern shores of the Moray Frith were elevated at very considerable angles previously to the deposit of the Old Red Sandstone, and that the granite by which they are penetrated also belongs to a prior epoch. The elevation of the secondary strata to their present situation, the fracture of the boulders contained in the great conglomerate, and the faults and fissures in the sandstone, may have been caused by elevations in the line of the Grampians or of the great Caledonian Valley at an epoch, most probably, posterior to the deposit of the lower Purbeck beds, which, at Linksfield, have been bent and fractured by the elevation of the subjacent cornstone.

2nd.

The great conglomerate and red sandstones, containing fish of the genera
Dipterus, Diplopterus, Cheirolepis, Cheiracanthus, Coccosteus, &c
., represent the Orkney, Caithness, and Gamrie rocks in Scotland, and the inferior division of the Old Red Sandstone of England.

3rd.
On these are superimposed a series of marly conglomerates and sandstones (containing cornstones), which are characterized by a distinct and very characteristic series of fossils, and are equivalent to the central division of the Old Red system to the south of the Grampians, and in England.

4th
and lastly, the superior siliceous conglomerates and sandstones without fossils occur, but no indications of the coal-strata.

These conclusions are perfectly consistent with the appearances presented by the strata containing ichthyolites in other parts of the north of Scotland. The Rev. Mr. Clouston, of Shandwick, informs me that the
On the Succession of the Older Rocks in the Northernmost Counties of Scotland; with some Observations on the Orkney and Shetland Islands
Authors: Murchison R. I. 
Published: October 2009

Introduction
In this memoir I propose to give a general sketch of the succession of the stratified rock-masses which occupy the northernmost counties of Scotland, or those of Sutherland, Caithness, and Ross, followed by brief notices on the Orkney and Shetland Isles, as determined by former and recent observations.
Having commenced to labour in this region in 1826, I then simply gave, as a first result, the account of the Oolitic coal-field of Brora, and of the Lias and Oolites of both the east and west coasts, including the Hebrides, with brief allusions to the bituminous schists of Caithness containing fossil fishes*. For, although I even then had traversed portions of the crystalline rocks, I considered all such masses as out of the sphere of my observation, presuming that their mineral and other characters had been adequately made known by Macculloch and others who were looked upon as authorities. In short, it was deemed a sufficient effort for a young geologist, as I then was, to point out the relative position of certain members of the Secondary series, to collect their organic remains, and to show the relations of such strata to their equivalents in England.
In the following year Professor Sedgwick and myself, devoting our efforts to the examination of the structure of the Northern Highlands, produced a memoir in which, after a brief allusion to the older and crystalline rocks, we gave the first account of the true order of the Old Red Sandstone and superposed masses, which we