bluuebunny/crossref_metadata_2025_split huggingface dataset:
THE MAIN DONEGAL GRANITE
Authors: PITCHER WALLACE SPENCER , READ HERBERT HAROLD , CHEESMAN R. L. , PANDE I. C. , TOZER C. F. 
Published: October 2009

The Main Donegal Granite is described in its regional setting and details are given of the envelope of Dalradian metasediments and the relation to the earlier members of the granite complex. A separation is made into the Main Granite Proper and the structureless Trawenagh Bay Granite, covering areas of 140 and 20 square miles respectively.
The Main Granite Proper is a biotite-granite showing a medium-grained, grey, apparently marginal type in the south-east of its outcrop, and a coarser, lighter-coloured variety in the north and west. Pegmatite forms a roof facies in the south-west. Flow structures are shown by mineral orientation and a perfect banding ; the latter is produced by granites of varying grain and biotite content, the finer-grained biotite-richer type being of earlier consolidation and possibly constituting a roof phase. Banding is everywhere steep and along the NE.–SW. length of the Main Granite Proper. Within the Granite, perfectly aligned trains of free-swimming rafts of country rocks, seen to be derived from roofs or walls, extend for some dozen or more miles in the Granite and agree perfectly with its flow pattern.
The contact-zones of the Main Granite Proper show marked sheeting by granite and, in these zones, high-grade contact schists are produced with staurolite and garnet—deformation, and heating have acted together. The marginal parts of the Granite and the adjacent contact-zones show an intense shoar structure, lineation and mullioning, the planar structures running vertically NE.–SW. and the linear elements plunging gently north-eastwards in the north-eastern part of the outcrop and south-westwards in the south-western. The production of these structures was contemporaneous with that of the contact schists and is related to the emplacement of the Main Granito Proper.

The phenomena shown by the Main Granite Proper and by its roof and walls are consistent with the almost horizontal flow, from north-east to south-west, of viscous magma in a long narrow body beneath a pronged roof and between steep walls. A broad divergence of raft-trains as they are followed into the granite shows that it cannot be of replacement origin, nor can the room problem be solved by major stoping. The authors propose that
lateral magmatic wedging
is the mechanism of emplacement this great granite body.
THE LUDLOVIAN AND DOWNTONIAN ROCKS OF THE KNIGHTON DISTRICT, RADNORSHIRE
Authors: HOLLAND CHARLES HEPWORTH 
Published: October 2009

The Knighton district displays a thick “ basin facies ” succession of over 6000 feet of Ludlovian rocks, which has been divided into five groups. The Old Red Sandstone, above the basal
Platyschisma helicites
Beds, is divided lithologically into Yellow, Green, and Red Downtonian. Correlation is made with successions in other Welsh Borderland areas.

Conditions of deposition of the Ludlovian rocks are considered. The Ludlovian succession shows two distinct faunas separated by a group of very poorly fossiliferous strata, apparently representing conditions unfavourable to the development of benthonic forms.
Structurally the most notable feature is a disturbed belt some 3½ miles wide, which occupies the western part of the area. It comprises a set of NE.–SW. folds associated with strike-faulting and much fracturing. The belt can be traced north-eastwards and south-westwards considerably beyond the limits of the Knighton district.
LOWER CARBONIFEROUS ROCKS IN COUNTY WEXFORD
Authors: GEORGE T. NEVILLE 
Published: October 2009

The Lower Carboniferous rocks of the Wexford syncline rest unconformably on the Bray Series. Basal conglomerates are followed by highly fossfliferous limestones and shales, with some dolomites, of mid- and upper Tournaisian age, the Old Red Sandstone and the Lower Limestone Shales being overlapped. The earliest beds of the Viséan stage are algal limestones and calcite-mudstones. They are overlain by crinoidal dolomites probably no younger than Upper Caninian in age.
The Tournaisian rocks are closely similar in facies to those of Hook Head . The basal Viséan rocks compare in lithology with, and are of about the same age as, the Calcite-Mudstone Group in South Wales. They are probably the correlatives of the lower part of the Waulsortian reefs of the Ardmore - Cork outcrops, and they suggest that no part of the Hook sequence is younger than Tournaisian.
The local migratory shoreline of the Dinantian Leinster massif is defined by the Tournaisian base, the rate of overlap reflecting a coastal slope of at least 65–70 feet to the mile. The a brupt change in lithology from Tournaisian to Viséan rocks hints at the occurrence of a westerly continuation from South Wales of the mid-Dinantian break, though proof is lacking. A pre-Viséan down warp may be discerned along the line of the present-day St. George's Channel.
THE STRATIGRAPHY OF THE UPPER CARBONIFEROUS ROCKS OF THE BIDEFORD REGION, NORTH DEVON
Authors: PRENTICE JOHN EDWARD 
Published: October 2009

The succession in an area lying mainly north and west of Bideford is described. The Northam and Abbotsham Beds, of “coal measures” facies, are followed by the slumped Greencliff Beds and then by the greywackes of the Cockington Beds. These are unconformably overlain by Permo-Triassie breccias.
The structure is interpreted as a series of E.–W. trending, faulted periclines super-imposed upon a southerly early regional dip. The folding and most of the faulting can be shown to be pre-Permo-Trias in age.
THE THREE FOLD-SYSTEMS IN THE METAMORPHIC ROCKS OF UPPER GLEN ORRIN, ROSS-SHIRE AND INVERNESS-SHIRE
Authors: FLEUTY MICHAEL JOHN 
Published: October 2009

The major structures in the area immediately north-east of the Monar area (
Ramsay 1958
) are a synform and a neutral fold with axes plunging south-west and south respectively. They appear to have formed on the western limb of a larger and earlier major N.–S. antiform. They are, however, separated from the axial region of this fold by a slide, which cuts out a maximum of 7700 feet of the structural succession, and was apparently formed contemporaneously with the synform and neutral fold.

All these structures were affected by refolding and distortion during a third phase of folding; this gave rise to structures plunging south-west, which on occasion obscure the earlier structures. It is suggested that the divergent attitudes of the major synform and neutral fold were one effect of this distortion.
This three-fold structural history is supported by evidence of the relations of minor structures to the major folds and by observations of earlier small-scale structures refolded or overprinted by later ones.
Petrofabric diagrams demonstrate that recrystallization and reorientation accompanied all three phases of folding.
GEOLOGICALIN TERPRATION OF MAGNETIC ANOMALIES OVER THE ASKRIGG BLOCK
Authors: BOTT MARTIN HAROLD PHILLIPS 
Published: October 2009

A vertical field magnetic survey of the Askrigg block discloses an E.–W.-striking belt of magnetic basement rocks between Wensleydale and the Craven faults, terminated to the west by the Dent line. These rocks are thought to underlie directly the Carboniferous Limestone in the region of maximum anomalies and to underlie the Ingletonian rocks farther south. The northern margin of this belt is apparently the steeper.
Gravity anomalies observed over the northern half of the block suggest that the northern margin of the magnetic belt may be pierced by a small granite mass elongated also in an easterly direction. The postulated granite appears to have a slight magnetic effect. Two-dimensional models that are approximately consistent with the gravity and magnetic profiles have been constructed with the help of rapid computing methods.
The belt of magnetic basement rocks, together with the postulated granite, appears to have stabilized the subsequent structural history of the southern half of the Askrigg block. The outcrop-pattern of the Dent and Craven lines correlates closely with the margin of this resistant block, and this fact suggests that it is the resistant block, rather than wrench-faulting, that has controlled the pattern. It is also notable that mineral veins are commoner to the north and south of the belt. There is no clear connexion between the distribution of mineral veins and the postulated granite.
OUR SOCIETY AND THE GEOLOGICAL SCIENCES
Authors: HOLLINGWORTH SIDNEY EWART 
Published: October 2009

Two major topics are considered. First, the activities of the Society : its publications, its services to Fellows (particularly those resident overseas), its finances, and the possibility of its contributing more effectively to the development of education and research activities in geology and in promoting their applications. Secondly, consideration is given to means of promoting the greater effectiveness of geological sciences in the life and economic health of the nation, especially in activities overseas.
Other countries have large government-financed organizations for exploring and developing mineral resources. In Great Britain there appears to be a contrast between the official attitudes towards mineral resources on the one hand and to other national assets, such as agriculture and manufacturing industry, on the other.
The massive growth of technical aid to the emerging nations, especially those of Africa and Asia, makes the development of mineral resources a matter of overriding importance. Relatively small numbers of British geological personnel appear to be engaged in major international aid programmes to which Great Britain makes substantial financial contributions.
Many other countries provide official teams of geologists and mining engineers for aid programmes abroad. In the U.K., unfortunately, an obvious nucleus for such operations has to a large extent been dispersed.
It is suggested that a major reorganization of British-based geology is required which would provide careers for a substantial number of geologists who would be available for secondment overseas. There is a considerable potential for the greater use of the staffs of geology departments of the universities of this country in co-operation with those of the new overseas universities in aid programmes. Other fields of growing importance, such as hydrogeology and marine geology, are mentioned.
The structure of the Rogart igneous complex, Sutherland, Scotland
Authors: SOPER NORMAN JOHN 
Published: October 2009

The Rogart igneous complex, Sutherland, is of Newer Granite age and consists of a zoned tonalite-granodiorite-granite body (the central granodiorite complex) emplaced in Moine metasediments which to the east and north are involved in a peripheral zone of migmatization (the migmatite complex).
Although the migmatite complex is genetically related to the central complex, it is not a static contact-effect. Evidence is presented which suggests the following sequence of events. An ascending body of granodiorite magma was preceded by a 'front' of migmatization. When it reached a higher crustal level, migmatization ceased and continued forceful intrusion of the magma deformed the migmatites into a plastic envelope around the expanding magma body, which consolidated as tonalite and granodiorite. Lateral distension exceeded upward movement and a partly funnel-shaped structure resulted. The granite cross-cuts structures in the tonalite and granodiorite and was emplaced later under more brittle conditions.
An analysis of the deformation of 'regional' linear structures around the complex confirms the forcefully intrusive nature of the igneous mass. The geometry of the deformation of the migmatites during the emplacement of the central complex is related to the stress field obtaining at this period as deduced from planar and linear structures in the tonalite.
On the geology of central Badakhshan (north-east Afghanistan)
Authors: DESIO ARDITO , MARTINA ERCOLE , PASQUARÈ GIORGIO 
Published: October 2009

Territory explored by the Italian geological expedition to Badakhshan during the summer of 1961 is described.
The metamorphic rocks have been divided as follows: Faydzabad Gneiss, Qara Mughul Gneiss and Rabat Gneiss (pre-Devonian);
Halqa Jar Amphibolite (from Devonian to Jurassic); black slates (undivided and probably of different ages).
Besides these complexes there are several lithostratigraphic units, with semi-metamorphic facies.
The igneous rocks are granite, granodiorite, quartz-diorite, and tonalite of three ages: Upper Permian-Lower Triassic, Upper Jurassic-Lower Cretaceous, and Tertiary.
The sedimentary rocks, Cretaceous, Eocene, and Neogene, have been subdivided as follows: Shingan Formation, Qara Bulaq Formation, Mashad Limestone, Mohammad Aba Sandstone, Gazestan Formation, Baba Darwes Formation (marls and limestones with Cretaceous fossils), Kharakan Formation (with Eocene fossils), Kokcha Formation (Neogene), and Taluqan Gravel (Quaternary). Fluvio-glacial deposits, loess, alluvial and lacustrine deposits, landslides, and talus slopes, all Quaternary, are also present.
Several formations border an old anticlinal core formed by the Faydzabad Gneiss. The anticline trends north-south. Groups of formations separated by unconformities are deformed to varying degrees of intensity.
Layered intrusive rocks in the Lewisian of the North-West Highlands of Scotland
Authors: BOWES DONALD RALPH , WRIGHT ALAN EDWARD , PARK ROBERT GRAHAM 
Published: October 2009

Layered ultrabasic and basic intrusive rocks occur in three structural environments in the Lewisian of the North-West Highlands of Scotland and 41 such layered masses, or groups of masses, in the area between Loch Laxford and Loch Torridon are recognized and described. Their igneous origin is indicated by the common mineralogical banding, the occurrence of sedimentation features, particularly current-and wedge-bedding, and by the association, in banded sequence, of ultrabasic, basic, and anorthositic rocks which are similar in chemical composition to corresponding rock-types in other layered igneous complexes.
One group of metaperidotites and metagabbroic rocks has undergone coeval, or near-coeval, granulite-facies metamorphism and folding, probably after an earlier period of disruption. Subsequently, about 2400 m.y. ago, further disruption and amphibolitization took place. No evidence of the later events is shown by most of these masses, but they have moved tectonically, as units, by slip around their margins during subsequent episodes of deformation. The masses are usually in the form of massive metaperidotite lenses generally concordant with the banding of the adjacent gneisses or granulites, although a few serpentinite masses now have the form of tectonic diapirs. Low-grade retrogressive metamorphism in zones of steep reverse faulting affected some of the masses.

Another group of metaperidotites has been deformed by isoclinal folding on axes trending nw-se with steeply dipping axial planes so that the mineralogical banding of the ultrabasic bodies is now vertical. Subsequent hydrous metamorphism, sometimes with the introduction of potassium, has caused marginal alteration of many of these masses to talc-trem-olite-carbonate-serpentine rocks, sometimes with biotite and muscovite. Complete minera-logical reconstitution to this low-temperature hydrous assemblage has taken place in some cases, but relict banding remains. After this episode, which was about 1500 m.y. ago, the rocks were deformed by a series of box-like folds, with steeply plunging axes, causing local deflexion of the banding from its
nw-se
trend.

A small group of banded picrites and gabbros has intrusive relations to these gneisses and shows subsequent retrogression with the uralitization of the pyroxenes.
The Songwe scarp carbonatite and associated feldspathization in the Mbeya Range, Tanganyika
Authors: BROWN PETER EVANS 
Published: October 2009

The carbonatite and associated rocks described occur on the Mbeya mountain range, which is at the junction of the eastern and western rift valleys in south-west Tanganyika. The main occurrence of carbonatite is a dyke-like body, possibly in discontinuous lenses, with an approximately linear outcrop trending nw-se over a distance of some 12 miles at the base of the Songwe scarp. This scarp bounds the Mbeya Range and delimits the southern end of the Rukwa trough. The carbonatite was emplaced in a zone of structural weakness along which there was probably rift-valley faulting before the introduction of the carbonatite and along which there has since been considerable faultmovement. The rift-faulting here follows the north-westerly trend of the crystalline basement rocks. Typically the carbonatite is ankeritic, fine-grained, and not flow-banded. Commonly there is a fragmentary or brecciated texture, the fragmentary material consi sting largely of feldspathized and carbonated country-rock. Minor amounts of niobium, uranium, and thorium are present but the location of these elements is uncertain and rare accessory minerals have not been detected.
Feldspathization by the introduction of potassium is strongly developed in the immediate vicinity of the carbonatite and also sporadically elsewhere on the Mbeya Range; both quartzofeldspathic cataclastic schists and coarsegrained mica-garnet schists have been converted to aggregates of potassium feldspar. Such feldspathization is particularly well displayed in the vicinity of Itete on the north-east flank of the Mbeya Range, where elongated belts of feldspathized country-rock illustrate the strong control exercised over their formation by the regional schistosity. Injection and brecciation of these feldspathized schists by carbonatite veins is common.
It is suggested that the Songwe scarp carbonatite is a high-level representative of the crystallization of a parent carbonatite at depth; the unusual form is due to the strong structural grain of the basement schists of the area.
Tertiary sediment cores and microfossils from the Pacific Ocean floor
Authors: RIEDEL WILLIAM REX , FUNNELL BRIAN MICHAEL 
Published: October 2009

Tighty-five cores containing either Tertiary sediment or abundant reworked Tertiary micro-fossils have been selected for description from approximately 900 Pacific deep-sea cores collected by the Scripps Institution of Oceanography between 1950 and early 1961. The area covered by the 85 cores extends from about 45°
n
to 45°
s
, and from 151°
e
to 73°
w
, although most were collected within the tropics.

A brief lithological and micropalaeontological description is given for each core; wherever possible, a photograph of the core and a profile of the adjacent topography are provided. The Radiolaria, planktonic Foraminifera, and calcareous nannoplankton were investigated. Stratigraphical interpretations are based on all three groups and supported by lists of species of Radiolaria and Foraminifera. The ages range from Eocene to Pliocene, with reworked Cretaceous at one locality.
Tentative interpretations are put forward regarding the distribution of pelagic sediments and water masses in the Pacific during the Tertiary. Miocene and Pliocene sediments are similar at most localities to near-by Quaternary deposits, and it is concluded that near-surface currents and water masses were generally similar to those of the present day. The only apparent exceptions are a displacement of the northern boundary of the Equatorial Current System to a location about 5° north of its present position at 139°w, and possibly a 5° southward displacement of the southern boundary of the Subarctic Current at 173°w.
During the Oligocene, the northern boundary of the Equatorial Current System was apparently 7° north of its present position at 137°w. At 130–50°w, the southern boundary of that current system and the northern edge of the West Wind Drift appear to have been situated near their present positions.
Eocene occurrences show greater departures from the pattern of Quaternary sediment types. The northern boundary of the Equatorial Current System appears to have been situated about 9° north of its present position, at 135–65°w. The few occurrences of this age south of the Equator cannot readily be interpreted in terms of a pattern of water masses similar to that of the present day.
The evidence from the cores does not indicate any substantial lowering of the calcium carbonate compensation depth during the Tertiary, with the exception that in low latitudes in the north-east Pacific it may have been depressed to 5100m during the Oligocene.
No systematic relationship between topography and the localities of Tertiary sediments cropping out or shallowly buried has so far been worked out.
The Pre-Cambrian history of Sweden
Authors: MAGNUSSON NILS H. 
Published: October 2009

Several difficult problems remain to be solved in the Pre-Cambrian of Sweden but in recent years progress has been made with the establishment of a time-scale. Two major phases of regional alteration, marked by extensive gneissification culminating in the formation of special granites and pegmatitic intrusion of regional extent, have been dated. In both cases temperatures were so high that argon-40 was entirely or almost entirely expelled. The ages obtained are therefore those of the rejuvenation of the rocks. The earlier of the two phases took place 1700 m.y. to 1800 m.y. ago, marking the close of Svecofennian-Karelian time. It corresponds to the Hudsonian in Canada and the Penokean in the U.S.A. A younger phase of regional alteration, the Sveconorwegian, is dated at 950 m.y. to 1000 m.y. and took place at the end of Gothian-Dalslandian time. This corresponds to the Grenville in both Canada and the U.S.A. The high-grade gneisses of south-western Sweden are bounded to the east by a zone of marked schistosity. Age-determinations from this zone have given an age of about 1200 to 1300 m.y.
These and other ages are discussed and an account is given of the complicated history of the Pre-Cambrian of Sweden.