bluuebunny/crossref_metadata_2025_split huggingface dataset:
The Ardara granitic diapir of County Donegal, Ireland
Authors: Akaad M. Kamal 
Published: October 2009

Summary
The composite diapir of Ardara, County Donegal, foreibly displaced contact-altered Dalradian rocks of its envelope by folding, thrusting and shearing. The intrusion consists of a granodiorite core surrounded by a mantle of course tonalite. The outer part of the core is made up, in the north, of contaminated quartz-diorite and, in the south, of less contaminated granodiorite. These rocks, and the tonalite, are well foliated. The central part of the core is composed of uncontaminated and unfoliated biotite-granodiorite
The emplacement of the body is believed to have begun with the movement of granodiorite magma along a pre-existing thrust-plane. The magma came in contact with basic rocks of an older complex and mobilized part of this complex, sweeping it upwards as a plastic skin which consolidated to form the tonalite mantle. Magma contaminated with basic material accumulated within this mantle to form the quartz-diorite and the slightly contaminated southern granodiorite. The outer part of the body cooled and developed radial fractures.
A new upwelling of essentially uncontaminated granodioritic magma pierced the still molten core of the pluton, causing remobilization and further distortion of the envelope. Radial fractures, later followed by tangential fractures, were again formed. At a late stage, the solidifying pluton rose vertically, with resultant shearing of its envelope.
The volcanic rocks of the area between Fishquard and Strumble Head, Pembrokeshire
Authors: Thomas Godfrey E. , Thomas Trevor M. 
Published: October 2009

Summary
Volcanic rocks of Ordovician age, of widespread occurrence within North Pembrokeshire, attain their maximum development in the Pen Caer peninsula, embracing the area immediately north-west of Fishguard and culminating seawards in Strumble 1 Head.
Referred to as the Fishguard Volcanic Series, these rocks are assignable to the Lower Llanvirnian. They reach a maximum thickness of some 3600 feet near Strumble Head itself, but attenuate rapidly towards the south and east so that at Lower Fishguard Harbour they are reduced to some 850 feet.
A well-defined tripartite subdivision is evident over the greater part of this area ; these components in upward succession are the Lower Rhyolite Division, the Pillowlava (Spilite) Division and the Upper Rhyolite Division.
Although pillow-lavas predominate within the Pillow-lava Division, this is made up of a diverse group of rocks, the detailed petrography of which reveals many unusual features. Its thickness of approximately 3000 feet in the extreme north of the Pen Caer peninsula contains the greatest local development of pillow-lavas in Wales. A discovery of particular interest is the presence of an intra-formational series intercalated within the dominant pillow-lavas.
Near Goodwick the two rhyolite divisions reach a combined vertical thickness of some 2500 feet, easily the greatest thickness of Ordovician rhyolitic rocks recorded in Pembrokeshire. Breccias, agglomerates, intercalated ashes or tuffs and perlitic or nodular varieties are of common occurrence, but flinty flour-banded types predominate.
The structure and stratigraphy of part of the Pre-Cambrian outcrop between Church Stretton and Linley, Shropshire
Authors: James John H. 
Published: October 2009

Summary
The use of top and bottom criteria combined with cleavage has shown that the succession is normal for the lower groups of the Longmyndian. The presence of a major overstep of the Mintonian (Portway Group) on to the Synalds Group in Deadmans Batch, with the complete elimination ofthe intervening Lightspout Group, suggests an unconformity at the base of the Mintonian. The eastward creep of the Bayston Group at the expense of the Mintonian when traced from north to south of the area, together with a variation in the dip and strike between these subdivisions, points to another, and possible greater, unconformity above the Mintonian. Although dipping to the west, top and bottom structures show the western half of the Bridges Group and the Oakswood Group to be inverted. This implies a major synclinal structure in the Wentnorian, as the eastern half of the Bridges Group and the Bayston Group have a normal succession. The Uriconian to the west has an inverted and unconformable relationship with the Wentnorian, the unconformities having combined to eliminate the Strettonian and Mintonian.
Interglacial plant remains from the Wolvercote Channel, Oxford
Authors: Duigan Suzanne L. , Sandford K.S. 
Published: October 2009

Summary

The Wolvercote Channel contains deposits with a fauna indicative, first, of warm and then of temperate conditions. These are overlaid by a peaty layer containing plant remains, itself succeeded by deposits indicative of cold conditions. Clement Reid and Bell recorded 23 different flowering plants from the peaty layer. From material in the Oxford University Museum some of Raid's labelled specimens have been re-examined, and further material not labelled by him has now been identified. The newly identified plants include
Atriplex
cf.
hastata
Linnaeus, cf.
Cardarmine pratensis
Linnaeus,
Draba
cf.
incana
Linnaeus,
Pastinaca sativa
Linnaeus,
Potamogeton
cf.
filiformis
Persoon or
pectinatus
Linnaeus, P. cf.
perfoliatus
Linnaeus,
Potentilla
sp.,
Rumex
cf.
acetosa
Linnaeus, cf.
Saxifraga
sp., and
Festuca
sp. The ranges and habitat preferences of these plants, together with the plants identified earlier by Reid and by Bell, support a tentative conclusion that the climate was cool temperate. What is more certain is that the landscape was, at least locally, incompletely covered with vegetation.
Pollen analysis of the Nechells interglacial deposits, Birmingham
Authors: Duigan Suzanne L. , Godwin H. 
Published: October 2009

Summary
Pollen diagrams from a deposit of silts and clays at Nechells, Birmingham, are presented. The vegetational history of the deposit and the extent to which the pollen analytical results can be used to determine the age of the deposit and the climatic conditions under which it was laid down are discussed.
Microplankton from the Kimeridge Clay
Authors: Downie Charles 
Published: October 2009

Summary
Planktonic organisms found in the Upper Kimeridge Clay of England are described. This plankton comprises dinoflagellates, hystrichospheres, coccolithophores and bodies of uncertain affinity. Coccolithophores and dinoflagellates alternate as the dominest members ; the abundance of the former varies considerably. The mode of occurrence is described and the stratigraphic value discussed.
A geomorphological comparison between Eastern Brazil and Africa (Central and Southern)
Authors: King Lester C. 
Published: October 2009

Summary
Large parts of central and southern Africa and of eastern Brazil form “stable shield regions” that have escaped orogenic deformation since the late Palaeozoic.
Similar erosional processes operating upon similar terrain in both regions have produced series of denudational and depositional land-forms that are closely comparable upon both the continental and local scales.
Both sub-continents have been subjected to periodic uplift, and in each the uplifts have conformed to a differential pattern that was repeated for the region at each epeirogenic episode ; in the two sub-continents the general pattern of repeated deformation is similar both in space and time.
In both regions, from the Carboniferous until approximately the Jurassic, sedimentation prevailed over denudation, but from the Jurassic onwards denudation exercised the dominant role and the principal features resulting are suites of cyclic land-forms. In each subcontinent the accumulative desert phase of the Triassic was concluded by the outpouring of floods of plateau basalt. The Jurassic denudation produced everywhere a landscape, termed “Gondwana”, of extraordinarily smooth planation, from which all subsequent scenery has been carved.
The following denudational cycles and the related deformations and sedimantary phases are common to both regions:—
1. The Gondwana denudational cycle, followed by the late Jurassic deformations and the early and mid-Cretaceous sediments.
2. The post-Gondwana denudational cycle, followed by the mid-Cretaceous disturbances and the late Cretaceous and early Cainozoic sedimentary series.
3. The “African” and “Sul-Americana” denudational cycles, followed by mid-Cainozoic epeirogenesis and late Tertiary marine and continental deposition.
4. The late Cainozoic denudational cycle, followed by epeirogenesis at the close of the Cainozoic and Quaternary sedimentation.
5. Quaternary valley incision and sedimentation.
The episodes of uplift and warping synchronized with well-established episodes of orogeny in other parts of the world.
The stratigraphy and structure of the Cotherstone Syncline
Authors: Reading Harold Garnar 
Published: October 2009

Summary
The Cotherstone area is a physical and geological depression lying between the two upstanding block areas of the northern Pennines. Structurally it is an asymmetrical syncline pitching gently to the east.

The succession of Carboniferous rocks displayed ranges from late P
2
to late E
2
and includes beds of Yoredale facies of the Middle and Upper Limestone groups, overlain by Millstone Grit.

The tracing of the marine members of the Yoredale rhythmic units or cyclothems has established correlations between the successions of the Alston Block to the north and the Askrigg Block to the south. These show that marine conditions frequently persisted longer to the south and east of the area than elsewhere. Millstone Grit facies enter at a lower horizon on the east and west of the Cotherstone area than they do in the centre, the lower horizon corresponding with the Tan Hill Grits to the south, which, it is suggested, pass laterally into the Coalcleugh Transgression Beds of the north. This is demonstrated by equating the Upper Felltop Limestone of the Alston Block with the Hearne Beck Limestone of Upper Swaledale. The upper horizon, of grit facies, is subjacent to the Botany Limestone and is considered to be the equivalent of the First " Millstone Grit " of Durham and the Water Crag Grit of Upper Swaledale, the Botany Limestone corresponding with the Shunner Fell Limestone.
The Carboniferous rocks of the Donegal syncline
Authors: George T. Neville , Oswald Desmond Henry 
Published: October 2009

Summary
The Donegal syncline in north-western Ireland is a shallow faulted downfold preserving a thickness of over 4000 feet of Lower Carboniferous rocks. Only the lower zones of the Viséan stage are represented : they rest upon the underlying metamorphic rocks with strong unconformity.
Along the south-eastern flanks of the fold the sequence is closely comparable in facies with the Ballyshannon Limestone, the Bundoran Shale and the Mullaghmore Sandstone of the Sligo syncline to the south.
Along the northern and north-western flanks of the fold, the Ballyshannon Limestone passes laterally into arenaceous rocks about Lough Eske and Banagher Hill. The overlying shales, though more persistent, carry tongues and lenses of sandstone and conglomerate that thicken northwards until along parts of the northernmost outcrops the whole Viséan succession is almost completely arenaceous.
The western outcrops, between McSwyne's Bay and Slieve League, display thick basal boulder-beds succeeded by sandstones ; these pass upwards into highly fossili-ferous limestones and shales overlain by sandy oolitic limestones, together about 600 feet thick. The rocks display strong overlap westwards, 2000 feet of the lower beds at Bruckless not being represented in the Largymore syncline.
The minerals of the sandstones and the facies changes indicate the proximity of a northern and north-western shoreline. The floor of the sedimentary basin suffered a near-shore downwarp to accommodate the thick deltaic sediments of the northern outcrops.
The Ballyshannon Limestone and the overlying shales carry a fauna of Upper Caninian and probably early Seminulan age.
The tectonic structure has a caledonoid grain and is partly inherited. Simple in essentials, it is complex in detail with several large oblique fractures that are in part tear-faults.
Fissure Metasomatism in Volcanic Rocks Adjacent to the Shap Granite, Westmorland
Authors: Firman Ronald John 
Published: October 2009

Summary
Localizod alterations in wall-rocks of a pre-granite joint system, and other fissures, in thermally metamorphosed andesites, rhyolites and tuffs have resulted in either epidotization or sericitization.
Epidotization is often associated with the development of Ca-Fe garnets within the fissure and, more rarely, in the wall-rock. Later minerals, such as quartz, calcite, magnetite, haematite and metallic sulphides, occur filling cracks in the garnet in the centro of these garnet-bearing veins. The formation of epidote is attributed to silicification of the wall-rock followed by the introduction of Ca and OH from the granite. Al, Fe, Mg and some Ca migrated toward the fissure, where under higher temperatures in conditions of iron enrichment Ca-Fe garnets formed. Subsequently, movement of the granite mass cause deformation of the country rocks and also opened the garnet-bearing veins to fluids which precipitated to suite of hydrothermal minerals.
Sericitization is associted with the formation of cordierite and is restricted to rocks adjacent to pyrite veins. Al, K, S and OH ions appear to have diffused into the wall-rocks, causing this alteration.
Superimposed folding at Loch Monar, Inverness-Shire and Ross-Shire
Authors: Ramsay John G. 
Published: October 2009

Summary
A sequence of rock types of over 20,000 feet in thickness has been established. Within this succession, rocks originally regarded as inliers of Lewisian Gneiss appear at four horizons ; the author believes them to be in integral part of the Moine Series.
The major folds were formed during two separate episodes of movement. The first major folds have E.-W. trending, southerly dipping axial planes and plunge at low angles to the west. A second set of major folds with NE.-SW. trending, south-easterly dipping axial planes were superimposed upon the earlier folds,refolding the limbs and axial planes of the first folds and distorting the early fold axes and minor structures. Gently dipping first-fold limbs were refolded into gently southwesterly plunging second folds, and steeply dipping first-fold limbs were refolded into steeply or vertically plunging major second folds. During the second folding there was some regeneration of folding about the first-fold axes. The microfabric of the metamorphic rocks shows cross-girdles of quartz c-axes and of biotite 001-plane poles.
Downward-facing structures of the Highland Border
Authors: Shackleton Robert Millner 
Published: October 2009

Summary
The structures in the Dalradian rocks near the Highland Border of Scotland consistently face downwards. They are upside-down. In the south-western districts they face downwards to the south-east, between Loch Lomond and Aberfoyle vertically downwards and from Aberfoyle to Stonehaven downwards towards the north-west. The view that the Upper Dalradian Ben Ledi Grits and Leny Grits are equivalent and younger than the Aberfoyle Slates which outcrop between them is tentatively supported. The Aberfoyle anticline implied by this view must face downwards, not upwards as previously claimed. The downward-facing structures are connected with the recumbent folds to the north-west. The Carrick Castle anticline, formerly regarded as the hinge at the front of the Loch Tay inversion, is thought not to exist. That hinge is either located in the Aberfoyle anticline, which would thus mark the southern limit of the Loch Tay inversion, or, if the Aberfoyle anticline does not exist, the hinge lies in the Ben Ledi Grits. On either view the roots of the Highland Border structures lie north of the Loch Tay flat belt.
The steep zone of down turned and overturned nappes near the Highland Border represents a powerful monocline associated with the Highland Boundary fault. It connects the Grampian Highlands with the Midland Valley. The nappes possibly continue beneath the Midland Valley.
Glacial Lakes anf Spillways in the Vicinity of Madeley, North Staffordshire
Authors: Yates Edward Marshall , Moseley Frank 
Published: October 2009

Summary
Captures by the River Weaver head-streams of the upper Trent drainage have breached the west-facing feature that the North Staffordshire Coalfield presents to the Choshire plain. As the Irish Sea Ice retreated from the coalfield the gaps thus formed were linked in a spillway system through which the melt-waters impounded in lakes against the high ground were discharged into the Trent. The deepening of the channels due to the passage of the melt-water, plus the moraine deposits, has prevented the drainage from recovering completely its former course.
Mircro-organisms and the presence of syngenetic pyrite
Authors: Love Leonard Gregory 
Published: October 2009

Summary

Certain beds of the Scottish Lower Carboniferous Oil Shale Group contain numerous small granules of pyrite. Isolation and subsequent solution of this pyrite has revealed the presence of a hitherto unknown group of microfossils clearly contained within the pyrite. Two new monotypic genera,
Pyritosphaera
and
Pyritella
, are described and their essential role in the production of hydrogen sulphide is suggested in relationship to the formation of syngonetic pyrite.
Sand volcanoes on slumps in the Carboniferous of County Clare, Ireland
Authors: Gill William Daniel , Kuenen Philip Henry 
Published: October 2009

Summary
In the Namurian basin of western County Clare, Ireland, investigated by the first author, there is a fine display of slumping, which recurred frequently during the deposition of some 3500 feet of sands, silts and muds. The slumps occur in sheets and in channels with complex sheared margins, and exhibit a wide variety in size and in the degree and style of break-up. On the majority of the slumps are sand volcanoes. Some of these are quite large (up to 50 feet in diameter), but most are from one to three feet in diameter ; the volcanoes often occur in great profusion. They are interpreted as having been formed under water, by extrusion of sediment-laden water from the slumped masses before burial by undisturbed covering sediments. They provide proof that the slumps were " open-cast " and not buried during the movement. They also indicate a permanent cover of water with only slight wind and current action.
Although there is a clear empirical connexion between volcanoes and slumps, field evidence of feeding fissures or pipes is not common. The manner in which the volcanoes were formed is more fully explained on the basis of models produced on experimental slumps by the second author.
The basal Coal Measures of the South Wales Coalfield from Llandybie to Brynmawr.
Authors: Leitch Duncan , Owen Thomas Richard , Jones David Gwyn 
Published: October 2009

Summary

The basal Coal Measures, from the
Oastrioceras subcrenatum
marine band to the Garw (Cnapiog or Bryn) Coal, have been studied in detail along that part of the North Crop of the South Wales Coalfield which lies between Llandybie in the west and the Clydach valley (near Brynmawr) in the east. This sequence falls mainly within the zone of
Anthraconaia lenisulcata
and its thickness ranges from 380 feet in the west to 130 feet in the east.

Along much of the belt a lower arenaceous portion (the so-called " Farewell Rock ") is succeeded by a predominantly argillaceous division which contains a number of marine horizons. These bands can be identified by means of certain distinctive features. Many of them can be traced into the eastern areas and they show that the sequence is there attenuated and more uniformly arenaceous. This eastward thinning occurs even within separate units of the sequence. It can now be shown that the " Farewell Rock " of the western areas is older than sandstones which have been given this name in the north-eastern part of the coalfield.
The basal Coal Measures of the North Crop are correlated in detail with those of other parts of South Wales and the variations in lithology and thickness are discussed. Isopachyte maps show that the present " structural " form of the coalfield was being moulded, through differential subsidence, in Lower Coal Measures times, with the maximum subsidence occurring in the Margam area. It is probable that these basal Coal Measures were never deposited over the Usk and Forest of Dean regions.
Moine-Lewisian relations at Glenelg, Inverness-shire
Authors: Ramsay John G. 
Published: October 2009

Summary
Metamorphosed psammitic and politic sediments of the Moine Series, together with a complex group of gneisses of Lewisian age, alternate in bands. A study of the relations of the individual members of the Lewisian complex shows that there has been an early phase of migmatization (probably of Scourian age) followed by a period of basic dyke intrusion. Neither of these events is shared by the adjacent Moine rocks.
New evidence indicates that the most extensive area of Moine rocks occurs in a major antiformal core and lies structurally beneath the Lewisian gneisses, whilst the alternating Lewisian and Moine bands represent slices of tectonic origin which came into position before the development of this antiform.
Two sets of major folds have been recognized, and the effects of their interference are discussed. The axial planes of the first folds originally dipped to the east. A second set of major folds with south-easterly dipping axial planes was superimposed across the early folds, distorting the early folds and their associated minor structures. This distortion is a combination of deformation resulting from a simple refolding of the first-fold limbs together with a plastic deformation.
The geological structure of the Wadi el Dirba area of Sinai
Authors: Robson Douglas Arthur 
Published: October 2009

Summary
The Egyptian province of Sinai can be divided into three geological regions: (1) the northern plain, the isthmus, whose surface outcrops are confined chiefly to strata of Mesozoic age, (2) the mountainous peninsula, formed of a complex of Pre-Cambrian rocks, and (3) the western coastal belt, flanking the Gulf of Suez and largely made up of a series of rocks belonging to the Mesozoic and Tertiary. The rocks of the coastal belt have been involved in the rift-faulting movement which produced the Gulf of Suez trough. The effect of these movements was to break up the whole area into a series of tilted blocks. The rocks of the isthmus dip gently towards the Mediterranean, but this regional dip is broken by a number of fold-axes and associated faults which trend WSW.-EXE. They form the western extension of a similar group in Palestine.
The particular interest in the Wadi el Dirba area lies in the fact that it is there possible to establish the relationship between the isthmus structures and the Rift movements. The field evidence within the area mapped may be summarized as follows:–
1. There are four normal faults belonging to the Rift system. One of them has a dyke associated with it (both dyke and faults can be established in age as Oligocene from evidence outside the area); one fault also appears to show some horizontal movement.
2. Another normal fault, the Dirba fault, running through the area in a direction parallel to the isthmus structures and assumed to be associated with them is displaced by the Rift faults. Movement along the Dirba fault must therefore have ceased before the main Rift faulting began.
Reference is also made to other evidence beyond the area mapped which indicates (1) that the main Rift faulting movement was active during and after Miocene as well as during Oligocene times, and (2) that the isthmus folds may owe their origin predominantly to vertical rather than to horizontal movement.