bluuebunny/crossref_metadata_2025_split huggingface dataset:
The Glaciation of Western Edenside and Adjoining Areas and the Drumlins of Edenside and the Solway Basin
Authors: Hollingworth Sydney Ewart 
Published: October 2009

This paper is divisible naturally into two parts. The first deals with the glaciation and deglaciation of western Edenside and adjoining areas, including the eastern and north-eastern parts of the Lake District as far north-west as Skiddaw. The work, which was commenced in 1923 as the result of problems which arose during the re-survey of the Brampton Geological Survey Sheet, has been facilitated by the fact that throughout I was in constant touch with Dr. F. M. Trotter, who was investigating the area east of the River Eden at the same time.
At an early stage in the work it was found that the drumlins were parallel to the ice-fronts for considerable distances. This was entirely unexpected and led to the study of the drumlins of a much larger area; this study forms the subject of Part II. Its results are of more than local interest, and this, together with the difference in area dealt with and the complexity of the problem, justifies, it is hoped, its separation from the chronological sequence in Part I. The drumlins mapped by my colleagues, Messrs. E. E. L. Dixon, J. M. Maden, L. H. Tonks, and F. M. Trotter, in the Carlisle Sheet, and by Mr. T. Eastwood in parts of the Bewcastle and Cockermouth Sheets, together with a larger area east of the Eden mapped by Dr. Trotter, have been incorporated in Part II. To these investigators my thanks are due for permission to utilize the result of their mapping; for its
The Post-Glacial Deposits of the Lincolnshire Coast
Authors: Swinnerton Henry Hurd 
Published: October 2009

Between the Lincolnshire Wolds and the coast there lies a narrow belt of low-lying land usually referred to as the Lincolnshire marsh. Within this belt two types of scenery exist. The one, founded on boulder-clay, is characterized by a well-wooded hummocky surface. It occupies a continuous strip of country along the foot of the wolds (Pl. XXX), but its seaward margin is irregularly indented and has outlying patches standing up like large mounds in the marshland proper. The latter constitutes the second type of country. It is flat and almost treeless, and is made up of stiff clays mainly of estuarine origin. The process of building up this marshland is still going on along the coast north of Mablethorpe and south of Skegness. The first-mentioned portion of the coast lies under the lee of Spurn Point, the latter lies within the shelter of the Wash, where extensive salt marshes exist.
Between Mablethorpe and Skegness the coast is being slowly eroded. This fact is disguised by the absence of cliffs and the presence of an almost continuous covering of sand which hides the outcrops of the marshland clays. Owing to the action of the waves and currents, this sheet of sand as it drifts southwards becomes broken by valley-like hollows, often more than a mile long, which extend obliquely across the beach. These hollows are scoured by strong and dangerous currents which sweep away the sand and both expose and erode the clays beneath. They offer the only natural and, at
Jointing in the Great Scar Limestone of Craven and Its Relation to the Tectonics of the Area
Authors: Wager Lawrence Rickard 
Published: October 2009

The Great Scar Limestone of Kilnsey Moor, 4 miles northwest of Grassington in Wharfedale, is traversed by many approximately parallel lead-veins whose direction is marked, in the field, by a series of small trial holes for lead. Over the same area, the limestone is cut by two series of joints which are nearly at right angles to each other. One of these sets of joints is parallel to the lead-veins. Traced towards the North Craven Fault, near Skirethorns, both the lead-veins and the joints parallel to them are found to change from a north-east and south-west direction to an east-north-east and west-south-west direction.

These observations, which were made in 1926, were sufficient to suggest:

(1)
that the jointing was probably formed in pre-Permian times, as the joints may be occupied by lead-veins for whose pre-Permian age there is considerable evidence;

(2)
that the jointing was produced by regional stresses, since it is constant in direction over large areas;

(3)
that the jointing, since it alters its direction on approaching the North Craven Fault, may be connected in some way with the faulting and may, therefore, throw some light on the nature of the Craven Fault-system.

To test these tentative deductions, and, if possible, to decide the relations between the joints and the tectonics of Craven, a detailed map of the direction of the jointing in the horizontally-bedded Great Scar Limestone between Dentdale, Wensleydale, and the Craven Faults was begun.
Previous
The Geological Work of the Cambridge Expedition to East Greenland in 1929
Authors: Parkinson Mark Mervyn Leofric , Whittard Walter Frederick 
Published: October 2009

East Greenland, a country of high coastal mountains receding under the cap-ice and of great fjords bounded by towering cliffs, has, within the last decade, attracted once again the attention of investigators. After an unsuccessful attempt in 1923, Mr. J. M. Wordie succeeded in reaching land and exploring Gael Hamkes Bay and Franz Josef Fjord in the very favourable ice year of 1926 (Wordie, 1927). That same summer, Dr. Lauge Koch took a party to Scoresby Sound, and himself made a sledge-journey the next spring northwards to Germania Land, returning by way of the fjords (Koch, 1929). Since Dr. Koch wished to elucidate further the stratigraphy of the Palæozoic rocks in 1929, the third Cambridge Expedition of 1929 concentrated mainly upon a determination of certain tectonic problems in the pre-Old Red Sandstone rocks, and upon a journey inland from Kjerulf Fjord into unknown country (Wordie, 1930). Had time permitted, a party was to sledge from the head of Gael Hamkes Bay as far north as Queen Louise Land, in order to determine the relations existing there between the sedimentary and metamorphic outcrops; but owing to delay in the pack-ice, this plan had to be abandoned.
The large fjords, Franz Josef Fjord and King Oscar Fjord, are connected through Antarctic Sound, and measure respectively about 110 miles and 45 miles in length. They have many branches, most of which traverse the rock-sequences across the dip, and afford cliff-sections of multicoloured bare rock, often attaining 6000 feet in height. The fjord-system is
The Loch Doon ‘Granite’ Area, Galloway
Authors: Gardiner Charles Irving , Reynolds Sidney Hugh 
Published: October 2009

I. I
introduction

F
our
large and several small plutonic masses occur intrusive in the Lower Palaeozoic rocks of the south-west of Scotland, the four large masses being those of the Criffel, the Cairnsmore Q.J.G.S. No. 349B of Fleet, the Loch Doon area, and the Cairnsmore of Cars-phairn. It is the object of the present paper to describe the Loch Doon mass, the intrusions which surround it, and its metamorphic aureole.

The Loch Doon mass is intrusive into Ordovician sediments showing the prevalent north-east to south-west strike which was imparted to the rocks of much of the south and west of Scotland by the Caledonian movements. These rocks include Hartfell and Glenkiln beds, represented by grits, flags, and black graptolitic shales, and Arenig beds, which include grits and radiolarian cherts. The district is included in Sheet 8 of the 1-inch Geological Survey map of Scotland.
The plutonic rocks occupy a large area extending for a distance of 11½ miles from Loch Doon in the north to just south of Loch Dee in the south, and spread over about 47 square miles. The outcrop is somewhat hour-glass shaped with a maximum width of 6½ miles, and the plutonic rocks are almost everywhere surrounded by high hills composed of metamorphosed Ordovician sediments, which form the Kells Range on the east and the Merrick Range on the west. Both ranges are, for the most part, well over 2000 feet high, Corserine in the Kells Range rising to 2668 feet and Merrick to 2764 feet. Through
The Geology of the N'Changa District, Northern Rhodesia
Authors: Jackson Gerald Christopher Arden 
Published: October 2009

I. I
ntroduction

T
his
paper presents a brief account of the general geology and petrology of a previously unmapped portion of the Northern Rhodesian copper belt, and covers approximately 800 square miles of territory. The map-area forms a portion of the Rhodesian Congo Border Concession now being explored by the Rhokana Corporation, Ltd. The area is bounded on the south by the 13th parallel of south latitude, on the east by the boundary between the Rhodesian Congo Border and the N'Kana Concessions, and on the west by the Lufwanyama River. Its northern boundary lies approximately 6 miles north of the Kafue River near N'Changa, and 8 miles south of the Belgian Congo border.

The district is in the heart of the Northern Rhodesian copper belt, and includes the N'Changa Copper Mines Ltd. Concession and its extensions; it lies in close proximity to the other principal copper deposits of Northern Rhodesia and the Katanga.
Within the last few years, Northern Rhodesia has attracted wide interest by virtue of its recently discovered copper deposits, which in tonnage and tenor of ore now rank amongst the foremost of the world. Lying within this region, the N'Changa district, in respect of both geology and mineralization, is typical of the Northern Rhodesian copper belt, and contains, perhaps, a wider range of rock types and a greater abundance of natural exposures than is usual in neighbouring districts. Consequently, the results of the studies described in this paper may assist in the elucidation of the broader problems of
The Geology of the Western Macdonnell Ranges, Central Australia
Authors: Madigan Cecil Thomas 
Published: October 2009

I. I
ntroduction

T
he
literature on the geology of Central Australia is now becoming somewhat voluminous. Owing to the vastness of this largely desert area, the sparseness of settlement, which is almost wholly confined to the neighbourhood of the overland telegraph line, and the cost and difficulty of travel in a land where waters are few and far between and petrol only available if sent out by camel, the geological work has been in the nature of rapid route reconnaissances in scattered directions.

Although the chief ore deposits are in the eastern MacDonnell Ranges, very little has been done in that area, while the western ranges, though quite devoid of any mineral wealth, have received a relatively large amount of attention geologically. The reason for this is that on the western side of the telegraph line the geological structures show comparative simplicity, while to the east there has been much more complex movement, the formations occurring in jumbled hills and ranges in such confusion as only closely detailed mapping could unravel. The key to the geology of the whole area lies in the west.
I first visited the western MacDonnell Ranges in company with Sir Douglas Mawson in 1927. A hurried motor journey was made to near Glen Helen Station, 90 miles west of Alice Springs, to inspect a deposit of saltpetre in limestone caves Only five days were spent in the field, three of them in travel ling, and there was little time for geological work apart from examining the
The Permian Lavas of Devon
Authors: Tidmarsh Wilfred George 
Published: October 2009

I. I
ntroduction

T
he
rocks to be described comprise the relics of a suite of lavas forming two main groups of exposures : (i) the Exeter lavas, constituting a zone of outcrops north of Dartmoor, and (ii) lavas south of Dartmoor occurring near Kingsbridge and in the Maker peninsula south-west of Plymouth. These rocks present features of special interest as being the latest surface manifestations of the Dartmoor cycle of igneous activity, and are products of a later stage of magmatic differentiation than any other known rocks of the region.

All the occurrences have been previously recorded and, in part, described, but the probable modes of origin have not hitherto been discussed. The present investigation was, therefore, directed to the study of the suite as a whole in the light of recent petrological progress, the object being to determine the precise character and sequence in time of the Devon lavas and to discuss the genetic relationship with the igneous rocks in the Devon sub-province.
(a) Distribution of the Lavas
Geographically, the lavas occur in five groups : (i) immediately to the south-west of Exeter, (ii) in the valleys of the Exe, Culm, and Clyst, (iii) in the Crediton valley, (iv) west of Tiverton, and (v) to the south of Dartmoor.
With the exception of the rocks in groups (ii) and (v), the lavas occur generally at or near the boundary between the Culm Measures and the Permian. Lavas of group (ii) appear to lie higher in the succession and, with minor
The Tertiary Ring Complex of Slieve Gullion (Ireland), with Petrological Notes by Herbert Henry Thomas
Authors: Richey James Ernest 
Published: October 2009

I. I
ntroduction

T
he
Tertiary plutonic rocks of north-eastern Ireland are confined to two main areas—the Mourne Mountains in Co. Down and the mountainous tract of country extending from the Carlingford peninsula, in Louth, north-westwards to beyond Slieve Gullion, in Co. Armagh. They are intruded into the middle of the well-known belt of Ordovician and Silurian strata which continues north-eastwards across the Irish Sea to form the Southern Uplands of Scotland. Near Carlingford, the Carboniferous Limestone also is cut by the plutonic rocks, while the country rocks immediately around Slieve Gullion consist of the Caledonian (or Lower Old Red Sandstone) granite of Newry (fig. 1).

The Tertiary age of the plutonic rocks has been for many years accepted, on account of their petrological similarity to those intruded into the Tertiary basalt lavas in western Scotland. In Ireland, the basalts overlie the Antrim chalk and transgress southwards across the Carboniferous, Silurian, and Ordovician sediments of Armagh and Down. Remnants of the basalts are now known to occur still farther south, within the Slieve Gullion and Carlingford area. These, as is shown below, are earlier than the Slieve Gullion plutonic rocks, and direct evidence of the Tertiary date of the intrusive complexes is thus forthcoming.
reservoir was formed by subsidence rather than by melting. Not improbably the western portion of the Newry granite itself occupies the space left by a cauldron subsidence of Lower Old Red Sandstone date. If at some depth in the crust there lay a subsided mass of country rock,
The Upper Estuarine Series of Northamptonshire and Northern Oxfordshire
Authors: Thompson Beeby 
Published: October 2009

In Northamptonshire, between the Lincolnshire Limestone and the Great Oolite Limestone in the north-eastern part of the county, and between the Northampton Sand (or the Lower Estuarine Beds) and the Great Oolite Limestone in all other parts of the county, occurs a series of variable beds, largely variegated clays containing abundance of vegetable matter of probably freshwater origin, interspersed with brackish-water beds and with distinctly marine beds. To this aggregate J. W. Judd, in 1867, gave the name ‘Upper Estuarine Series’, which he then thought represented the Stonesfield Slate or Lower Zone of the Great Oolite of the more south-westerly parts of England, Oxfordshire in particular.
In Northern Oxfordshire, between certain Inferior Oolite Limestones or White Sands (the time-equivalents of the Lincolnshire Limestone), or ferruginous sands (the equivalents of the Variable Beds of the Northampton Sand or even the ironstone series) below, and the Great Oolite Limestone above, occurs a series of beds which in various parts physically, and in others palæontologically, agree, as does the complete set in sequential position, with the Upper Estuarine Series of Northamptonshire.
It is an important object of this part of the paper to show how the Northamptonshire and Oxfordshire sections at this geological horizon may be more definitely correlated. The name ‘Upper Estuarine’ is retained for the complete series in both counties as free from the complication of an incomplete local place-name (Chipping Norton Limestone Series) and an incomplete and unsatisfactory palæontological one (Neæran Beds).
In attempting to correlate a variable set of
The Geological Structure of the Eastern Mendips
Authors: Welch Francis Brian Awburn 
Published: October 2009

I. Introduction
The area under discussion comprises that part of the Mendip Hills lying east of a north-and-south line from Oakhill to Shepton Mallet, and extending eastwards as far as Frome.

Investigations were begun by Miss A. E. Bamber and Miss B. Gullick, who, being later prevented from continuing their undertaking, allowed me to conduct my research over their territory. They gave to me all their notes and maps, which have been of much use and for which I wish to express my gratitude. The later stages of my work were completed whilst holding a Carnegie Teaching Fellowship in the University of St. Andrews. I should also like to take this opportunity to thank Dr. Stanley Smith for his examination of the D
3
material, and Miss H. Muir-Wood for naming certain Productids.

The summary of literature dealing with this area, since it must of necessity be almost a repetition of that given in my paper (1929) on the adjoining area to the west (the central Mendips), will be omitted here. Two papers, however, by Prof. S. H. Reynolds (1907 & 1912) describing the Silurian inlier in the eastern Mendips, and one by G. E. Bush (1925) on the Avonian of Vallis and Spring Gardens were not included in that summary.
Geologically, the area consists of the Beacon Hill pericline, which is the most southerly situated of the four echeloned periclines constituting the Mendip Hills. This pericline forms an approximately east-and-west ridge which attains at its western end a maximum altitude
The Geology of the Fairbourne-Llwyngwril District, Merioneth
Authors: Jones Brynmor 
Published: October 2009

I. Introduction
This paper deals with that part of western Merioneth which lies between the village of Arthog and the town of Towyn. The area is included in a rectangle, the longer side of which runs north-east and south-west and is 8 miles long; the shorter side has a length of 3 miles. The western and northern boundaries are formed by Cardigan Bay and by the estuary of the River Mawddach. On the southern side, the area is bounded by the alluvium of the River Dysynni, and the south-eastern margin is the old Roman road which runs from Llanegryn to Dolgelley. The region is comprised within the Ordnance Survey 6-inch map, quarter-sheets Merioneth 36 S.W. & S.E., 40 S.E., 41 N.W., N.E., & S.W., 45 N.E., and 46 N.W., and within the Geological Survey 1-inch map, Sheet 59 N.E. (Old Series).
The topography of the district to be described is in marked contrast to that of the country adjoining it on the north-east, which includes the range of Cader Idris and its foot-hills. Sharp, craggy ridges are absent, the hills having smooth, rounded outlines and grassy slopes. The even contours are largely due to a mantle of glacial drift which smooths out pre-glacial irregularities and in many places conceals the solid geology.
The greater part of the area is upland country of low agricultural value, woodland being absent and the general aspect monotonous and bare. The maximum elevation, on Pen-y-garn, is 1500 feet above O.D. The main lowland region lies
The Geology of the Country between Abergwesyn (Breconshire) and Pumpsaint (Carmarthenshire)
Authors: Davies Kenneth Arthur 
Published: October 2009

I. Introduction
In 1926, I described the area between Abergwesyn and Drygam, and subsequently the district on the north-east, between Abergwesyn and Rhayader, formed the subject of another paper (Davies, 1928). The present work is a continuation of the previous surveys, and deals with the country between Abergwesyn and Pumpsaint in Carmarthenshire (see fig. 1). The southern boundary is the main road from Lampeter to Llanwrda, while the northern and western limits are defined by the Towy–Teifi watershed.
The area forms part of the western flank of the Towy anticline, and has been mapped on the scale of 6 inches to the mile. It is about 130 square miles in extent, and is included within the Geological Survey maps, Old Series, 1-inch sheets 41 and 56 S.W. It is essentially that part of the Central Wales plateau which is drained by the upper Towy and its tributaries. The country is given over almost entirely to sheep-farming, and on the north-west it is desolate and somewhat inaccessible.
II. Historical Summary
Sir R. I. Murchison (1839, p. 342) mentioned the ‘slaty rocks and their associated conglomerates’ which are found on the north-west of the better-known areas with shelly fossils. He placed these slaty rocks within the ‘Cambrian’ system, and referred especially to Rhandirmwyn, where lead-mining was being carried on even at that time.
The Geological Survey Horizontal Sections, published in 1844 and 1845, throw some light on the nature of the folding, for No. 3 passes through Ogofau, near Pumpsaint, and No.
The Geology of Eastern Jersey
Authors: Mourant Arthur Ernest 
Published: October 2009

I. Introduction
The island of Jersey stands in a key position between Normandy and Brittany; being easily accessible to English geologists, it also forms a valuable link between the rocks of England and France. Yet the work of many scores of investigators has not sufficed to determine satisfactorily the age and structure of its rocks or to bring to light the concealed structures which join it to Normandy and to Brittany. In this paper some advance is attempted in these directions.
The island is roughly rectangular, 10 1/2 miles from east to west and 6 1/2 from north to south. It forms a dissected plateau, some 300 feet high, overlooking the sea in the north but terminating against discontinuous coastal plains elsewhere.
The north-eastern corner of Jersey is formed of conglomerate and the other three corners of plutonic rocks. Between the granites in the western half of the island is a series of unfossiliferous mudstones and shaly grits, generally known as shales. Most of the eastern half of the island consists of volcanic rocks.
The area described in the present paper includes all the volcanic group, together with certain sediments and intrusive rocks lying to the north-east, south, and west of them. The whole of the eastern half of the island is dealt with except the highly complicated intrusions of the south-eastern coast. The thin layer of Pleistocene deposits which covers much of the solid geology is not considered in this paper.
The area