bluuebunny/crossref_metadata_2025_split huggingface dataset:
The Loch na Cille Boulder Bed and its place in the Highland Succession
Authors: Elles Gertrude Lilian 
Published: October 2009

I. Introduction and Literature
The authors of the Geological Survey Memoir on Knapdale, Jura, and North Kintyre stated in 1911 that the real interest of the Tayvallich peninsula was far from being exhausted in their account, and that the geologist who visited its western shores would be well rewarded.

This is undoubtedly true, for this region of the South-West Highlands, which includes all the promontories west of Loch Sween and south of Carsaig Bay and Loch a' Bhealaich, together with the adjacent islands, seems to afford some definite clues, hitherto apparently overlooked, which may prove to be important in the solution of the two great problems of Highland geology—the succession and the structure. To deal first with the succession: there may be said to be a general agreement amongst the workers in different parts of the area that the rocks seen belong to what has been termed the Loch Awe Group, which comprises the following members:—

Quartzitic Series

Limestone-Slaty-Schist Series (Tayvallich Limestones)

Boulder Bed

Tayvallich Volcanic Series

There is, however, considerable difference of opinion upon the relationship of these beds to each other, and to the rock-groups of other regions outside this district. Some geologists, reading the whole in the light of what is seen in the Loch Awe country and some supposed evidence in the lavas, would place the Volcanic Series at the top and the Quartzitic Series at the bottom; this is the interpretation finally put forward in the Survey Memoir, where the supposed evidence of
The Eocene and Pliocene Deposits of Lane End, Buckinghamshire
Authors: Wooldridge Sidney William , Ewing Colin James Craig 
Published: October 2009

An account of the geology of the Lane End district was published in 1925 (Wooldridge & Gill), following special excavations undertaken by a Committee of the British Association for the Advancement of Science with the object principally of confirming H. J. Osborne White's earlier account of quartzose gravelly elements in the Reading Beds. The pit described by him was reopened in part, and further exposures of the gravelly beds were examined, notably in a pit on Bolterend Common. The conclusion reached was that the London Clay was normally superimposed on the beds in question, and that their Eocene age was thereby definitely established. This interpretation carried with it two important corollaries: namely, (a) that the Chalk cover, north-west of the London Basin, must have been locally breached in early Eocene times, permitting the contribution of Lower Cretaceous and Jurassic material to the Eocene sediments; and (b) that a distinctive polygenetic marginal facies of the Reading Beds formerly existed, of which the Lane End Reading Beds were a surviving remnant.
Recently, much new geological information has become available in this district. New pits have been opened and certain of the older exposures have been extended. Moreover, a water reservoir has been constructed on the hill-top in Widdenton Park Wood and a water-tower erected on the companion hill-top of Fining Wood. In connexion with them, an extensive series of deep pipe-line trenches was dug; these were kept under continuous observation by one or other of the present authors and the information obtained
Geological Observations on the Northwest Frontiers of the Anglo-Egyptian Sudan and the adjoining part of the Southern Libyan Desert
Authors: Sandford Kenneth Stuart 
Published: October 2009

In the autumn of 1932 an expedition led by Major R. A. Bagnold, Royal Corps of Signals, traversed about 6000 miles of country between the Nile, the southern boundary of Italian Libya, and the northern and eastern frontiers of French Equatorial Africa (Bagnold, 1933). The geological objects of the expedition were to map the route and to study the wedge of Sudanese territory, lying between the northeastern frontier of French Equatorial Africa and the southern part of Libya, known as the Sarra Triangle, east of which lies the massif of 'Uweinat. The border hills of Erdi and Ennedi, where in Sudanese territory, and the oases of the southern part of the Libyan Desert were also to be studied.
Scientific work was practically limited to the line of route, since so long a journey without permanent bases for water, fuel, and supplies must be executed with the utmost dispatch. The zones of operation lie hundreds of miles from the nearest administrative centres, and any severe breakdown must prove serious; moreover, care was necessary in case of encounters with the fugitives from Kufara, captured by the Italians in 1930, and with unadministered people who make raids from the border hills. Much of the country in the vicinity of these hills proved almost impracticable for motor transport. As part of the ground had not previously been visited by Europeans, the following account may serve as a preliminary survey.
The expedition owed material support to the Sudan Government, the Royal Geographical Society, and Dr.
The Superficial Deposits of The Country north of Stratford on Avon
Authors: Tomlinson Mabel Elizabeth 
Published: October 2009

The district under discussion in this paper comprises:—

(a)
Areas in which the superficial deposits have been mapped and studied in detail by the author
(Pl. XXVII, map).

(i)
The valley of the Warwickshire Avon between Leamington and Stratford and of
its tributary, the Dene, together with the adjacent country extending eastwards to the longitude of
Compton Verney and Leamington, and westwards to the river Arrow.

(ii)
The country roughly bounded by the longitude of Warwick
and Kenilworth Castle (W. 1° 35′′) on the east and by the upper valley of the
Alne on the west, and extending northwards from the district described above (i) to the country
included in the Birmingham Sheet (168) of the Geological Survey 1-inch map.

(iii)
The valley of the Alne to its junction with the Arrow.

(b)
A wider area, surrounding the aforementioned districts, in which the superficial deposits have
been examined, but where continued observation has not been possible.

Reference will be made to the lower valley of the Warwickshire Avon, the superficial
deposits of which I have described elsewhere (Tomlinson, 1925), and to the valley of the Warwickshire Stour, the superficial deposits of which have been described by Mr. H. G. Dines (Richardson and others, 1929) and myself (1929).
The object of this paper is to attempt a classification of the superficial deposits of the areas which have just been defined, with a view to determining their distribution and relative age. Since the district presents so many difficulties of interpretation and appears
The Stratigraphy and Tectonics of the Cross Fell Inlier
Authors: Shotton Frederick William 
Published: October 2009

I. Introduction
The Cross Fell inlier of older Palaeozoic rocks extends for 16 miles from Roman Fell to near Gamblesby, as a narrow belt of highly-disturbed country parallel to the north-north-west and south-south-east escarpment of the Westmorland and Cumberland Pennines. Its boundary on the east is formed by the outcrop of the gently dipping Carboniferous sediments which constitute the Alston Block (Trotter and Hollingworth, 1928). On the west, if we include as parts of the inlier certain blocks of greatly disturbed Carboniferous strata, the boundary is defined by the appearance of the down-faulted Permo-Triassic rocks of the Vale of Eden. These are folded into a gentle syncline, or series of synclines in echelon, devoid of complex folding and fractured by but few faults. Between these two bounding regions of quiet tectonic history, the inlier exhibits a complex maze of folds, faults, and thrusts which are not limited to the outcrops of older Palaeozoic rocks. For some distance to the north, faults and steep dips affect the Carboniferous formations east of the Pennine Fault; while south-eastward from Roman Fell the disturbances continue with undiminished intensity for seven miles or so until, east of Brough, some, at least, appear to merge into the Dent Fault system of earth movements.
It is unnecessary, at this stage, to recall more than a few of the papers which deal with the Cross Fell area. Early work by Goodchild (1874, 1889) and by Nicholson and Marr (1891) made great advances in the stratigraphy of the area.
The Ordovician Rocks of the Trefriw District (North Wales)
Authors: Davies D. A. Bryn 
Published: October 2009

The area described is a rugged and mountainous tract on the eastern flanks of Snowdonia, lying largely between the villages of Dolgarrog, Trefriw, and Capel Curig. The eastern boundary is defined by the alluvial flats of the Conway valley, and the northern by the Afon Porthllwyd and Afon Eigiau. In the south and west, the mapping has been carried as far as was considered necessary for the elucidation of the geology.
The area is shown on the six-inch Ordnance Survey Map, Caernarvonshire, Sheets XVIII and XIII, with portions of the quarter-sheets XIV SW. and XIX NW., and on the one-inch Geological Survey Map, Sheet 78 SE. (Old Series). The results of the present work are embodied in the map (PI. VII) accompanying this paper.

The area was first described by Sir Andrew Ramsay (1866), who himself mapped the greater portion of the district. His colleague Aveline was responsible for the mapping of the country “east of Llyn Eigiau”. Ramsay regarded the whole succession of “slates and grits with interbedded felspathic traps, felspathic and sandy ashes” as “Caradoc or Bala” age, and recognized at the top of the volcanic series in the neighbourhood of Llyn Crafnant and Llyn Geirionydd a bed of muddy crystal tuff—“a dark blue or black slaty base containing numerous scattered phenocrysts of yellow felspar.” In this “topmost igneous bed” he found at Cwm Llanerch, 2½ miles south of Llanrwst, an abundance of
Trinucleus concentricus
, Leptæna sericea, and “other common Bala fossils”.

Ramsay considered the upper ashes of
The Aymestry Limestone of the Main Outcrop
Authors: Alexander Frances Elizabeth Somerville , Caldwell Née 
Published: October 2009

I. Inroduction
The main outcrop of the Aymestry Limestone forms a sinuous ridge, doubled between Aymestry and Ludlow, about 1000 feet above O.D. It is 25 miles long and lies within an area measuring 12 miles from north to south and seven miles from east to west, the boundary of which passes through Craven Arms, Ludlow, Aymestry, and Leintwardine.
The limestone was named by Murchison in 1839, after the village of Aymestry, in the neighbourhood of which it is well exposed, and since that date no detailed work has been done on it.
In 1900 Dame Ethel Shakespeare (then Miss Wood) described the Lower Ludlow shales, and in 1906 Miss Elles and Miss Slate described the beds lying above the limestone in parts of the area here described. The later paper contains an excellent summary of all the work done in the neighbourhood up to 1906.
III. Detailed Description of the Aymestry Limestone
(a) Lithology
Three lithological types are found in the Aymestry Limestone. The most common is a fine-grained, massive or nodular, blue-grey limestone occurring in beds of from one to three feet in thickness, separated by greenish calcareous shales in bands from a half to six inches thick. The fossils in this type of limestone are complete, the valves of the brachiopods being still articulated, and many specimens are still apparently in the position of growth. Fossils are more or less evenly distributed throughout, the rock and there is no sorting, as in the second form of the
The non-Marine Lamellibranchs of the North Wales Coalfield
Authors: Wood Alan 
Published: October 2009

In the recent correlation of the Upper Carboniferous of England and Wales published by Professor A. E. Trueman (1933) the most obvious omission was a consideration of the North Wales coalfield. At that time, indeed, only three lamellibranch species had been reported from the area. In the present paper knowledge of the fauna is extended and the modern zonal scheme is applied to the coalfield. The floral zones recently introduced by Dr. E. Dix (1934) can be partially distinguished in the area, but these form the subject of a separate paper (Wood 1936b). The results are in accord with those based on the lamellibranchs.
The area dealt with is shown on the map (Fig. 1), while the relationship of the lamellibranch zones and the coal-seams can be seen from Fig. 8.
The Geological Survey memoirs dealing with the coalfield (Wedd & King 1924; Wedd & others 1923, 1927) contain little account of the fauna of the Coal Measures.

The shell
Carbonicola robusta
(J. de C. Sowerby) (sic) was recorded from above the Main Coal at Mancot, near Hawarden, and was considered to indicate the Lower Coal Measure age of this seam.
Anthracomya calcifera
Hind was collected from the Upper Coal Measures to the south of Ruabon, while this shell and
A. phillipsi
(Williamson) were found in the Upper Coal Measures south of the Dee, outside the limits of the area dealt with in this paper. No other records were published, and shells were stated to be rare in the Coal Measures
Petrographic Description of Volcanic Rocks from Turkana, Kenya Colony, with notes on their Field Occurrence from the manuscript of Mr. A. M. Champion
Authors: Smith Walter Campbell 
Published: October 2009

The province of Turkana in Kenya Colony comprises a tract of country west of Lake Rudolf bounded on the north by the Anglo-Egyptian Sudan and on the west by Uganda. It covers an area of about 27,000 square miles, and until recently the geology was entirely unknown. During his term of office as Provincial Commissioner, Mr. Arthur M. Champion surveyed the country and made a large collection of specimens of rocks and careful observations on the geology, particularly the physical geology, of the region.
During his administration, Turkana was visited by two scientific expeditions, one under the leadership of M. C. Arambourg in 1932–3, and one led by Dr. V. E. Fuchs in 1934. M. Arambourg's expedition was directed mainly towards the investigation of beds rich in mammalian remains, discovered in 1902–3 during the expedition of le Vicomte Robert du Bourg de Bozas in the lower part of the valley of the Omo at the north end of Lake Rudolf. In the course of the expedition he made some observations on the volcanic rocks, and the petrography of his specimens has been written by Mme E. Jérémine (1935). These specimens I was privileged to study in the Mineralogy Department of the Muséum national d'Histoire naturelle at Paris in the spring of 1937 by the courtesy of Professor Orcel and Mme Jérémine.
An account of Dr. Fuchs's expedition has been published (1935) and the geological results will be available shortly. I have been privileged to examine his specimens, but although he
The Petrography of the Permian Rocks in the Southern Part of the Vale of Eden
Authors: Versey Henry Cherry 
Published: October 2009

I.
Introduction

The Permian rocks of the Vale of Eden are readily divisible into two areas contrasting in their lithology. The main part of the valley shows a development of the well-known Penrith Sandstone, but south-east of a line drawn from Dufton to Grackenthorpe this sandstone is replaced by thick breccia —the Brockrams—until near Winton, south of Brough-under-Stainmore, it almost disappears. In this southern portion of the area the Penrith Sandstone is covered by plant-bearing beds, the Hilton Plant Beds, and a magnesian limestone. To the west, the Permian rocks rest uncomformably on Lower Carboniferous strata, while to the east they are covered with apparent conformity by Triassic rocks, although locally there is evidence of overlap or even unconformity. Detached masses of Permian material are found in the broken ground along the Outer Pennine Fault near Long Fell and Kirkland. The type section in this southern area is taken, following Harkness (1862, p. 207) and Goodchild (1893), in Hilton Beck and the country on the opposite bank of the Eden. The succession here is as follows:—
This general succession may be traced to the south-east as far as the River Belah, but in this distance the breccia beds thicken at the expense of the sandstones. South of the Belah section the Hilton series disappears, but at Merry Gill Viaduct, near Kirkby Stephen, a magnesian limestone, full of pebbles, occurs. The whole of the Penrith series suffers considerable diminution in thickness. To the north-west the Hilton Beck succession may be traced as
The effects of frost action and solifluxion around Baffin Bay and in the Cambridge District
Authors: Paterson Thomas Thomson 
Published: October 2009

These studies constitute part of the geographical results of the Wordie Arctic Expedition, led by Mr. J. M. Wordie of St. John's College, Cambridge, to Melville Bay and the east coast of Baffin Land in the summer of 1934.
It was found that some of the arctic soil forms had strong similarities to structures observed in the Pleistocene gravels of the Cambridge area, and that, treated together, these forms and structures would throw new light on the mechanics involved in their formation.
The studies are divisible into three portions: frost cracking, polygonal structures, and solifluxion.
I. Frost Cracking
Travellers in northern and eastern Siberia report that the tundra, in places, is scarred and seamed by ramifying linear depressions flanked by low ridges, the depressions being marked out by a darker growth of mosses, generally interlacing to form roughly polygonal features many feet across. They have not, so far as is known, been excavated (Sukatchev 1911, Nikoroff 1928).
Leffingwell (1919) observed frost cracks occurring in Alaska only in “muck”, though Smith (1909, p. 272), writing on the Nome deposits, noted a “series of ramifying streaks of a black peaty material cut in irregular directions across the layers of sand and gravel”, which streaks he attributed to frost cracking. Leffingwell (1919, p. 211) also noted “frequently straight lines leading across the gentle undulations of sandspits”, though he saw no polygonal forms in such places. However, his classic treatment of the theory of the formation of ground ice led him to generalize on
The Borrowdale Volcanic Series of Coniston, Lancashire
Authors: Mitchell George Hoole 
Published: October 2009

I. Introduction
The Furness Fells lie at the extreme northern corner of Lancashire between the higher reaches of the River Duddon and the upper end of Lake Windermere. The highest summits are those of Wetherlam (2502 feet), Swirl How (2630 feet), Brim Fell (2611 feet), Old Man of Coniston (2633 feet), and Dow Crag (2555 feet). These are but the most prominent peaks on a high ridge extending from north-east to south-west. This watershed divides the waters which flow westwards to join the Duddon and northwards to the Brathay from those which find their way south-eastwards into Coniston Lake. From north to south there are six principal becks which, rising near the watershed, make their way ultimately to Coniston Lake. In the north Tilberthwaite Gill descends through its picturesque gorge along a course which is nearly northward in direction as far as Tilberthwaite, where, turning abruptly south-east and then south-west, it becomes known as Yewdale Beck, thereafter forming a strike stream almost along the junction between the Borrowdale Volcanic and later rocks. Approaching Coniston it again turns south-eastwards over the low ground to the lake. Church Beck is formed by the gathering together of a bunch of tributaries which are known as Red Dell Beck, Levers Water Beck, draining the tarn of that name, and Low Water Beck, which issues from Low Water. These all descend in marked steps to the Coniston Copper Mines, below which the main stream of Church Beck descends by a further succession of falls to
The Killough-Ardglass Dyke Swarm
Authors: Tomkeieff Sergei Ivanovich , Marshall Charles Edward 
Published: October 2009

I. Introduction
The dykes described in this paper are those occurring on the coast of County Down, Northern Ireland, between Killard Point in the north and Inner Dundrum Bay in the south-west (Pl. XX); the length of coast-line is approximately 20 miles.
The country rock of the district is entirely of hard, compact Lower Palaeozoic grits and slates, highly folded and faulted and considerably affected by glacial action, which tend to give a very bold and rugged shoreline. Exceptions occur in only one or two places; Ballyhornan Bay is occupied by a wide stretch of sand with few rock exposures; Dundrum Bay includes a very long stretch of sand with few outcrops of solid rock. The fact that a number of dykes are found in the few outcrops that are exposed in these covered stretches suggests that the solid rock concealed by the sand may contain many more.
South of Dundrum Bay, the Palaeozoic grits and slates again rise above tide-level and the rocky coast-line is traversed by the numerous dykes of the Mourne swarm, which have already been described by the present authors (1935). In the same paper the geographical relations of the dyke swarms of the Tertiary Province of Northern Ireland have been discussed, and consequently need not be referred to here.
The first survey of the dykes of this swarm was completed by Traill and Egan (1871), who gave a brief account of some of the dykes. No further attention appears to have been given to the
The Garabal Hill-Glen Fyne Igneous Complex
Authors: Nockolds Stephen Robert 
Published: October 2009

I. Introduction
The Garabal Hill-Glen Fyne igneous complex lies just west of the head of Loch Lomond and stretches westward into Glen Fyne. The complex occupies an area
of some 12½ square miles embraced by sheets 37, 38, 45 and 46 of the one-inch Geological Survey map of Scotland. It breaks through various Dalradian schists already folded and regionally metamorphosed and these suffered thermal metamorphism when the rocks of the complex were intruded. The age of the complex is generally accepted as Lower Old Red Sandstone, owing to its close resemblance to other igneous masses of that age in Scotland.
The earliest account of the area is given by Dakyns and Teall (1892) in a paper which has since become classical. The boundaries of the massif were accurately delineated, some of the rock types were mapped, briefly described and chemically analysed, and the hypothesis put forward that they had been derived from some parent magma by a process of differentiation operating at depth. A description of part of the western portion of the mass and of the thermal metamorphism induced there in the surrounding schists was published in the Cowal Geological Survey memoir (1897, pp. 96–101) and in the mid-Argyll memoir (1905, pp. 92–3). Finally, a paper by Wyllie and Scott appeared in 1913, dealing mainly with the ultrabasic rocks of the complex but including some data on the basic and intermediate rocks. The variation in the ultrabasic and dioritic rocks was ascribed to local variation