bluuebunny/crossref_metadata_2025_split huggingface dataset:
Large-scale superficial structures in the Northampton Ironstone Field
Authors: Hollingworth S. E. , Taylor J. H. , Kellaway G. A. 
Published: October 2009

From Major J. C. McM
ath
, B.Sc. F.G.S. :—

The authors are to be congratulated on these detailed researches and conclusions, with their interesting economic implications. The work emphasizes afresh the great caution necessary in the interpretation of tectonics generally and it is clear that a revision of much structural and stratigraphical work is required in the light of the authors' results. It can be expected that wherever strata of strongly contrasting competency under load occur analogous phenomena may be found.
Features similar to those described in the paper, though on a much smaller scale, have been observed by me in the lateritic areas of Lake Province, Tanganyika Territory, particularly in the Saragura and Mawe Meru areas to the south-west of Lake Victoria.
“Dip-and-fault” structure, together with cambering, were noted especially on the lateritic flats abutting on the Rhino and Mabubi rivers. The features were developed a short distance from, and parallel to, the courses of these streams, and they faded out where the laterite was of little thickness or where it directly overlay the igneous country rock. The structures were best seen where the laterite was over eighteen inches in thickness and was underlain by ferruginous earth or clay (uncemented decomposition products of the country rock). Both “dip-and-fault” structure and cambering could also be seen on a very minor scale in old prospecting trenches where these were of some size. No “valley bulging” was observed.
Authors' reply :—
The authors write that they recognize that, as observations accumulate from a
Intraformational Contorted Rocks in the Upper Carboniferous of the Southern Pennines
Authors: Cope Fred Wolverson 
Published: October 2009

Summary
Beds of contorted shale, both overlain and underlain by normally bedded shale, occur in the Millstone Grit and Lower Coal Measures of the Goyt Trough to the west of Buxton. A brief synopsis of the geology of this area is given. The beds of contorted shale, usually from 6 inches to 2 feet 6 inches in thickness, are remarkably constant in horizon throughout the area; the majority directly overlie marine bands, but at least two are unassociated with these fosailiferous shales. Structures discernible within the contorted beds comprise sheer-planes and small folds. On each limb of the Goyt Syncline both the axial planes of the small folds, and the shear-planes, clip towards the major axis at an angle greater than the stratal dip. Wherever the pitch of the small folds can be observed it is northerly, in the same direction as the pitch of the major fold. Contacts of the contorted beds are almost invariably plane surfaces, often polished or bearing slickensides running along the line of dip.
The contorted shsles are considered to be of tectonic origin and to be an expression of adjustment through bedding-plane slip during the folding of a succession of rocks of varying competency. It is thought that shearing, resulting from bedding-plane slip, affected the least competent beds in the succession.
Shear-planes are interpreted as fracture cleavage and the small folds as congruous drag-folds.
Similar beds of contorted shale occur at some of the same horizona on the borders of the North Staffordshire Coalfield and in Lancashire.
The Relation of the Main Peneplain of Central Africa to Sediments of Lower Miocene Age
Authors: Dixey Frank 
Published: October 2009

Summary
Observers of the Lower Miocene beds of kavirondo Gulf, kenya, and of the western side of Lake Rudolf, Have come to the conclusion that these beds have been faulted below the level of the adjacent main peneplain, usually referred to as the “Miocene” peneplain, and that the age of this peneplain must therefore be pre-Lower Miocene. In this paper different interpretation is advanced, namely; that the peneplain was eroded across the sediments as they now stand, and that these have been revealed by the erosion of the Pliocene cycle at a lower level; the date of termination of the main peneplain would thus fall within the later Miocene, assuming the whole of the Pliocene was required for the erosion of the Pliocene cycle. This view is based on a brief survey of the geomorphology of the region, with special reference to the erosion surfaces and the limiting escarpments, certain of which are regarded as essentially erosion surfaces and the limiting escarpments, certain of which are regarded as essentially erosion-scarps and not as fault-scarps postdating the main peneplain. In East Africa there are remnants of a number of erosion surfaces at various levels, hidden to a greater or less extent beneath a cover of volcanic rocks, and it is suggested that failure to recognize the significance of the “pre-Rift” topography has sometimes led to misconceptions of the extent and nature of the rifting.
The Harlech Dome, north of the Barmouth Estuary
Authors: Matley Charles Alfred , Wilson Theodore Stacey 
Published: October 2009

Summary
The area described, 150 square miles in extent, lies between the Barmouth estuary and the Vale of Ffestiniog and contains some 10,000 feet of Cambrian rocks which range from ?Lower Cambrian to Ffestiniog Flags and include thick formations of grit. The igneous rocks are all intrusive, are of Lower Palaeozoic age (though of more than one date), and are nearly always found in an altered condition; they are " greenstones " of either dioritic or basic composition. Quartz veins and metalliferous lodes are common. The sediments, the materials of which are chiefly derived from an easterly extension of the Mona Complex of Anglesey and south-western Caernarvonshire, have undergone low-grade metamorphism; some beds (especially the Manganese Ore Bed) are rich in authigenic spessartite.
The general structure is a broken anticlinorium which has been compressed from west to east. The cleavage is predominantly northerly. Faults are numerous, the latest being an important north-and-south series with displacements up to about 4000 feet.
The Great Glen Fault
Authors: Kennedy William Quarrier 
Published: October 2009

Summary
The powerful dislocation which intersects Scotland along the line of the Great Glen has, in the past, been regarded by most geologists as a normal or dip-slip fault with a predominant vertical downthrow to the south-east. A reconsideration of the entire problem now suggests that this view is no longer tenable and that the dislocation is, in reality, a lateral-slip or wrench fault with a horizontal displacement of approximately 65 miles. Such an interpretation is supported by several independent lines of evidence, as follows :—
(1)	The dislocation possesses physical characters unlike those of most normal faults but similar to the great strike-slip shears of the California Coast Range.
(2)	It belongs to the same system as the Strathconon, Ericht-Laidon and Loch Tay faults, all of which have proved lateral displacements of up to 5 miles.
(3)	It displaces the great belt of regional injection which affects the Moine Schists of the northern and Grampian Highlands, the nature and amount of the displacement being consistent with lateral shift but not with vertical downthrow.
(4)	It similarly displaces the metamorphic zones of the Highlands in an equally significant manner.
(5)	It truncates the Strontian Granite, the southern portion of which, according to the detailed structural evidence, is missing. The missing portion, moreover, can be identified in the Foyers mass which outcrops on the other side of the fault-line some 65 miles to the north-east and is similarly truncated by the fault. These two major Caledonian intrusions consist of identical rock types and are structurally homologous.
(6)	Finally, the occurrence of Lewisian and Torridonian rocks in Islay and Colonsay and the presence of the Moine Thrust-plane in the former island are more readily explained on the assumption of a lateral rather than a vertical displacement along the fault.
Although the dislocation is still active, the available evidence indicates that the main lateral movement was accomplished prior to the deposition of the Upper Carboniferous sediments of Lochaline and subsequent to the intrusion of the Strontian and Foyers (Lower Old Red Sandstone) granites. Middle Old Red Sandstone strata along the Great Glen have, moreover, suffered intense crushing and deformation during the faulting, which must, therefore, be referred partly if not wholly to a post-Middle Old Red Sandstone epoch. The sinistral nature of the displacement, i.e. towards the south-west on the northwest side of the fracture and towards the north-east on its south-east side, implies the operation of a stress system involving regional compression acting in a general north-and-south direction accompanied by an east-and-west relief of pressure. This is regarded as evidence of the fact that the Hercynian forces, to which the formation of the Great Glen Fault is ascribed, were already in operation during Upper Old Red Sandstone or Lower Carboniferous times.
The complex intrusion of Welfield, near Builth Wells, Radnorshire
Authors: Jones Owen Thomas , Pugh William John 
Published: October 2009

Summary
The paper deals with an area of dolerites intrusive into Llandeilo Shales and forming a prominent ridge near Welfield, north-west of Builth. The area has been mapped on the scale of 25 inches to the mile and an analysis of the relations between the dolerites and the associated strata, usually strongly baked near the contacts, leads to the conclusion that the ridge is occupied by a core of dolerite having the habit of an elongated .laccolith. The inferred main body is accompanied by many lenticles of dolerite on the flanks of the structure and also sheets which appear to spring off from two dyke feeders near the crest of the laccolith.
The whole area has been tilted to the north-west in post-Silurian times. The height of the laccolith is inferred to have been about 500 feet and its width about 1500 feet, and it was intruded under a cover of Ordovician and possibly early Llandovery sediments estimated to be at least 4500 feet thick.
The geological structure of East Poland and West Russia: A summary of recent discoveries
Authors: Sujkowski Zbigniew 
Published: October 2009

Summary
Recent investigations have yielded the following results.
The extensive Ukrainian granitic massif has been traced some 30 miles farther north beneath the Pripet Marshes, and the primary Archaean massif must have been at least twice as large las the present one. The Donetz Basin, instead of being relatively small and enclosed, proves to be part of a great trough extending northwestwards for at least 1000 miles to the Pripet Marshes. In the middle of this North Ukrainian trough several Permian salt domes have been detected.
The Lower Palaeozoic in Podolia and Volhynia differs in some respects from that of the Baltic countries. The Devonian is more uniform in the two regions. As the younger Palaeozoic rests directly on the granite, the impression is given of two Lower Palaeozoic provinces separated by an Archaean belt.
Three new Carboniferous deposits have been discovered; one of Moscow facies with coal in Polesia (under the Pripet Marshes), one in Volhynia with coal near to anthracite and one in Lithuania without coal measures. The last-mentioned would appear to be a prolongation of the Danzig-Lwow trough.
Of later connexions between the Russian and the West European basins that pass more or less through Poland, probably none existed in the Triassic period. The Upper Cretaceous seas were very extensively connected in Cenomanian times; the connexion was narrower in the Turonian and apparently absent in Senonian time. In the Oligocene it followed approximately the same line as in the Cretaceous, with a slight displacement to the south. The youngest connexion, in the Upper Miocene, is much farther south.
The relation between East and West Europe is much more complicated than has been supposed and Tornquist's hypothetical line does not, in fact, exist. The big syncline passing from Danzig to Lwow is related only to the West European structure although situated east of the hypothetical line. The Lithuanian basin appears to be a side branch of that trough; here the western structure passes slowly into the Russian type. The extensive North Ukrainian basin perhaps marks more completely the line of separation between the two main parts of Europe.
Notes on Cambro-Ordovician fossils collected by the Oxford University Ellesmere Land Expedition 1934-5
Authors: Poulsen Christian 
Published: October 2009

Summary
To a description of the fossils collected by Mr. Bentham on the Oxford University expedition to Ellesmere Land, the author has added a re-determination and description of some fossils from the same area collected in 1898-9 by Per Schei on the second Norwegian Arctic Expedition in the Fram. All these specimens, mainly brachiopods and trilobites, are from Cambrian and Lower Ordovician sediments exposed along the western side of Kane Basin from Bache Peninsula (latitude 79° N.) to Scoresby Bay (latitude 80° N.).
Lower and Middle Cambrian rocks rest upon a peneplaned Archaean surface on the south shore of Bache Peninsula, and Middle Cambrian rocks are represented in Per Schei's collection from a locality at the south-east tip of the peninsula. Collections from the remaining seven of Mr. Bentham's localities, and other of Per Schei's specimens, indicate rocks of Lower Ordovician age. The sequence for North-West Greenland as developed on the opposite side of Kane Basin (in Washington Land and Inglefield Land) is more completely known and includes formations not yet recognized in Ellesmere Land and Grinnefi Land, and the lowest Cambrian horizon of Ellesmere Land (Bache Peninsula) has not yet been found in Greenland; but the two columns correspond perfectly in most respects.
In the palaeontological section, descriptions are given of four new genera and 10 new species of trilobites, and of two new brachiopod species.
The thanks of the Society were unanimously voted to Prof. A. E. True-man, retiring from the office of Vice-President and from the Council; to Mr. W. N. Edwards, retiring from the office of Secretary; and to Dr. L. R. Cox, Prof. H. P. Lewis, Dr. F. J. North and Dr. J. Phemister, retiring from the Council.
The textural features of the granites and invaded rocks of the Singo batholith of Uganda and their petrogenetic significance
Authors: King Basil Chables 
Published: October 2009

Summary
The batholith invades quartzites, sandstones, sandy shales and shales of the Karagwe-Ankolean System, which were sharply folded before the emplacement of the granite. The structures show that the invaded rocks were not swept aside, but that areas formerly occupied by country rocks are now occupied by granite.
The granite is remarkably uniform in character over the greater part of the batholith and is principally a pink or reddish, coarse-grained, porphyritic rock, with large felspar phenocrysts. A finer- and more even-grained marginal variety is often found.
The Karagwe-Ankolean sediments, in addition to showing increasing metamorphism of regional type towards the southern part of the area, are also contact-metamorphosed by the granite. Progressive recrystallization of original clastic grains of quartz to form a quartz mosaic, and reconstitution of other constituents into sericite and muscovite, are traceable.
Certain of the marginal “granites” contain sericite in place of felspar and are only distinguishable from contact-altered sediments by the absence of bedding. The sericite always exhibits replacement relations towards the quartz and is believed, in part at least, to represent an intermediate stage in the development of felspar.
Even in the coarse-grained granites, quartz was always the earliest mineral to form and was replaced successively by two generations of potash felspar as well as by oligoclase. The various felspars also show mutual replacement relations, while the phenocrysts of perthite were formed at a late stage in the development of the granite.
It is believed that the granite never existed wholly as a magma or melt, but that it evolved by a series of replacements, effected by differential fixation in time and place of a succession of introductions from below and of materials displaced within the body itself.
The sequence of geochemical changes leading to granitization
Authors: Reynolds Dorris L. 
Published: October 2009

If we agree that in science the emphasis is placed on the interpretation of facts, then it is obvious that Dr. D. L. Reynolds's paper will eventually occupy a very important place in the history of petrogenetic ideas. The value of this work is twofold. On the one hand, Dr. Reynolds “tolls the knell ”of the passing theory of “magmatism ” as an all-embracing explanation of the origin of all plutonic rocks, and, on the other hand, she provides a new and most powerful support to “ transformism ” as applied to the processes of granitization. It is important to remember, however, that “ transformism ” in relation to the origin of granite is well over a hnndred years old, whilst “ magmatism ”, which was first developed by Iddings, Rosenbusch, BrSgger and Vogt in the nineties of the last century, is barely sixty years old. Thus “ transformism ” is not a revolutionary innovation, but is rather a restoration of an old and more balanced opinion which has been known to petrogenesis since the time of Ami Bout. Present-day petrologists, nurtured on pure magmatism, are usually oblivious of the saying of James Hutton that people often “ judge of the great operations of the mineral kingdom, from having kindled a fire, and looked into the bottom of a little crucible ”
“ Transformism ” does not deny the existence of magma or migma, hob-ever, but it does restrict its field and function. “ Transformism ” postulates a wide cycle
A Revision of the Genus
Pentamerus
James Sowerby 1813 and a Description of the New Species
Gypidula Bravonium
from the Aymestry Limestone of the Main Outcrop
Authors: Alexander Frances Elizabeth Somerville 
Published: October 2009

Summary

The history of the genera
Pentamerus
and
Conchidium
is reviewed, and the conclusions reached that, according to the International Rules of Zoological Nomenclature, the generic name
Conchidium
is inadmissible,
Pentamerus
should be applied to forms congeneric with
P. knightii
J. Sowerby, and a new generic name is required for brachiopods congeneric with
P. oblongus
J. de C. Sowerby. In order to avoid the confusion which would follow this strict observance of the rules, the International Commission on Zoological Nomenclature has been asked to suspend the
Régles internationales
in this case. The genera
Pentamerus
(type
P. oblongus
J. de C. Sowerby 1839) and
Conchidium
(type
C. bilocularis
[Hisinger 1799]) are re-defined by the author in accordance with her application.

A new species,
Gypidula bravonium
from the Aymestry Limestone, is described and figured.

This paper is a revision of a paper read before the Geological Society of London and published in abstract in July, 1936 (Alexander 1936). Publication in full was unavoidably delayed, and in 1938 Dr. St. Joseph (1938, pp. 256–65) published a history of the genera
Conchidium
Linnaeus auctt. and
Pentamerus
J. Sowerby auctt. Though I agree with Dr. St. Joseph's conclusions in general, I differ from him in details of interpretation and I consider it worth while restating the case. The question of the nomenclature of this group of brachiopods has been referred to the International Committee of Zoological Nomenclature but it is not expected that an opinion will be obtained for some time.
The geology of the eastern part of the English Channel
Authors: King William Bernard Robinson 
Published: October 2009

The paper is an attempt to bring together the existing information about the geology and structure of south-eastern England and north-western France, together with the few fragments of information concerning the rocks forming the floor of the eastern part of the English Channel.
The fold pattern on the two sides of the Channel is discussed and the evidence for a continuance of the echelon arrangement of the folds is emphasized. By plotting the axes on a map and taking the outcrops at 100 feet below sea-level on the land areas, together with the few records from soundings for the sea areas, a map has been constructed showing the probable outcrops on the floor of the Channel.
The most interesting and probably most controversial point is the presumed presence of a large outcrop of Triassic rocks in mid-Channel south of the Isle of Wight. Much of the evidence for this has been obtained from Admiralty sources.

This
paper is an attempt to bring together and to interpret the present information regarding the geology of the eastern part of the English Channel.

On most maps the geological boundaries of the English side end at the coast, and the same may be said of the French side., Dangeard's work (1929), however, gives some important information regarding the age of the solid rocks forming the floor of the Channel. His samples were obtained by dredging. Admiralty charts are also informative, and the Hydrographer has been most helpful in attempting to obtain some confirmatory samples.
The problem of mantled gneiss domes
Authors: Eskola Pentti Eelis 
Published: October 2009

In many orogenic zones there occur domes having a superincumbent mantle of sedimentary strata layered parallel to the dome contacts and the foliation of the gneiss. In the Karelidic zone of East Finland are numerous domes showing somewhat different development. In some, the lowest horizon of the mantle consists of basal conglomerate with boulders of the same gneiss that forms the dome; in others, the basement stratum is a layer of quartzite, above which follow dolomite and micaschist; and in still others, dolomite forms the basement. Ivariably the domes are more or less inclined according to the general tilt of the orogenic zone. In some domes the gneiss, or rather granite, has apparently been preserved as it was when the sediments were deposited upon the croded surface of the plutonic mass. In most cases, however, it has become migmatized and granitized during the doming, and now shows a veined structure and has a potash-rich ideal-granitic composition, although its original composition may have been granodioritic or quartz-dioritic. In some cases massive granites break through the domes, and at the contacts the palingenic gneissose granite may display an intrusive relation to the mantle rocks. On this account certain domes were formerly thought to be younger intrusions.
Migmitized domes of exactly the same character as the Finnish examples, and likewise mantled with sediments, occur in Maryland and elsewhere within the Appalachian range of North America. Very similar also are the Variscan gneiss masses in the Alps, such as the St. Gotthard, Aar, and Mont Blanc massifs. Other Alpine mantled domes have been deformed and drawn out into extensive nappes, as is illustrated by the Simplon Tunnel profile.
The manteld domes apparently represent earlier granite intrusions related to a orogenic period. The plutonic mass was later eroded and levelled, and thereafter followed a period of sedimentation. During a subsequent orogenic cycle the pluton was mobilized anew and new granite magma was injected into the plutonic rock at the same time as it was deformed into gneiss, causing its migmatization and granitization, or palingenesis.
It seems that a neccessary condition foth the formation of mantled domes is that the area in which they occur should have been subjected to two orogenic revolutions: in Finland the Svecofennidie and Karelidie, in eastern North America the late Pre-Cambrian (or ? Taconic)and the Appalachian, in the Alps the Variscan and the Alpidie. The repeated upheaval of such rather small plutons, a few tens of kilometres in maximum diameter, is a remarkable fact that throws light upon the nature of orogeny, as well as on the genesis of granites, and invites interesting speculations upon the original source of the granitic material.