bluuebunny/crossref_metadata_2025_split huggingface dataset:
The Cretaceous Strata of County Antrim
Authors: Hume W. Fraser 
Published: October 2009

I. I
ntroductory
and D
escriptive
.

Although, during the last twenty years, the Upper Cretaceous strata of England and the Continent have been the objects of detailed investigation, the deposits of the same age, which form so conspicuous a feature in the North-east of Ireland, have been practically neglected. Two observers only, Prof. R. Tate and Dr. C. Barrois, have seriously attempted to classify these formations on definite palæontological principles, but the results at which they respectively arrived differ in several material particulars. The present paper is the outcome of two excursions carried out in the summers of 1895 and 1896: the first connected with, and following on, the Geologists' Association's visit to County Antrim, under the guidance of Mr. A. McHenry; the second aiming at a more detailed examination of the stratigraphy of the same district. The first and second parts will be devoted to the consideration of the various sections visited, together with an account of the results obtained by applying the methods of analysis and microscopical examination previously employed by me in considering the Upper Cretaceous zones of the South of England. In the third and fourth parts it is proposed to examine the theoretical questions arising out of these researches, dealing with the zonal classification of the Irish Cretaceous strata, the probable distribution of the land-masses, and the sequence of physical changes during the period under consideration.
My thanks are due to the following members of the Belfast Naturalists' Field Club, who have freely placed their local knowledge
Deposits of the Bajocian Age in the Northern Cotteswolds: The Cleeve Hill Plateau
Authors: Buckman S. S. 
Published: October 2009

I. I
ntroduction
.

The present essay is in continuation of a former paper which described deposits of similar date in the Mid-Cotteswolds. The district now under discussion consists of an outlying isolated plateau, cut off from the main mass of the Cotteswolds on the east by the deep valley at Sevenhampton, and separated from the Mid-Cotteswolds by the Vale of Whittington. The best-known portion of this plateau is called Cleeve Cloud or Cleeve Hill; other portions include the hills above Whittington and Hewlett's Hill. For the purpose of the present paper the whole will be named the Cleeve Hill plateau.
The literature relating to the district is not extensive. The latest detailed section is that of Cleeve Hill given by Wright. As, however, the sequence of the strata set forth by that author differs so considerably from that which will be described in the present communication, it is not thought desirable to discuss his section in detail, or to combat his views. An almost entirely new reading will be presented now.
One more point may be referred to. A postscript to my communication on the ‘Mid-Cotteswolds’ (p. 461) first gave a short summary of the sequence found at Cleeve Hill. Further researches fully tended to bear out this sequence; and then, within the last few months, an important portion of the Rolling Bank quarry has been opened up, showing, in one exposure, confirmation of what was before an inductive surmise from the piecing together of several.

II. T
he
S
ections
of the
On the Pyromerides of Boulay Bay (Jersey)
Authors: Parkinson John 
Published: October 2009

The acid lavas forming the more easterly part of the northern coast of Jersey have been the subject of investigation by many geologists. M. de Lapparent, in a note on the eruptive rocks of the Isle of Jersey published in 1884, summarized these accounts, and his paper was extensively quoted by M. Noury in his ‘Geólogie de Jersey,’ published a few years later, the quotations including those paragraphs which relate to the work of previous authors. The earliest is that of Macculloch, in 1817, in which a hornstoneporphyry is noticed from this neighbourhood. A geological map of the island was published by A. Transon in 1851, in which the northern half of Boulay Bay is represented as being occupied by porphyries, the southern by grit, while the line of demarcation between the latter rock and the more easterly conglomerate is correctly indicated. In 1879 the ‘spherular character’ of the rhyolites of Boulay Bay was briefly noticed by Mr. Thomas Davies, principally from specimens supplied to him by Dr. Dunlop, of Jersey.
M. Noury, in his work, supplements his quotations from M. de Lapparent with additional observations of his own on the characteristics and origin of the structures exhibited by the rhyolite, at the same time giving a map wherein the principal locality at which pyromerides occur is indicated. Since the publication of Noury's book, a few notes on Jersey have been intercalated in some general observations on the Channel islands by M. A. Bigot; and the Rev. Edwin Hill has
Exploration of Ty Newydd Caves, Tremeirchion, North Wales
Authors: Pollen G. C. H. 
Published: October 2009

I. I
introduction
.

In November 1896 a committee was formed, consisting of Dr. H. Hicks, F.R.S., our President, Dr. H. Woodward, F.R.S., with myself as secretary, to excavate some caves at Tremeirchion, very near the caves of Ffynnon Beuno and Cae Gwyn. These last were excavated by Dr. Hicks and Mr. E. B. Luxmore, and during part of the time by a committee appointed by the British Association in the years 1883 to 1888, and it was hoped that the contents of the new caves might throw some additional light on the discoveries made there.
Our work is still far from complete, but Dr. Hicks, to whose authority I shall frequently appeal throughout this report, considers that the results already obtained are of sufficient interest to be brought before the Society.
In addition to organizing the committee of excavation, Dr. Hicks obtained two grants, from the Reserve Fund of the Royal Society and from the Government Grant Fund, to cover expenses. I am moreover indebted to him for much valuable advice and assistance, in examining the materials found, and even in visiting the cave in person.
I must also express my gratitude to Mr. A. Foulkes-Roberts, of Denbigh, for his very kind help in the prolonged negotiations that I have had with the tenants of Ty Newydd Cottage, after which I have named the cave. I must add that, since we first came to an understanding, the owner, Mrs. M. E. Griffiths, of Mold, has shown every disposition to assist me.
Cone-in-Cone: Additional Facts from Various Countries
Authors: Gresley W. S. 
Published: October 2009

abstract
Examples of flinty stone in the ‘fire-clay series’ of the Ashby coal-field exhibit ‘areas of conic structure lying unconformably.’ In the same stratum of shale are large masses of the same flinty rock, more or less coated with conic structures, which appear to have been formed out of layers of shale and ironstone. The bending-up of the shale above the nodules and down below them, the close but unconformable covering of Permian breccia, and the staining of the whole section suggests, if indeed it does not demonstrate, to the Author that the growth of the cone-in-cone took place subsequently to the deposit of the Permian breccia. Several American and other examples are described, and a series of conclusions are appended to the paper.
A Phosphatized Trachyte from Clipperton Atoll (Northern Pacific)
Authors: Teall J. J. H. 
Published: October 2009

The following remarks are based on five rock-specimens from Clipperton Atoll, referred to by Admiral Wharton in his description of that island.
One is a dark brown rock composed of porphyritic crystals of glassy felspar and a compact groundmass; the others are white or cream-coloured, and in some of these the same porphyritic felspars as in the first-mentioned rock may be observed. The examination of a series of microscopic sections shows that the rocks are all more or less altered trachytes.
The brown rock is the least altered. It consists of phenocrysts of sanidine (Pl. XXIII, fig. 1) set in a groundmass of microlitic felspars and brown interstitial matter. No ferro-magnesian minerals are recognizable. The conspicuous phenocrysts of sanidine are, as a rule, comparatively free from inclusions; but the rock contains also some patches of felspar, which are so crowded with inclusions of a brown substance that the felspar-material forms only a small portion of the compound mass.
An analysis of this rock yielded the following somewhat surprising result:—
The phosphoric acid is present in the brown substance, which evidently represents, in a more or less altered form, the interstitial matter of the original trachyte.
The microscopic sections of the white or eream-coloured rocks all show the structure of a trachyte. In some specimens the phenocrysts of sanidine have been more or less preserved, while the groundmass has been replaced by isotropic secondary material; in others the phenocrysts have disappeared, and their places have been wholly or partially filled up
On an Outlier of Cenomanian and Turonian [equivalent to Lower and Middle Chalk] near Honiton, with a Note on Holaster altus, Ag.
Authors: Jukes-Browne A. J. 
Published: October 2009

The existence of an outlying tract of Chalk in the parish of Widworthy, near Honiton, has been known for many years, but no description of it has ever been published, although it is the most westerly inland tract of Chalk in England: the only more westerly patches being those on the coast.
It was known to Dr. Fitton, who mentions the occurrence of a particular stone called grizzle by the quarrymen ‘in a large pit or quarry at the bottom of the Chalk, near Sutton and Widworthy,’ remarking also that ‘it contains green particles, and does not burn to lime.’
The outlier of Chalk is marked on De la Beche's geological map published by the Geological Survey in 1845. In 1874 the district was re-surveyed by Mr. Ussher for a new edition of the Survey map, but he found that the quarry referred to was disused and overgrown.
My object in visiting the locality last year was to ascertain whether the succession of beds was similar to that on the coast, in which case the Chalk would be Middle Chalk (Turonian), and the Lower Chalk would be represented by quartziferous limestone and calcareous sandstone; or whether it included anything like the more ordinary kind of Lower Chalk, such as occurs at Membury and Chard.
The Structure of the Davos Valley
Authors: Jennings A. Vaughan 
Published: October 2009

In several of the high Alpine passes and valleys there are certain structural features which show that important changes in the process of denudation have taken place, and that in many cases there has been an alteration or complete reversal of the drainage-system.
Among a considerable number of instances, that of the Upper Engadine or source of the Inn is perhaps the most familiar. Prof. Heim, Prof. Bonney, and others have called attention to this area as showing the way in which the gorges of the southern side of the Alps are cut back with far greater steepness than the river-valleys of the northern slopes. While Prof. Bonney regards the difference as due to the greater rainfall and more rapid current on the southern side, and the consequently greater erosive power of the torrents, Dr. Preller believes that it is not possible to account for the present condition of the district without presupposing a subsidence on the south. Whichever view may be held, however, there is no doubt as to the facts. It can hardly be disputed that the Inn once took its rise beyond Maloja, and that the glaciers on the south once contributed to its formation streams now diverted towards the Italian plain. The valley has in fact been decapitated, and its feeding-streams have been diverted into a new and opposite course.
The object of the present paper is to call attention to the conditions which exist in the adjacent area of Davos: conditions which are to some extent parallel, but, on the other hand, are distinctly more complicated and less easy of explanation.
On some Palæolithic Implements from the Plateau-Gravels, and their Evidence concerning ‘Eolithic’ Man
Authors: Cunnington William 
Published: October 2009

Since the publication of the late Sir Joseph Prestwich's series of papers (1889–1896) on the chipped flints found by Mr. Benjamin Harrison on the Chalk-plateau of Western Kent, these specimens have attracted wide attention. For it was conclusively shown in those papers that the chipped flints came from a gravel which was much earlier than the gravels containing Palæolithic implements in the valleys of the existing rivers of the district. A British Chalk-plateau, in a period of intense cold or of on-coming cold, would hardly afford a comfortable cradle to the human race; and though Kent was not claimed as man's birthplace, it was held that the chipped flints of that county were the earliest and most primitive known specimens of his handiwork.
The enormous antiquity of these chipped flints was deduced, in the first place, from the stratigraphical relations of the gravel where they occur, which was referred to the Pliocene. The gravels are part of Prestwich's ‘Southern Drift,’ and were formed before the erosion of the Darent gorge or of the transverse Ightham valley. The plateau-gravels are therefore older than the existing river-system; but at present there is no evidence whatever to show that they are of pre-Pleistocene age.
The main claim of the plateau-flints to notice rests on the assumption that the chipping is of so primitive a character that it cannot be the work of the skilled flint-flakers of the Palæolithic age. These chipped flints have accordingly been held to represent the first crude attempts by
The Garnet-Actinolite Schists on the Southern Side of the St. Gothard Pass
Authors: Bonney T. G. 
Published: October 2009

At intervals during the last 20 years I have studied the well-known garnet-actinolite schists which are exposed on the southern slope of the St. Gothard Pass from perhaps 500 to about 1600 feet above the mouth of the tunnel. They extend westward along the flank of the Val Bedretto to beyond All'acqua, with one slight interruption near this spot, and can be followed eastward to the vicinity of the Pizzo Columbe, that is, for a total distance of from 16 to 17 miles, the breadth of the outcrop, which is locally interrupted by elongated masses of more normal hornblendic schist, being at its maximum about 1¼ mile. They are intersected by the Val Tremola and the Val Canaria with its tributary glens, and are exposed on the right bank of the Val Piora. Here the lower part of the mass must be about 6700 feet above sea-level, that is to say, the outcrop rises at least 2500 feet in about 5 miles.
My later visits threw some light on the origin of these rocks; but I felt that more work in the field was necessary before I could come to any conclusion. Therefore I determined to return to the district and examine more particularly the outcrops near the Val Piora, of which hitherto I had seen little, having spent my time on another group of schists, which apparently overlie them. This intention was carried out in July 1897, and I had the good fortune to be accompanied by my friend
The Carboniferous Limestone of the Country around Llandudno (North Wales)
Authors: Morton G. H. 
Published: October 2009

I. G
reat
O
rme's
H
ead
.

In Carboniferous Limestone, and the subdivisions into which it is divided in North Wales, were described in papers read before the British Association and the Liverpool Geological Society between the years 1870 and 1898. The most recent paper on ‘The Carboniferous Limestone of the Vale of Clwyd,’ is in the Proe. L'pool Geol. Soc. vol. viii, 1897-98. It contains a description of the subdivisions of the Limestone, including the Purple Sandstone, which consists of a series of sandstones and shales described by Mr. George Maw in 1865 as Permian, and more recently by Mr. Aubrey Strahan in 1890 as Coal Measures.
The following table shows the subdivisions that occur in the Vale of Clwyd, and in two other areas previously described. The Purple Sandstone is shown to be on the horizon of the highest subdivision of the Carboniferous Limestone in Flintshire and Denbighshire:—
The Great Orme's Head is a prominent headland on the seacoast of Caernarvonshire. It is separated from the mainland by an isthmus a mile in width and about 20 feet above Ordnance datum, and must have formed an island in post-Glacial times. Llandudno, the well-known watering-place, is situated on the southeast, and principally on the alluvial land. The Head is 2 miles in length from east to west, and 1 mile from north to south; it is bounded on the north and west by precipitous cliffs, which rise from the sea-level to an elevation of 200 or 300 feet. Along the southeastern side
On a Volcanic Series in the Malvern Hills, near the Herefordshire Beacon
Authors: Acland H. D. 
Published: October 2009

The rocks of the Malvern Hills have afforded scope for much study and discussion. Dr. Holl, Mr. Rutley, and Dr. Callaway have elaborated papers on them. Mr. Rutley's relates mainly to the general character of the rocks; while Dr. Callaway devotes himself to an enquiry into the genesis of the crystalline schists, and the production of secondary minerals in shear-zones.
I propose to deal with a small area of the hills and describe some of the rocks to be found there. The district lies east and south-east of the Herefordshire Beacon, which has three spurs. The northernmost is Tinker's Hill, south of that comes Broad Down, and south of that again Hangman's Hill. The latter is, in its turn, bounded on the south by the ‘Silurian Pass,’ so named in the Geological Survey memoir by the late Prof. Phillips. The Beacon Hill itself is of the same character as the main axis of the hills.

Prof. Phillips called attention to these rocks, and remarked that they ‘appear partly in lines like dykes.’ Dr. Holl also mentioned them, and considered them to be sandstone altered by the intrusion of trap-dykes. He noticed that some of the dykes contain a large proportion of augite. In a note to p. 100 (
op. cit.
) Dr. Holl says that fragments of these rocks are found in the Gullet Wood conglomerate. This statement requires investigation, as it might form a clue to the age of the series.

Dr. Callaway has expressed the opinion that these rocks
On some High-level Gravels in Berkshire and Oxfordshire
Authors: Shrubsole O. A. 
Published: October 2009

I. I
ntroduction.

A
fter
the appearance of Buckland's ‘Reliquie Diluvianæ’ the higher gravels of this district were for a time somewhat neglected. Much has now been done in the Geological Survey Memoir by Mr. Whitaker, and in papers by the late Sir J. Prestwich, Messrs. H. W. Monckton, H. J. O. White, A. :E. Salter, and other observers to throw light upon the interesting and difficult questions connected with the later physical history of this part of England. It has been found convenient in the present paper to refer to these gravels as a whole, but to treat more briefly those points which have been already discussed.

II. T
he
P
ebble-gravel
.

This term is used for the deposits, composed very largely of flintpebbles, which are found on the higher slopes of the Chiltern Hills, resting on Lower Tertiary outliers.

A familiar example of this gravel is that at Nettlebed, which has been fully described by Sir J. Prestwieh and Mr. White (
op. cit
.). It may be seen at various places on the plateau in the neighbourhood of Cadmore End and Lane End, near High Wycombe, by surface-indications; also at Coleshill, near Amersham, at which locality there is a very good section, showing about 5 feet of the gravel, but at a lower level (500 feet above Ordnance-datum).

The composition of the gravel will be seen from the following table, which states the percentage of the various stones in the samples examined :—
A pebble of chert, from the gravel at Nettlebed, was
Additional Notes on Rocks and Fossils from Franz Josef Land
Authors: Newton E. T. , Teall J. J. H. 
Published: October 2009

In our previous notes an account was given of the rocks and fossils which had been collected by Dr. Kœttlitz and sent home in 1896. Another large series was brought back by the same gentleman on the return of the Jackson-Harmsworth Expedition in 1897. These specimens have been examined, and it is satisfactory to have to report that they confirm our previous conclusions, necessitating no modification of our previous notes, except as regards some of the altitudes at which the specimens were obtained; these, however, do not alter the relative positions of the beds. At the same time, there are some additional facts which it is desirable to place on record.
The corrected measurements of altitudes are given by Dr. Kœttlitz on a preceding page (p.636), and these, it will be seen, alter materially the position of the beds at Cape Gertrude as given in our section. There are two errors on p.503 of our previous paper which we desire to correct. On line 4 the 100 feet of basalt refers only to what is seen in the cliff-section, and on line 9 ‘highest’ should have been printed ‘lowest,’ which will be found to agree with the section and the measurement that we then had.

I. R
ocks
.

A very large number of rock-specimens have been examined, but as these belong, for the most part, to varieties already described in our former paper, it will be unnecessary to refer to them at any length in these general notes.
The common type
The Geological Structure of the Southern Malverns, and of the Adjacent District to the West
Authors: Groom T. T. 
Published: October 2009

I. H
istorical Summary
.

E
asily
accessible, situated in a charmingly picturesque country, and marking some of the most interesting phases in the evolubion of the British Is]es, the Malvern Hills have now for nearly 80 years formed the subject of geological investigations, and have ever yielded new facts of interest and importance.

Leonard Horner described the Malverns as a granitic mass intruded into the associated strata. Murehison 2 regarded the chain as essentially of igneous origin, though including ‘Silurian’ beds altered by the intrusion. Phillips, in his masterly work on the district, maintained that the Lower Palmozoie strata associated with the range had been deposited against the crystalline rocks. Ho11, regarding the range as probably composed of pre-Cambrian metamorphosed sedimentary and igneous rocks, described the Cambrian aud Silurian beds as overlapping the metamorphic series.
Mr. Rutley considers that the gneissic and schistose rocks of the Malverns are a series of altered tufts, grits, sandstmnes, and volcanic and other igneous rocks. Dr. Callaway, on the other hand, regards the former series as metamorphosed plutonic rocks, chiefly granite and diorite, and compares them with the Archamn Series of Primrose Hill in Shropshire. The same author` recognized the volcanic series of the Herefordshire Beacon, and correlated it with the Urieonian rocks of Lilleshall Hill in Shropshire. The Herefordshire Beacon rocks have subsequently been studied by Green, and by Messrs. Rutley, Harker, and Acland.
During the past year the present writer has maintained that the Malvern and Abberley Hills are the basal wrecks of an