bluuebunny/crossref_metadata_2025_split huggingface dataset:
The Upper Towy Drainage-System
Authors: Jones Owen Thomas 
Published: October 2009

The most remarkable feature in the physical geography of Wales is undoubtedly the great plateau which extends almost without interruption from near the coast of Denbighshire in North Wales through Central and South Wales, where it occupies a large area of the counties of Cardigan, Carmarthen, Radnor, and probably also of Brecon. It truncates alike the highly folded Lower Palæozoic rocks of North and Central Wales and the gently inclined Old Red Sandstone marls of Breconshire. Its surface is apparently little influenced, either by the attitude of the rocks or by their lithological characters.
It abuts against the mountains of North Wales between Cader Idris and Snowdonia, which in places rise abruptly above its level, while southwards it extends to the foot of the great Upper Old Red Sandstone escarpment of Breconshire and Carmarthenshire, which overlooks it as a line of high cliffs overlooks a level foreshore.
Sir Andrew Ramsay attributed the formation of the plateau to marine denudation, and at one time regarded the escarpment of the Brecon Beacons as an ancient line of cliff.
Occasional references to the plateau occur in later publications. I have given reasons for distinguishing in Central Wales two distinct plateaux: namely, the Higher Plateau described above, and the Coastal Plateau which lies south of the Dovey Estuary and, extending inland from the coast of Cardigan Bay for a distance of 3 to 15 miles, is sharply marked off from the High Plateau on the east.
The Coastal Plateau was attributed to marine erosion
The Fossil Elephants of the Upper Thames Basin
Authors: Sandford Kenneth Stuart 
Published: October 2009

Succession of Deposits : Recent Developments.
In a paper published recently in the Journal of this Society (Q. J. G. S. vol. lxxx, 1924. p. 113) I described the river-gravels of the Thames and of its tributaries about Oxford, and, on a considerable body of evidence, suggested the following sequence of events:—
Glacial Plateau Drift; about 140 feet above the present river-level. [‘Glacial’, because, among other things, it contains glacially-striated erratic boulders and pebbles.]

Handborough Terrace; base about 90 to 100 feet above river-level, containing a well-marked ‘
Elephas antiquus fauna
’.

Wolvercote Terrace; about 40 feet above river-level, with derived Chellean implements, no fauna known; placed later than the above on stratigraphical evidence.

Wolvercote Channel; about 40 feet above river-level, a ‘ravinement’ of the Wolvercote Terrace, containing at the bottom unrolled Upper Acheulean and Micoque implements,
Elephas antiquus
and associated animals, capped by sands with mollusca indicative of temperate climate, and at a higher level peat, with plants, mosses, and coleoptera of temperate to sub-arctic character; above are clays containing rare implements, which are suggestive of Mousterian workmanship. At the top the Warp Sands are driven into the underlying deposits, as if by considerable force from above (suggestive of a cold and wet climate).

Summertown-Radley Terrace; about 20 feet above river-level, separated from the Wolvercote Terrace by a step; lower gravels abundant in remains of
E. primigenius
and accompanying fauna (less the Reindeer), overlain unconformably by gravels in which occur Hippopotamus, sometimes abundant,
Corbicula fluminalis
—occasionally very abundant, with valves united and
The Pleistocene Non-Marine Mollusca of the Avon Valley
Authors: Kennard Alfred Santer , Woodward Bernard Barham 
Published: October 2009

The most important paper on the Pleistocene deposits of the Avon Valley is by H. E. Strickland. This was sent to the Geological Society in June, 1835, and a brief abstract was published; but the paper was first printed in full in 1858.
As Jardine states, ‘most of the localities mentioned are now either filled up, worked out, or become otherwise inaccessible,’ and it is a matter of congratulation that so careful and competent an observer as Strickland was a resident in the district, while it is noteworthy that but little has been added to our knowledge since. It is, however, necessary to bring our knowledge up to date, and we thank Miss Tomlinson for submitting her specimens for examination; we also thank Mr. W. H. Edwards of the Victoria Institute, Worcester, for similar courtesy, and Mr. Hugh Watson for assistance with the Strickland Collection now preserved at Cambridge.
Fourteen species were obtained from this locality, namely :—

Pupilla muscorum
(Linné). 3 examples.

Limnæa pereger
(Müller). Common.

Limnæa truncatula
(Müller). 2 examples.

Planorbis læevis
Alder. 2 examples.

Ancylastrum fluviatile
(Müller). 2 examples

Valvata piscinalis
(Müller). 2 examples

Bithynia tentacutata
(Linnæ). 1 example

Unio littoralis
Cuvier. 1 valve.

Corbicula fluminalis
(Müller). 6 valves.

Sphærium corneum
(Linnæ). Common.

Pisidium amnicum
(Müller). Common.

Pisidium cinereum
Alder.
The Llandovery Rocks of Garth (Breconshire)
Authors: Andrew Gerald 
Published: October 2009

I. Introduction.
The area described in this paper is shown on Sheet 196 (uncoloured edition) of the 1-inch Ordnance Survey map, and on Sheet 56 S.W. of the (Old Series) 1-inch Geological Survey map, and also on the following 6-inch maps:—Brecònshire, viii N.W., N.E., S.W., S.E.; x N.E., S.E.; and xi N.W., S.W.
The district lies north-west of the Irfon, a tributary of the Wye, and mainly in the basin of the Chwefru, which flows southeastwards through the northern portion to join the Irfon near Builth.
Murchison dismisses most of the tract as containing ’hardly a single bed of solid stone’, and compares it with the Radnorshire area, where the ‘Upper Silurian’ lies, without the intervention of the Caradoc and Llandeilo groups, on the ‘Cambrian’. The rocks of Pen cefn-ty-mawr, Allt-y-elyêh, and Dol-y-fan are definitely referred to the ‘Cambrian’. His plate (facing p. 346) illustrates this arrangement, as do also the map and section. In ‘Siluria’ (5th ed. 1872) the strata west of the previous boundary-line of the ‘Lower Silurian-Cambrian’ were included as ‘Lower Silurian’.

The area was first surveyed by the officers of the Geological Survey, W. T. Aveline & Andrew Ramsay, and the map was published in 1850. The section (Sheet 5, Sect. 1), on the scale of 6 inches to the mile, shows the relationships of the Wenlock, ‘Tarannon’ (Pale) Shales, and Upper and Lower Llandovery. The occurrence of ‘sandstones and shales with fossils distinct from those of the Upper Llandovery,
Rhynchonella angustifrons, Atrypa marginalis, Pentamerus undatus
The Relations between the Llandovery Rocks of Llandovery and those of Garth
Authors: Andrew Gerald 
Published: October 2009

While we were engaged in examining the districts described in the two preceding communications, we frequently compared notes upon the succession and fauna. These comparisons appeared to show that during the Llandovery Epoch the geological events in one district were reproduced with some exactness in the other. A closer enquiry revealed, however, certain significant differences between the two areas, and, as both the similarities and the differences throw an interesting light upon the earth-movements which affected these areas during the Llandovery Epoch, we believe that it will serve a useful purpose to bring them to the notice of the Society. The observations upon which the comparisons are based are contained in the accounts of the respective areas, except that some additional facts relating to the northern part of the Llandovery district are recorded in this paper and on the map which accompanies it (p. 408).
Both districts lie on the eastern flank of the Towy Anticline, and on the same general line of strike. The rocks belong to the shelly facies, but contain an occasional graptolite. About 5 miles away to the west, the Llandovery rocks of Rhayader and of Ystradffin mark the position of the western flank of the Towy Anticline, but these belong to the graptolitic facies. The axis of that anticline is not situated midway between the eastern and the western Silurian outcrops; it must, in fact, pass within a mile or two west of the base of the Silurian in both the Garth and the Llandovery
On some Occurrences of Spherulitic Siderite and other Carbonates in Sediments
Authors: Spencer Edmondson 
Published: October 2009

I. Introduction, and Summary of Earlier Work
Mineral crystallizations possessing a radiate or divergent form are of common occurrence in certain types of igneous rocks, and to a more limited extent in sedimentary rocks. In igneous rocks these structures were first examined and described by H. Vogelsang (1), who gave to them the name of ‘spherulitic structures’, a term which has since been employed by petrologists for these igneous rock-growths in particular and for similar structures in general.
J. P. Iddings (2), in 1891, in a review of these igneous spherulites, pointed out that their essential feature was crystallization outwards from a centre or from a number of neighbouring centres, with a divergent or radiate arrangement, and that any concentric zoning or banding present was incidental to the radiate growth, since such bands or zones become truncated at points of contact with an obstacle, or with an adjacent spherulite.
Dr. Alfred Harker (3), in his ‘Natural History of Igneous Kocks’, discussed these igneous structures, and suggested that they had been formed by relatively rapid crystallization from saturated or supersaturated solutions.
In sedimentary rocks, spherulitic structures occur sometimes in the form of large isolated individuals, and sometimes as colonies of small interfering units. The latter variety which, on the one hand, possesses many of the features of igneous spherulites, appears to pass gradually, on the other hand, by an increase in the amount of zoning or banding, into true oolitic structures.
Modern research in colloid chemistry has brought new facts to
Report on the Non-Marine Mollusca
Authors: Kennard Alfred Santer , Woodward Bernard Barham 
Published: October 2009

Botanic Garden Pit, Cambridge.
Fifteen species were obtained from this section, namely :—

Of these, the most interesting form is
Sphærium dickinii
Clessin. We have previously recorded this species from the Pleistocene of Crayford and Barnwell Abbey as S.
mænanum
Kobelt, but Clessin’s name has priority. It is quite unknown from any other of the Pleistocene deposits in these islands. This gravel is probably of the same age as that of Barnwell Abbey.

Milton Road, Cambridge.
We have identified twenty species from this deposit, namely :—
Although no extinct forms were present, it is a typical mid-Pleistocene assemblage, and this deposit is probably of the same age as the gravel of Barnwell Abbey.
Travellers’ Rest Pit, Cambridge.
From the upper gravels of this section three species were obtained, namely :—
It is quite impossible to say anything as to the age of this deposit, except that it may be late Pleistocene.
Bordeaux Pit, Little Chesterford (Essex).
We have identified ten species from this deposit, namely :—
This faunule would appear to indicate rather a late Pleistocene age.

From the Black Gable, Storey’s Way, Cambridge, a valve of
Corbicula fluminalis
(Müller) was obtained at a depth of 3 feet, probably indicating a deposit of the same age as the Barnwell Abbey gravel.

Pear Tree Inn Pit, Hildersham.
From this section we have determined eleven species, namely:—
This deposit is probably of late Pleistocene age.
Manea.
The various pits in the neighbourhood of Manea have yielded the following species :—
All these
The Geology of the Cayman Islands (British West Indies), and their Relation to the Bartlett Trough
Authors: Matley Charles Alfred 
Published: October 2009

The Cayman Islands, a small dependency of the British Empire, with a local government controlled by the Government of Jamaica, occupy an isolated position of exceptional interest, both geographical and geological, in the Caribbean Sea. Situated between Jamaica and Cuba, and flanked on the south by the great depression of the Bartlett Trough, which descends over 20,000 feet within 18 miles of the shores of Grand Cayman, they are the only projecting peaks in the submarine ridge that extends from the Sierra Maestra of Cuba to the Misteriosa Bank in the direction of British Honduras. This ridge, though a recognized submarine feature, is irregular, and a depression of 7000 feet lies in it between Grand Cayman and the Lesser Caymans.
The dependency consists of three islands, of which the two smaller, Cayman Brac and Little Cayman, are separated by only 4 miles of sea, while the third, Grand Cayman, is about 60 miles away. Cayman Brac is situated about 125 miles north-west of Montego Bay (Jamaica), and Grand Cayman lies 178 miles west-north-west of Negril Point, the nearest point of Jamaica, and about 150 miles from the Isle of Pines (Cuba). The combined area of the three islands is about 100 square miles. Columbus discovered the Lesser Caymans in 1503, and named them ‘Las Tortugas’, as the shores were swarming with turtle. Grand Cayman was discovered at some later unknown date, and is first recorded in history as being in the occupation of Spanish buccaneers. Europeans appear to have been
On Bolopora undosa
gen. et sp. nov.: a Rock-building Bryozoan with Phosphatized Skeleton, from the Basal Arenig Rocks of Ffestiniog, (North Wales)
Authors: Lewis Herbert Price 
Published: October 2009

In the course of many years' map-making and searching for fossils among the cleaved and altered Cambrian and Ordovician rocks which compose the Moelwyns and the Manod, and the Slate-Belt of Blaenau Ffestiniog, Prof. W. G. Fearnsides has noted the almost general occurrence of streaks and nodules of some dark fine-grained, banded, chert-like material in the basal part of certain conglomeratic lenticles or beds, at or near the surface of discordance where Tremadoc and Arenig rocks adjoin, that is, in the lowest layers of the so-called ‘Garth Grit’. In 1913, when Prof. E. J. Garwood gave his Presidential Address on ‘Algæ as Rock-Builders’ to Section C at the Birmingham Meeting of the British Association, Prof. Fearnsides exhibited specimens of the nodular material which he had collected from the basal layers of the Garth Grit exposed in the cliff at the head of Cwm Bowydd, 100 yards south of the new hospital at Blaenau Ffestiniog, and from Bryn Glas. At that time, Prof. Fearnsides had recognized that the micro-structure of the nodules afforded evidence of their organic origin, and suggested that they had been built up by algal incrustation upon a grit or pebble base. As, however, biologists were unable to discern any real resemblance between micro-sections of the nodules and those of algae, no interpretation of their structure was at that time forthcoming.
Since the Birmingham B.A. Meeting, quarrymen, endeavouring to exploit an unproved vein of slate at Bryn Glas, west of Llyn Morwynion, have opened further chambers in the
The Geology of the Country between Drygarn and Abergwesyn, (Breconshire)
Authors: Davies Kenneth Arthur 
Published: October 2009

The region with which this paper deals lies in the north-western corner of Breconshire, and is situated some 5 miles north of Llanwrtyd Wells, the nearest place of note. The area surveyed is one bordered on the south-west by the rivers G-wesyn and Culant, both tributaries of the Irfon, and stretches roughly 4 miles to the north of this line; its western boundary is marked by the Irfon—Towy watershed. Abergwesyn, a small village, stands at the junction of the Irfon and the G-wesyn.
The district comprises part of the plateau of Central Wales, and is drained by the Towy and tributaries of the Wye, of which the Irfon, roughly bisecting the area, is the most important. The Irfon and its two main tributaries, the Gwesyn and the Cammarch, cut through the rocks generally at right angles to the strike, so that the streams (at least on the south side, where the valleys are deeply incised) afford good sections through the greater part of the succession.
The country on the north, however, closes in to form a desolate moorland at a height of about 1600 feet, rising to 2115 feet in Drygarn, a prominent mountain-top which can be seen from most parts of Central Wales. This northern region is thickly covered with peat, so that the rock-exposures are much fewer and of by no means so satisfactory a character as on the southern side of the area.
The district has, apparently, never been described in detail, and there are no difinite
The Geology of North-East Land (Spitsbergen)
Authors: Sandford Kenneth Stuart 
Published: October 2009

This paper is the result of exploration carried out in 1924 by the Oxford University Arctic Expedition, and observations are also included which were made by Mr. C. S. Elton with the Merton College Expedition of 1923.
North-East Land is about 100 miles long from east to west, and some 80 miles from north to south. That it is so little known is due to its peculiar position remote from the Gulf Stream, which keeps the western coast of the main island of Spitsbergen remarkably clear of ice-pack. On the other hand, North-East Land is struck by the cold Polar current which brings large quantities of ice from the neighbourhood of Franz Josef Land. This current divides, to pass along both the northern and the southern coasts. These factors, together with almost incessant fog, combine to make North-East Land difficult of approach, except late in the season or in unusually favourable years. Moreover, unless an expedition is prepared to winter there, the time available for scientific research is extremely limited.
We owe our introduction to the geology of the northern coast to Baron A. E. NOrdenskiöld (1), who, in the spring of 1873, sledging along the sea-ice, made close observation of its structure (2). Landing near its eastern end he traversed the dome of ice to a point about half-way down the western coast, whence he skirted the shore back to Low Island and returned by water tp his base at Mossel Bay (see fig. 7, p. 632).
Among others
Jurassic Chronology: III—Some Faunal Horizons in Cornbrash
Authors: Buckman S. S. 
Published: October 2009

This communication was commenced and mainly written several years ago: it was intended to form the concluding part of the paper on Watton Cliff (III, 8) following after consideration of Fuller's Earth, Great Oolite, etc., strata. But that paper grew to a length which rendered necessary exclusion of studies of strata later than Inferior Oolite. Now lack of time makes further partition necessary, so that the Cornbrash portion is taken by itself.
The Cornbrash has usually been described as a comparatively thin band of limestone-rock stretching continuously across England from the coast of Dorset to the coast of Yorkshire, parting the Oxford Clay above from Forest Marble Clay below. It is implied in such description that the Cornbrash is a synchronous deposit, which took a short time to form, and that it contains a comparatively homogeneous fauna.
Is such a view correct, or is the continuity of the Cornbrash deceptive? Is not this band of limestone made up of various heterochronous deposits and how far is its fauna homogeneous?

Many years ago, my father noticed the phenomena which form a basis of the present studies—the distribution of dissimilar faunas —in regard to the brachiopods of the Cornbrash. In 1853, speaking on the subject at the Meeting of the British Association for the Advancement of Science (II, 2) he remarks: ‘The author expressed his opinion that certain oolitic Terebratulæ (viz.
T. digona, obovata, lagenalis, ornithocephala
) should be considered as forming one species, at the same time admitting that these forms characterized
The Nature and Origin of Soil-Polygons in Spitsbergen
Authors: Elton Charles S. 
Published: October 2009

The observations recorded in this paper are largely the result of work carried out during the summer of 1924, the bulk of which was done on Reindeer Peninsula, Liefde Bay, in Northern Spitsbergen, and, unless otherwise stated, the notes refer to that place. I wish to acknowledge my indebtedness to Mr. George Binney, the leader of the Oxford University Arctic Expedition, for giving me every facility that lay in his power, and to Dr. K. S. Sandford, geologist to the expedition, who has allowed me to use some of his observations, and whose advice has been of great value. I also wish to thank Mr. R. C. Spiller for examining and giving me his opinion on some soil-samples; Mr. O. W. Richards for certain useful notes on polygons; and Mr. D. Kempson for the care with which he has made prints of some of the photographs.
While investigating the factors which affect the distribution and succession of Arctic animals and plant-communities I was brought up against certain problems of surface-geology, and found it necessary to solve these before progress could be made with the other work. The most important of these problems was presented by the various polygonal arrangements of the soil, which are known to be peculiar to Arctic and Alpine regions, and have now been shown to play a definite part in the processes of weathering and disintegration of rock in such regions. Further, by affecting the nature and drainage-conditions of the soil, they have very marked effects
On Old Red Sandstone Plants showing Structure, from Brecon, South Wales
Authors: Heard Albert 
Published: October 2009

The plants that are described in this communication represent the first recorded occurrence of well-preserved early Devonian plants in England and Wales.
The fossil locality was first observed by Mr. F. N. Gossling, B.A., of the Post Office Survey Department, who informed Prof. A. H. Cox of the occurrence. Prof. Cox and I subsequently examined the locality, and collected a large number of specimens, and I am greatly indebted to Prof. Cox for handing over to me the investigation of the fossil plants. The quarry from which the fossil plants were collected is situate on the western side of the road between Merthyr and Brecon, and lies 7½ miles south of Brecon. (See fig. 1, p. 196.)
The plant-remains are entombed in sage-green arenaceous shales, which are intercalated among the typical sage-green sandstones of the Senni Beds of this locality. The fossil plants appear to be confined to the sediments of finer grain.
Some of the plants in this Brecon assemblage of early Devonian types assume an increased importance, on account of their perfect mode of preservation, which enables a more or less complete account of the anatomy of the vegetative organs to be furnished.
The plants exhibit great diversity in their mode of preservation. At first sight, most of the fossils appear to consist of carbonaceous material. A closer investigation, however, reveals the fact that in many cases a carbonaceous film merely covers the interior of the stem, which has been subject to varying degrees of pyritization.
In some