bluuebunny/crossref_metadata_2025_split huggingface dataset:
Note on the Junction of the Thanet Sand and the Chalk, and of the Sandgate Beds and Kentish Rag
Authors: Hughes Thomas McKenny 
Published: October 2009

At
the bottom of the Thanet Sand there is always a bed of greencoated flints in a green and rust-brown clayey sand. The following observations have led me to infer that this bed is due to the decomposition of the top of the Chalk after the deposition of the Thanet Sand:—

1. The flints never show any traces of having been rolled or worn by the action of water, or broken up and weathered by any subaërial agency, but are, except in colour, exactly similar to those in place in the Chalk.
2. No fossils, except chalk fossils preserved in flint, have been found in it.
3. Where a nearly continuous bed of flints, or a large tabular mass of flint occurs, the base-bed of the Thanet Sand seems to be arrested by it in a manner that would suggest rather the chemical decomposition than the mechanical erosion of the surrounding chalk.

Again, to look at the question from another point of view, it is highly improbable that it could be otherwise. As water charged with carbonic acid, soaking through the Thanet Sand, reaches the chalk below, it must decompose the surface to a certain extent; and if the water can pass freely away so that new supplies, not saturated with carbonate of lime, are brought to act upon it, that decomposition must go on
ad infinitum

The only difference, therefore, between this action extending over the whole surface of the chalk where covered by Tertiary or later deposits and
On the “Lower London Tertiaries” of Kent
Authors: Whitaker William 
Published: October 2009

From what has been said above, and from a study of the sections in Plate XXII., we may gather the following facts amongst others:—

1.

That the base-bed (
a
) is the only constant part of the Thanet Beds.

2.

That the higher and fossil-bearing parts of that series (
d, e
) occur only in the east, which partly explains why it is often very hard to separate the Thanet Beds from the overlying series in the eastern part of Kent, whilst the division is well-marked westward; and that the unfossiliferous sand (
c
) thins out on the east, so that the Thanet Beds near Canterbury may be a different thing from the Thanet Beds between London and Rochester.

3.
That the bottom-bed (1) is also constant, except in the far east.

4.

That above this last there is always a sand (2), a pebble-bed (2
a
), or a mottled clay (2
b
), which replace one another.

5.
That one very thin bed (3) in the middle of the Woolwich Series seems to occur right through Kent, at all events through the eastern division.

6.
That the higher and estuarine members (4, 5) of the same series occur only in the western and central parts of the county.

7.
That the pebbles (β) at the bottom of the Oldhaven Beds (except at Upnor, where there is a little sand (α) below) are constant, being, however, locally replaced by brown iron-ore in some places near Canterbury.

8.
That in West Kent this series lies irregular on that below, whilst in the
On the Examination of Brown Cannel, or Petroleum, Coalseams at Colley Creek, Liverpool Plains, New South Wales
Authors: Keene W. 
Published: October 2009

Already acquainted with the succession of deposits visible in the various natural sections on the line and in the vicinity of the Great North Road, so far as Aberdeen, I was desirous of working out the geological position of the Brown Cannel Coal (specimens of which had been sent to me from Liverpool Plains), so that I might be able to judge of the probability of success in any search for this coal in the district of the Lower Hunter. I therefore went to Colley Creek, the station of Mr. Loder, and this gentleman at once offered to accompany me and point out the places whence he had taken specimens identical in appearance with the Brown Cannel I had seen from Hartley.
From an examination of the rocks, I was able to determine that the geological position of this Brown Cannel is below the coalseams worked in the Newcastle field—that, in fact, it forms the very base of our Coal-measures, and in such close contact with the porphyries that these latter are absolutely mixed up with the lower portion of the Cannel. I found two seams of workable thickness, tilted at a high angle, running north and south, not far from, and parallel to, each other, both of the same quality.
I was the more desirous of determining the geological position of this coal, because a large piece from a block of Brown Cannel was given to me a short time ago, which had been brought up by the buckets
A Sketch of the Gravels and Drift of the Fenland
Authors: Seeley Harry 
Published: October 2009

By the Fenland is here understood the great flat country west of the Chalk-hills of Norfolk, from Hunstanton to Cambridge, thence to Bedford, and so north to Peterborough.
Such an area offers many conditions favourable for a consideration of the subject of this paper, being bounded by Cretaceous rocks east and south, and the outcrop of the Oolites flanking the west, while the sea opens to much of the north; and the included country, being nearly flat, presents a minimum of complications.
This tract slopes gradually to the sea, which it resembles in its dreary uniformity. Every village and town, however, indicates a patch of higher land than that around it; and from Chatteris, round by Haddenham and Ely, to Littleport the level is relatively by no means low. South of this, too, by Denny Abbey, Cottenham, Rampton, Over, and St. Ives, towards Huntingdon, there is a line of higher ground. And south of this, to the east of Cambridge, are low Chalk-hills, and to the west of Cambridge an undulating country of Cretaceous outliers and hills of Boulder-clay and Oxford Clay. All the higher land north-east of Cambridge is capped with Shanklin Sand(?). And the great level itself is the Fen-clay, in which are a few isolated reefs of Coral-rag, and some stone-bands in its Oxford-Clay member, which clay covers nearly the entire area.
There are in this region three kinds of drift—namely, a Boulderclay covering the high land, a coarse gravel which caps the hills, and the fine
On a New Genus of Phyllopodous Crustacea from the Moffat Shales (Llandeilo Flags) Dumfriesshire
Authors: Woodward Henry 
Published: October 2009

Having lately received from Mr. D. J. Brown, of Edinburgh, specimens of shells, attributed to
Discina
and
Modiolopsis
, from Garple Burn, near Moffat, I examined them in conjunction with my colleague, Mr. W. Carruthers, F.L.S.; and we were enabled, by the help of these specimens and of others in Mr. Carruthers's own collection, to determine them all to belong to one organism (folded in some instances, and in others spread open), and that not a mollusk, but a crustacean allied to
Apus
&c.

The fossil might readily be mistaken for the upper valve of a
Discina
, having a strong resemblance to
Discina nitida
from the Carboniferous Limestone, and to
Discina lamellosa
, recent, from Peru; but upon a more careful examination nearly every specimen is found to have in the front of the shell a wedge-shaped opening with a well-defined border, which cuts the disk nearly to its centre.

In a specimen from Mr. Carruthers's collection (Pl. XXV. fig. 7) the wedge-shaped sector which closes this opening remains
in situ
, but the suture can still be detected.

In another specimen, from Mr. Brown's collection (Pl. XXV. fig. 5), remains of the tail-segments are preserved on the same slab with the folded shell.
The carapace, for such it must be considered, is ornamented by concentric lines of growth, which curve slightly inwards upon reaching the margin of the wedge-shaped suture in front. These concentric fines are finer and closer to each other near the apex, and more stronly marked and further apart
On a Cheirotherian Footprint from the Base of the Keuper Sandstone of Daresbury, Cheshire
Authors: Williamson W. C. 
Published: October 2009

Abstract
The specimen in question was discovered by Mr. J. W. Kirkham, in the Lower Keuper Sandstone at Daresbury Quarry. It differs from all footprints hitherto obtained from this district, in being more quadrate, and distinctly that of a scaly animal; the separated toe is also less recurved, and approaches nearer to the other toes. The arrangement of the scales corresponds very closely with that seen in the foot of the living Alligator; many of them run across the foot in oblique lines, as is common amongst living Crocodilians, leaving no room to doubt that they represent true scales, and not irregular tubercles, such as are seen on the skin of some Batrachians. Traces of other impressions of feet occur on the slab, particularly an imperfect one with much larger and more oblong scales, especially under the heel; and this difference is so very similar to what is seen in the fore and hind feet of many Saurians, that Prof. Williamson believed that they did not belong to a Batrachian animal at all, but that they were Saurian, if not Crocodilian, in every feature.
Geological Notes of the Pacific Coast of Ecuador, and some Evidences of the Antiquity of Man in that Region
Authors: Flower J. W. 
Published: October 2009

Abstract
The western slope of the Cordilleras is occupied with projected volcanic matter, presenting an irregular aggregation of boulders, gravel, sand, fine earthy matter, or ashes, and pumice. The boulders are of various sizes, and consist principally of the more ancient and the hardest plutonic rocks. Small angular fragments of granite are occasionally met with many miles from where that rock is found at the surface, and where there exists no evidence of their having been transported by water.
In some of the older strata of this volcanic rock, extending along the coast and some distance inland, occur cavities, that have been once occupied by the roots of trees, in their original place alongside prostrate stems, which indicate that there were periods of repose of the volcanic agencies by which the materials constituting this rock were distributed. Traces of forest-vegetation in the volcanic material were found on the coast and in some of the older beds of that deposit, commonly below high-water mark, and also at various points up the river Esmeraldas, and at all altitudes up to the foot of Pichincha. In this latter locality, and in beds of more recent date than those which extend to the coast, roots and stems of small trees, completely carbonized, have been found, some descending to the depth of 100 feet below the surface. Whilst the trees in this latter locality, though of more recent production, are converted into perfect charcoal, those of the older volcanic deposits are not at all carbonized.
On the Relations of the Tertiary Formations of the West Indies
Authors: Guppy R. J. Lechmere 
Published: October 2009

It may be that some apology is needed for again bringing before the Geological Society the subject of West-Indian Geology. I should not, indeed, have ventured to do so, but for the circumstance that the considerations involved do not alone concern the geology of the West Indies, but have an important bearing on several questions connected with the distribution of organic beings in Europe and Asia, and on the correlation of deposits in those countries. These questions have much interest for geologists; and I believe that the facts and arguments presented in this communication are such that my labour in bringing them together will not be lost, even if the hypothetical views I have built upon them should prove to be untenable. Moreover the present communication forms a necessary sequel to those I have already had the honour of laying before the Society.
My object now is to present some general remarks on the results obtained by recent investigations into the geology and palæontology of the West-Indian islands. But before going into these, it may be as well that I should review our knowledge of the deposits, beginning with the oldest Tertiary formations.

§2.
Eocene
Formations
.

The existence of Eocene strata in Jamaica has been demonstrated by Mr. Barrett and by Dr. Duncan and Mr. Wall Determinable fossils are rare; but three species of corals have been enumerated by Dr. Duncan, none of which are new.No strata of ascertained Eocene date have been shown to exist elsewhere in the
On the Discovery of Remains of
Halitherium
in the Miocene Deposits of Malta
Authors: Adams A. Leith 
Published: October 2009

Various forms of Cetacea have been met with in the four upper beds of the Miocene strata of the Maltese group. The discovery there of teeth of
Zeuglodon
by Scilla, and the abundant remains of one or more species of Dugong allied to recent forms and Balœnœ, show the prevalence of these mammals in the seas of the period. They are met with in the greatest numbers in the sand-bed and nodule-bands of the Calcareous Sandstone. In the latter situation I lately discovered a tooth which appeared to me to belong to the
Halitherium
, and in the sand-bed an ear-bone and caudal vertebræ of possibly the same genus. The tooth and ear-bone I have shown to Professor Owen, who has confirmed their identity with the above-named genus.

The molar, possibly a penultimate, has lost one of its fangs. The crown is encased in thick shining enamel, and is 9 lines in length by 8 lines in breadth; the height of the crown is 2·6 lines. The fangs are two in number; the anterior small, the posterior large and diverging. The length of the latter is 7·5 lines.
The accompanying sketch represents the crown (nat. size), which probably shows a more advanced state of wear than any figured by Cuvier.
The ear-bone is entire, and measures 1·4 inch in breadth, by 9 lines in vertical diameter.
The specimens referred to in this note are in the Musuem of the Geological Society.
Note on supposed Burrows of Worms in the Laurentian Rocks of Canada
Authors: Dawson J. W. 
Published: October 2009

Among other indications of fossils in the Laurentian rocks, mentioned in my paper on the structure of
Eozoon
, are certain perforations resembling burrows of worms, found in a calcareous quartzite or impure limestone from Madoc, in Upper Canada. They occur in specimens in the Museum of the Geological Survey, and also in specimens subsequently collected by myself at the same place.

The beds at Madoc, containing these impressions, underlie, unconformably, the Lower Silurian limestones, and are regarded by Sir W. E. Logan as belonging to a somewhat higher horizon in the Laurentian than the Eozoon Serpentines of Grenville. They are also less highly metamorphosed than the Laurentian rocks generally. They are described in Sir W. E. Logan's Report on the Geology of Canada, 1863, at p. 32.
The impressions referred to consist of perforations approaching to a cylindrical form, and filled with rounded siliceous sand, more or less stained with carbonaceous and ferruginous matter, more especially near the circumference of the cylinders. These superficial portions being harder than the containing rock, and of darker colour, and also harder than the interior of the cylinders, project as black rings from the weathered surfaces; but in their continuation into the interior of the mass, they appear only as spots or lines of a slightly darker colour, or stained with iron-rust.
When sliced transversely and examined under the microscope, they appear as round, oval, or semicirenlar holes drilled through the rock, and lined around their circumference with dense and dark-coloured siliceous matter, while
On the Graptolites of the Skiddaw Series
Authors: Nicholson Henry Alleyne 
Published: October 2009

Abstract

T
he
author first describes the geological relations and distribution of the Skiddaw Slates, and notices their correspondence with the Quebec Group of Canada, and then gives a description of the Graptolites found in these rocks. The genera and their distinguishing characters are the following:—

1.

Dichograpsus
, Salter (3 species): possesses a frond, repeatedly dichotomous from a basal stipe into eight, sixteen, or more branches, each with a single row of cells, the lower part of the stipe being enveloped in a corneous cup.

2.

Tetragrapsus
, Salter (3 species): possesses a frond composed of four simple stipes, arising from a non-celluliferous funicle, which bifurcates at both ends.

3.

Phyllograpsus
, Hall (2 species): differs from the last in possessing a frond composed of four simple stipes united back to back by their solid axes.

4.

Didymograpsus
, M'Coy (7 species): the frond consists of two simple stipes springing from a mucronate radicle, which may be rudimentary or apparently absent.

5.

Diplograpsus
, M'Coy (4 species): two simple stipes, united by their solid axes into a celluliferous frond furnished with a radicle at the base.

6.

Graptolites
vel
Graptolithus
, Linn. (4 species): consists of a simple stipe, with a single row of cells on one side, and a small, generally curved, radicle at the base.

7.

Pleurograpsus
, Nicholson (1 species): celluliferous branches derived from a main celluliferous rhachis.
Notes on the Lower-Lias Beds of Bristol
Authors: Stoddart W. W. 
Published: October 2009

T
he
occurrence of beds in the Bristol district corresponding to the Sutton beds of Glamorganshire has been thought worth noting.

In this locality the sequence of the different groups of strata is so perfect that the position of any one of them becomes almost a matter of certainty.
In many places the beds are apparently so bare of organic remains, that the collector is at once discouraged. The very horizontality of the beds themselves is frequently an obstacle, from the great distance to be walked over before a change of zone takes place.
The line of section in the following sketch (fig. 1) runs from a quarry (No. 1) north of the Orphan House on Ashley Down, across Montpelier, to Gotham Hill.
As shown in the figure, three quarries, now fortunately opened, explain the whole series of beds contained in the section.

It will be seen that the series extends from the base of the zone of
Ammonites Turneri
down to the Rhætic beds.

All of them dip 8°, to the north-east. This small angle makes the beds appear nearly horizontal, and at first sight makes their order very puzzling.
It is rather singular that the strata here should dip north-east while those on the opposite side of the Severn dip to the southeast. It shows an anticlinal to exist somewhere to the south of that river. The rising of the land must of course be very gradual, but quite sufficient to form a shallow trough from the neighbourhood of
On the Speeton Clay
Authors: Judd John W. 
Published: October 2009

I. I
ntroduction
.

I
n
the attempt to study the Neocomian formation as developed in this country, my attention has been directed for some years past to the series of beds in Yorkshire which since 1829 has been known as “the Speeton Clay.” I have found that, although a very great variety of opinions had been expressed concerning the age of this formation, but little had been done towards working out in detail the true succession of the beds which compose it; and, as this part of the Yorkshire coast-section is greatly complicated by faults and contortions, and much obscured by landslips and drift, I soon became convinced that it was only by such detailed and systematic examination that satisfactory conclusions were to be arrived at. The fact that the mining operations now pursued on an extensive scale at these cliffs are rendering this
unique
section every year more and more obscure acted as a further incentive; and I accordingly determined on the execution of the following tasks:—

1.
A careful survey of the Speeton Cliffs, and the construction of a map and section upon a very large scale, showing the various landslips &c., with a view to arriving at the true succession of the beds. The necessary basis for this work was opportunely furnished by the publication in 1862 of the beautiful 6-inch Ordnance Map of this part of the Yorkshire coast.

2.
The collection of the fossils and drawing up accurate lists of the contents of the several beds.
On the Physical Geography of Argyllshire in connexion with its Geological Structure
Authors: Duke  
Published: October 2009

I
n
a work published in 1865 upon “The Scenery of Scotland viewed in connexion with its Physical Geology,” Mr. Geikie has set forth with much ability certain theories upon that subject which seem to be gaining ground with the younger school of geologists.

Not believing in the truth of those theories, I have selected the work referred to as the best text I could find for the purpose of bringing them under discussion. Although a popular treatise, the work of Mr. Geikie is at once elaborate and systematic. It states the questions in dispute with great distinctness. I propose therefore in this paper to deal with the theory of the “Erosionists” as I find it there defined and there defended.
According to these theories subterranean movements and commotions have had comparatively very little to do with the origin of the hills and valleys of the Highlands. Their form is mainly due to atmospheric powers of waste acting slowly and gradually through uncounted “millions of years.” The mountains have been carved out of the original thickness of the strata of which they are composed. The valleys are nothing but the hollows out of which vast masses of material have been removed; and, further, this removal has not been effected by convulsions of any kind, but merely by the streams which now occupy the bottom of the glens, and, during the Glacial period, by continuous masses of ice which passed downwards from a few central ridges to the sea. This theory is
Observations on the Parallel Roads of Glen Roy
Authors: Babbage Charles 
Published: October 2009

Many years have passed since I visited the remarkable scenery of the parallel roads of Glen Roy. Several explanations of their origin have been given; and my own view of the subject was, I apprehended, in accordance with the views of geologists. The recent paper of Sir John Lubbock upon that subject shows that the causes which have hitherto been assigned for their origin have not yet received general assent. Under these circumstances, I think it desirable to record the very simple explanation of their origin which had satisfied my own mind.
In the largest of a system of valleys many hundred feet deep and whose sides are very steep, there occur three lines of terraces at different heights, each apparently preserving its horizontality over an extent of above twenty miles.
The sight of these extensive parallel lines immediately suggests the idea either,
1st, that they had arisen from the beaches of ancient lakes which had formerly filled the intervening valleys, and that the levels of those lakes had at distant intervals been reduced by the bursting of successive barriers by which their waters had been confined; or
2ndly, that they had formed the beaches of a system of fiords, or narrow inlets of the sea, which had been elevated at various times by internal heat.
The first of these suppositions is, I believe, most generally adopted; and it appears to me to be the most probable.
These parallel roads themselves slope gently inwards towards the central valley. They are