bluuebunny/crossref_metadata_2025_split huggingface dataset:
On the Silurian Grits of Corwen, North Wales
Authors: Hughes T. McKenny 
Published: October 2009

I
beg
to offer a few notes, made chiefly in the summer of 1876, while endeavouring to correlate the base of the Silurian rocks of North Wales with the corresponding beds in the Lake-district and South Wales.

I found that some important changes in the mapping and consequent classification of the rocks in the neighbourhood of Corwen were necessary. These corrections being made, I obtained a key by which I was able to detect, over the whole of the district I then examined, a very variable but yet a more satisfactory and easily recognized base for the Silurian rocks.
It will be seen by reference to the Geological-Survey map of the Corwen district, that the Denbigh Grits are represented as thrown down by a fault (running W.S.W. and E.N.E.), while no Grits are are shown on the map between this and Pennyglog Quarry.

I found, however, that the Grits at Corwen were not the Denbigh Grits, as seen
e. g.
on top of the Flags at Penyglog Quarry E.S.E. of Corwen, but that the Corwen Section is as follows (fig. 1):—
On the Chemical and Mineralogical Changes which have taken place in certain Eruptive Rocks of North Wales
Authors: Phillips J. Arthur 
Published: October 2009

At Penmaenmawr, in the county of Caernarvon, six miles southwest of Conway, a crystalline felspathic rock has been erupted through Silurian strata, and rises to a height of 1553 feet above the sea-level, forming a boss-like elevation two miles in length and one in width.
This stone, which is of a greenish-grey colour, is moderately fine-grained, and to the unassisted eye, appears to consist of felspar associated with minute crystals of some dark hornblendic or pyroxenic mineral. The general mass is divided into beds by a series of predominating joints dipping north at an angle of about 45°; and these are again divided by a system of double jointings which are sometimes so developed as to the cause the rock to become distinctly columnar.
On the northern flank of the mountain, where four large quarries have been opened upon it, this stone is extensively worked both for general building-purposes and for road-making. Of these quarries the two more easterly ones belong to Messrs. Kneeshaw, Lupton, and Co., while those situated further towards the west are worked by Messrs. Brundrit and Co. The crystalline rock at the eastern extremity of the outcrop, near its point of contact with the slates, sometimes encloses small schistose fragments, but is fine-grained and frequently assumes a columnar structure.
Here the stone is often so close in texture as to almost resemble chert, and to break with a conchoidal fracture; but particles of kaolinized felspar show that it has, even here, been subjected to a certain
On the Beds between the Gault and Upper Chalk near Folkestone
Authors: Price F. G. Hilton 
Published: October 2009

We have no better section of the Upper Cretaceous rocks than at Lydden Spout, which is a name given to a portion of the cliff between Folkestone and Dover.
The chalk cliffs at this locality were carefully measured by Mr. C. E. De Rance, F.G.S. (of H.M. Geological Survey), and myself; and the height was found to be 433 feet above the mean sea-level. The thickness of the beds between the Upper Gault and the first bed of flints (Upper Chalk) is 348 feet.

These beds I propose to divide into three general groups,
i. e.
Chalk Marl, Grey Chalk, and Lower Chalk, the former two corresponding with the
Cénomanien
of D'Orbigny, and the latter with his
Turonien
. As these divisions contain several well-marked lithological bands or beds, I have again subdivided them into six zones and nine beds, distinguishable by their palæontological contents or lithological characteristics.

Mr. Whitaker, in vol. iv. p. 33 of the Geological-Survey Memoirs, quoting Phillips, estimates the Grey Chalk or Chalk Marl at about 200 feet, and describes it as varying in colour and texture, but softer, more sandy, and less compact than the other divisions. He makes his division extend to the top of the thin yellowish bed, the zone of
Belemnites plenus
.

It will be seen from the present paper that I have given the same limits for the Grey Chalk and Chalk Marl together as Mr. Whitaker, and that I have estimated the thickness of those beds at 197 feet; but instead
Observations on Remains of the Mammoth and other Mammals from Northern Spain
Authors: Adams A. Leith 
Published: October 2009

My friend Mr. O'Reilly, Professor of Mineralogy to the Royal College of Science, Dublin, has kindly permitted me to examine a collection of fossil remains made by himself and Professor Sullivan, of Queen's College, Cork, when engaged in surveying the mineralogy and geology of the province of Santander.
The conditions under which the remains were found are fully detailed in the able reports of these gentlemen, published in the 4th volume of the ‘Atlantis,’ and reprinted in a separate volume entitled ‘Notes on the Geology and Mineralogy of the Spanish Provinces of Santander and Madrid.’
It appears that, during the sinking of a shaft in search of calamine in limestone underlying the dolomite of the valley of Udias, the workmen,at about 12 metres from the surface, suddenly broke into a cavern of considerable dimensions. At the north end of the cavity was a mound of soil which had fallen down a funnel blocked up at the time of the discovery by surface-soil and débris. Close to this mound were found many bones of mammals and birds. The remains were either partially or entirely buried in calamine, which covered the floor and formed an enormous bed of variable thickness. It appears, therefore, not only from the large funnel, which was evidently the original opening, but also from the remains, that the cavern was an enlarged joint or rock-fissure, into which the entire carcasses or else the live animals had been precipitated from time to time.
The following, I am informed, does
On the Agassizian Genera
Amblypterus, Palæoniscus, Gyrolepis
, and
Pygopterus
Authors: Traquair Ramsay H. 
Published: October 2009

W
hat
is an
Amblypterus
? What is a
Palæoniscus
? How do we distinguish them? What special reasons have we for referring any of our smaller Carboniferous fishes to the one or the other genus? These are questions to which, I fear, few collectors of Carboniferous fossils could offer very definite answers, and for the very good reason that the definitions of these two genera, which are found in the works usually consulted by palæontologists, are, it must be owned, of a somewhat unsatisfactory nature.

Gyrolepis
and
Pygopterus
also are terms frequently met with in lists of fossils from British Carboniferous localities. But by what characters do we distinguish
Gyrolepis
as a genus? Or what are the special marks which justify us in assuming any of our larger Carboniferous Palæoniscidæ to be generically identical with the
Pygopteri
of the Magnesian Limestone and Kupferschiefer? Here, again, we shall find our subject enveloped in an obscurity which can only be dispelled by fresh and careful original observation in a field which, since the days of the illustrious Agassiz, has been comparatively little trodden.

The present communication embodies the results of my own recent investigations into these subjects, though there is room and need for much additional inquiry, as is self-evident from the nature of the remains with which we have to deal.
Amblypterus and Palæoniscus

The definition of
Amblypterus
given by Agassiz in his “Tableau synoptique” is as follows:—

“Toutes les nageoires très-larges et composées de nombreux rayons, P. très-grandes; A. large; D. opposée
The Bone-caves of Creswell Crags.—3rd Paper
Authors: Mello J. Magens 
Published: October 2009

I
t
will be remembered that on two previous occasions the history of the Creswell-Caves Exploration has been brought before the Society, on the latter of which the results of the work were given up to the close of 1875.

During the early part of last summer the exploration has been carried on under the auspices of a Committee, consisting of Sir J. Lubbock, M.P., F.R.S., as President, Prof. W. Boyd Dawkins, F.R.S. (Secretary), F. Longdon (Treasurer), Prof. G. Busk, F.R.S., W. Bragge, F.G.S., R. D. Darbishire, B.A., F.G.S., J. Evans, F.R.S., A. W. Franks, F.R.S., Rooke Pennington, LL.B., F.G.S., Prof. Prestwich, F.R.S., and the Rev. J. M. Mello, M.A., F.G.S. (Director and Reporter), Prof. W. Boyd Dawkins and T. Heath, F.R.H.S., being Superintendents.
It will hardly be necessary to do more by way of recapitulation than just allude to the first papers read, which have established the fact that we have at Creswell a series of highly important caves, illustrating by their contents two periods of human occupation during the Palæolithic age in Britain, when man was contemporary in Derbyshire and the adjoining district with the characteristic Pleistocene fauna. The remains of animals belonging to this fauna, in great abundance and representing a remarkably large number of species, have been found in these caves, in conjunction with quartzite and flint implements of two different types:—the one ruder than the other and underlying it, corresponding in character to the rude implements of the Lower Breccia of Kent's Hole and of the
The Exploration of the Ossiferous Deposit at Windy Knoll, Castleton, Derbyshire
Authors: Pennington Rooke , Dawkins W. Boyd 
Published: October 2009

Introduction
.—In the spring of 1876, by the courtesy of the owner of the land, Mrs. Champion, we were able to carry on the exploration of the ossiferous deposit at Windy Knoll, near Castleton, begun in 1874 by Mr. Rooke Pennington, and described in the ‘Quarterly Journal’ (May 1875, p. 241), with the following results.

If reference be made to the above paper (p. 242) it will be seen that the fissure in which the remains were first met with was traced to a sort of basin filled with clay and packed full of bones of animals and large and small blocks of stone. We resolved to have this thoroughly examined by a body of experienced miners, working under the constant supervision of Mr. John Tym, of Castleton, while we were, as far as possible, present during the six weeks spent in the work.

Exploration
.—We began operations on the east side of the mound of clay, and rapidly exposed the following section (fig. 1) in descending order:—

C.
Clayey débris forming the summit, without bones, and probably rubbish piled up when the quarry close by was worked at that level 6 feet.

B.
Yellow clay with large blocks of limestone, fragments of Yoredale shale washed down from the adjoining heights of Mam Tor, bits of elastic bitumen or elaterite, and of fluor spar derived from the deposits of those minerals close by, together with bones of bison, reindeer, wolf, fox, and grisly bear 8

A.
Below this
On the Serpentine and associated Rocks of the Lizard District
Authors: Bonney T. G. 
Published: October 2009

T
he
following papers occur in the ‘Transactions of the Royal Geological Society of Cornwall:’—

“Sketch of the Geology of the Lizard District,” by A. Majendie, i. p. 32.
“Hints on the Geology of Cornwall,” by Sir H. Davy, i. p. 38.
“On the Serpentine District of Cornwall,” by the Rev. J. Rogers, ii. p. 416.
“Contributions towards a Knowledge of the Geology of Cornwall,” by H. S. Boase, iv. p. 160.
The subject is also treated in the following works:—
“On the Physical Structure of the Lizard District,” by Professor Sedgwick (Trans. Cambridge Phil. Soc. i. p. 291).
“Report on the Geology of Cornwall and Devon,” by H. T. De la Beehe (published 1839).
“On the Serpentinite of the Lizard,” by Profs. W. King and T.H. Rowney (Phil. Mag. ser. 5, vol. i. p. 280).
In the last of these papers the authors maintain the metamorphic character of the serpentine, but consider it probably an altered pyroxenic rock, like that of Bufaure in the Fassa-Thal. The paper appears to have been mainly written with the view of calling attention to imitative organic, especially Foraminiferal structures. So far as my experience goes, any thing of this kind is very rare.
The great work of Sir H. De la Beche, and the shorter paper of Professor Sedgwick, are models of careful observation; and several things mentioned hereafter have been already noticed by them. The former author strongly inclines to the belief that the serpentine is of igneous origin, though he admits some
On Sand-worn Stones from New Zealand
Authors: Enys J. D. 
Published: October 2009

B
efore
describing the Eolian or wind-worn stones, specimens of which are exhibited, I will give a short description of the locality from which they come. On the western side of the entrance to the Harbour of Wellington (situated on Cook's Straits, at the southern end of the North Island of New Zealand) is a peninsula attached to the mainland by an isthmus which has only a slight rise above the sea. This peninsula runs parallel to the mainland for two or three miles; and the connecting isthmus is about a mile across, dividing this space unevenly into two bays, which are known as Evans Bay and Lyells Bay.

On each side of the isthmus is a line of low sand hills; and between them is situated a flat piece of sand which is mixed with sufficient clay to form a hard bottom. On this rest the stones which are the subject of this paper.
From the ground on both sides of these bays being of considerable height and lying north-west and south-east, the prevailing winds, which blow from the same directions with great force, drive a cloud of siliceous sand from one set of sand dunes to the other. This sand, on a windy day, forms a dense mass reaching to about the knees of any one walking over the ground. The result of this is the gradual wearing away of the stones on this flat ground. Originally of the ordinary shape of broken stone, they begin by showing sloping
Note on a Rock-specimen from the Centre of the so-called Porphyritic Mass to the East of Tal-y-sarn
Authors: Davies T. 
Published: October 2009

A microscopical examination of this rock discloses a very fine-grained ground-mass containing evenly distributed quartz grains, and a felspar in very small, dull, opaque, crystalline grains.
In thin sections, under the microscope, the quartz is found to he more abundant than at first was evident; indeed it forms a very considerable part of the mass. It is very angular in outline, and appears to be fragmentary, the rounded crystalline grains with inclusions of the ground-mass, so characteristic of the quartz-felsites and porphyries, being but sparsely represented. The felsitic groundmass is very uneven in texture, has very little action on polarized light, and is only occasionally to be observed folding in bands around a crystal of felspar or quartz. In some parts the quartz grains are so numerous and closely aggregated as to afford but little space for the ground-mass, and bear a close resemblance to some of the more quartzose members of the so called “ashes” of North Wales. The felspar, like the quartz, is very fragmentary and much kaolinized. Some altered magnetite is present.
The rock is evidently a breccia in which both the fragments and the cement are of the same mineral nature; it is, in fact, a quartz-felsite breccia.
On the Glacial Deposits of West Cheshire, together with Lists of the Fauna found in the Drift of Cheshire and adjoining Counties
Authors: Shone W. 
Published: October 2009

I
n
March 1874, I communicated through Mr. D. Mackintosh, F.G.S., a paper on the “Discovery of Foraminifera, &c., in the Boulder-clays of Cheshire” (Quart. Journ. Geol. Soc. vol. xxx. p. 181). Since that time I have continued my observations, which I now place before the Society.

The extension recently of the Midland Company's line from Mouldsworth to Chester has caused interesting sections of the Drift to be exposed. The accompanying section to this paper exhibits that portion of the line which commences where the road from Hoole to Trafford crosses it, and is continued from that point for two miles and a quarter to a point a little beyond where the road from Trafford to Guilden-Sutton passes under the railway. From the commencement of the cutting at the Newton-road bridge to a spot near the top of Newton Hollows, a distance of half a mile, the Upper Boulder-clay through which it passes contains very few (if any) striated stones, and no shell-fragments, though small rounded gravel is present throughout it.
The cutting varies from 5 to 10 feet in depth up this point, consequently only the upper part of the clay is exposed; its entire thickness at the commencement of the section I estimate at 30 feet.The sand may at intervals be observed to crop out from beneath the clay in a dell which runs parallel to the railway-cutting, called Newton Hollows, proving its (the sand's) continuance beneath the clay throughout this part of the section. I am indebted to
The Chronological Value of the Pleistocene Deposits of Devon
Authors: Ussher W. A. E. 
Published: October 2009

Part I. D
eposits.

A: (a) The high tableland of the Cretaceous area of the Blackdown Hills and the summit of its outlying landmark, Haldon Hill, are capped by an accumulation of brown, yellowish, or grey clay full of broken unworn fragments of flint and chert. The clay rests alike on Chalk and Greensand in pipes*. Its character in Chalk districts is almost identical with that of the clay with flints in Kent; but near the westernmost extension of the Chalk (to the east of Sidmouth) the contained flints are seldom whole. In many places the matrix is thickly crowded with small flint chips and powder, giving it a grey colour and gritty texture, as on Haldon and Peak Hill, near Sidmouth. The clay with flints is confined to tableland areas : where the contour has been subsequently modified, it is only found on such heights as exhibit the original surface of the old plain from which they were isolated. The clay with flint and chert varies in thickness up to nearly 50 feet.
That it has suffered from denuding agencies is testified by the presence of
(β) Waterworn fragments of flint on its surface, bearing somewhat the same relation to the c]ay with flint and chert that is presented by the brick-earth to its representative in the south-eastern counties. This waterworn material is of very local occurrence on the Cretaceous tableland; upon Haldon it has been described by Mr. Godwin-Austen † and others.
(γ) A patch of flint– and quartz-gravel
On the Fish-remains found in the Cannel Coal in the Middle Coal-measures of the West Riding of Yorkshire, with the Descriptions of some new Species
Authors: Davis James W. 
Published: October 2009

In paper I had the honour to read before this Society in 1876*, a section of the strata composing the West Riding of Yorkshire Coal-field from the Elland Flag rock to the Blocking Coal is given. The Blocking Coal is probably the equivalent of the Silkstone Coal of the more southern part of the Coal-field, and is regarded by the members of the Geological Survey as the most convenient stratum to form the dividing line between the Lower and Middle Coal-measures. The coal-seams yielding the fossil fish-remains which form the subject of the present paper occur about 400 feet higher in the series than the Blocking Coal. The following section may serve to give an idea of the position of the Stone- or Gas-coal of Adwalton and the surrounding district :—
The whole series exhibits considerable variations in the character and relative thickness of the strata. The coals, though perhaps more persistent than the other members of the series, do not form an exception. Sections exposed in pits and borings in different localities prove the coals to thin off in certain directions and almost disappear; in some the coal is divided into two bands by lenticular masses of shale or sandstone many feet in thickness; in others two beds of coal gradually converge and form one thicker bed. In this respect the Middle Coal-measures differ from the Lower Coal-measures. The latter, especially in the Lower or Halifax series, are remarkably persistent. The Halifax hard and soft coals extend over the
On the Probable Temperature of the Primordial Ocean of our Globe
Authors: Mallet Robert 
Published: October 2009

So far as my reading has extended, I am not aware that any author on physical geology or terrestrial physics has expressed any definite views as to the temperature of the primordial ocean—that is, of the large body of water which, as now collected together, fills the existing basin of the seas and great oceans, the configuration of which, like that of the surrounding continents, has, perhaps, not very largely changed during what is called geological time. Some very vague and indefinite notions may, indeed, be found in the writings of the early and long-since obsolete cosmogonic authors to the effect that the primordial ocean was probably at some indefinite period, and to some indefinite extent, warmer than the sea as existing within the period of human history; but no attempt to assign its temperature at any epoch anterior to our own has, to my knowledge, yet been made. Nevertheless it seems to me that, on grounds of very high probability deducible from admittedly physical laws, we can approach this problem with a facility and certainty of result greater than those which can be obtained in reference to many physical questions smaller in extent and apparently nearer our reach.
According to the calculations of Mr. Gardner, the extent of land is about 37,673,000 square British miles, leaving out, of consideration the Victoria continent, and that of the sea 110,849,000 square miles. That this cannot be regarded as furnishing the true proportion of land and water is evident, as there is
On Mammalian Remains and Tree-trunks in Quaternary Sands at Reading
Authors: Poulton Edward B. 
Published: October 2009

The pit furnishing some interesting sections to be described in the following paper is situated on the Redlands estate, at Reading, a little east of the new Grammar School, and about a mile south-east of the market-place. The pit is about halfway up the south slope of the conjoined Thames and Kennet valleys, and is 36 feet above the river-level. It has been worked for gravel and sand for some years, and recently for clay; and the gravel-bed, from 10 to 15 feet in thickness, has been cleared out over an area 276 feet in length from north to south, and of about the same average length from east to west, where, however, the boundaries are irregular and, to the east, partly effaced. The beds exposed in the north face are far more perfect and instructive than elsewhere. This face, about 20–25 feet in average height, and, where completely exposed, 65 feet in length, is drawn to a scale of one-fifteenth in. to the foot in fig. 1.

A. About 12 feet thick, represents the gravels and reoent strata overlying certain reconstructed beds of sand and clay.

(1)
1 foot 6 inches thick, is the superficial alluvium containing elements derived from the waste of the gravel below.

(2)
2 feet 6 inches thick, is transitional between the alluvium and the underlying gravel. It consists of rounded and subangular flints scattered thinly through a base of yellow clayey soil.

(3)
8