bluuebunny/crossref_metadata_2025_split huggingface dataset:
The Start-Dodman-Lizard Boundary-Zone in Relation to the Alpine Structure of Cornwall
Authors: Hendriks E. M. Lind 
Published: May 2009

Previous opinion sums up in favour of the continuity of the three boundaries, the entire line being one of dislocation in the east, dislocation and intrusion in the west. Previous opinion also favours the view that, inside the boundary-zone, not only are the Start-Lizard schists continuous, but they have features comparable with some of the Alpine “Schistes lustrés”, with recumbent folding at the Lizard.The boundary-zone is defined as a belt of variolite (ophiolite), exotic blocks, and serpentine intrusive in, and contemporaneous with, a great thrust.Recent work by the writer has shown that some of the beds outside the boundary-zone are a “facies flysch”. Younger beds come in towards the west, in association with the westerly pitch visible in the older beds in South Devonshire; geanticlines occur in the Lower and Middle Devonian respectively, of South Devon and South Cornwall. In an area further north some of the beds show an accumulation of folds comparable with those of the “autochthonous sedimentary” in front of some of the great Alpine nappes; recumbent folding is prevalent in both Devon and Cornwall. The Cornish Flysch was deposited under conditions such as might have preceded a great nappe movement; it is described in relation to the exotic blocks and serpentine in the fracture.The much younger Alpine Flysch also includes ophiolites and exotic blocks, with serpentine intrusive in the fractures upon which the great nappes advanced. According to some authors, the nappes arose from recumbent folds based on geanticlines.The similar direction of both the Cornish (Variscan) and the Alpine movements makes possible a comparison in certain effects as, for instance, the southward increase in albitization and metamorphism, between the great Alps and the similar but older, comparatively tiny, flattened, and denuded relic in south-west England.These cases are also strikingly paralleled by a zone of basic igneous rocks and exotic blocks which overlies the Himalayas.The evidence appears sufficient basis for the suggestion that the Start-Dodman-Lizard boundary-zone may be the relic of a great Variscan nappe, associated with the fan-structure of Cornwall.
Crozzle and Hussle
Authors: Cope F. Wolverson 
Published: May 2009

AbstractDescription of an intraformational contorted shale in the Middle Coal Measures of the Potteries Coalfield. The contorted bed occurs immediately below the Winpenny Coal in thin argillaceous measures between thick sandstones. It shows strongly slickensided contacts, and consists of black carbonaceous shale, folded, sheared, and burnished. Deformation is ascribed to shearing stresses operating during folding. This shale is called “hussle” by the miners, whilst a similarly contorted, but non-carbonaceous, shale was termed “crozzle” by old miners of the Staffordshire-Derbyshire moors.
Lineation in Moinian and Lewisian Rocks of the Northern Highlands of Scotland
Authors: Phillips F. C. 
Published: May 2009

AbstractIt has recently been reaffirmed, on the basis of evidence derived from published maps, that in the Moine schists the south-easterly plunging lineation appears to increase in intensity as the Moine thrust area is approached. This statement is not in accordance with facts observable in the field and is a false premise on which to base the conclusion that thrusting and lineation are related. A further fact of vital significance in relation to such a conclusion is the widespread development of a similar lineation, plunging south-easterly and likewise expressive of a girdle fabric, in unmoved Lewisian rocks of the foreland.
A Restudy of the Ingletonian Series of Yorkshire
Authors: Leedal G. P. , Walker G. P. L. 
Published: May 2009

AbstractA description of the Ingletonian Series is given, with special reference to the sedimentary structures which occur and their use in determining the nature of the folding of the beds; this is shown to be isoclinal. The age of the series is discussed, and it is considered to be in all probability Pre-Cambrian.
The Chalky Boulder Clays of Norfolk and Suffolk
Authors: Baden-Powell D. F. W. 
Published: May 2009

In the past there have been two main lines of approach to the glacial problems of East Anglia:—(1) Attempts to find out the number of. glacial and interglacial deposits; and(2) The direction or directions of ice-movement as shown by the constituent materials.A fresh investigation of the boulder clays has been undertaken, combining as far as possible these two points of view, with special attention (so far) to the varieties of “Chalky Boulder Clay” (see Baden-Powell, 1948, pp. 287–8).
Note on the Sandstone Injections of Eathie Haven, Cromarty
Authors: Waterston Charles D. 
Published: May 2009

AbstractThe sandstone injections which penetrate the Kimmeridgian strata of Eathie are described, the presence of sill-like injections being particularly noted. It is considered that the occurrence of “sandstone-sills” at Eathie is of importance in ascertaining the mode of origin of the injections of the locality. It is further suggested that the sills support the hypothesis that the injections are the result of infilling of fissures from below by sand and water.
Darwin and the forgotten Mr. Lonsdale
Authors: Tasch Paul 
Published: May 2009

AbstractWilliam Lonsdale's associations with Sedgwick, Murchison. and Darwin are noted and his inference that the “transition series” was Devonian age, derived in 1837 from a study of fossil corals, is interpreted as an unique contribution to the belief that “species undergo modification”. As the first applied evolutionist, it is argued that he belongs on the list of important early contributors to the theory of evolution.
Sandy Gypsum Crystals from Berbera, British Somaliland
Authors: Macfadyen W. A. 
Published: May 2009

AbstractGypsum crystals containing 62 per cent by volume of sand are described from a late Raised Beach, where they were found by digging shallow coastal wells. An account is given of their crystallographic form and of the circumstances in which they have been produced. Gypsum has not only been deposited in the voids of the sand but has even moved the individual grains apart. A review is given of earlier records of sandy gypsum crystals, sometimes called “desert roses”, and comparison is made.
The Hinge of certain Non-Marine Lamellibranchs from the Lenisulcata Zone of the Coal Measures
Authors: Eagar R. M. C. 
Published: May 2009

(1) The Carbonicola fallax group of shells, which characterize the Lenisulcata Zone of the Coal Measures, is an extremely variable one comprising a wide range of forms, between which there appears to be perfect gradation.(2) The hinge of the group is also a highly variable feature, bearing little relation to the outline of the shells. Its variation, however, is more fully known in small forms than in large ones.(3) Evidence submitted in the present paper indicates that, although the hinge pattern of the C. aquilina group may not be as constant a feature as has hitherto been supposed, the group is distinct from that of C. fallax. There is no evidence suggesting genetic relationship. A basis for the distinction between internal moulds of C. aquilina and C. fallax is fully described.(4) The basic features of the hinge of the C. fallax group are essentially those which characterize the Carbonicola pseudorobusta–C. communis group of the Ovalis Zone. While certain of the hinges of the larger shells appear typical of the latter group there are a number of other patterns which have not previously been described in the Carbonicolidae.(5) The hinge features of the C. fallax group appear less specialized than those of shells from the Ovalis Zone, especially Carbonicola pseudorobusta Trueman (MacLennan, 1944).(a) Large strong teeth have not been seen. Definite small teeth are not commonly developed. It is usual to find gentle swellings on the hinge plate corresponding to depressions in the opposing valve. Some forms are quite edentulous.(b) Only one tooth has been found in either valve, although more than one swelling or depression may be present. There is no approach to the more complicated patterns figured by MacLennan (1944).(c) In most cases engagement of the dental apparatus would only take place as the valves opened. Notches or sockets in the hinge plate are not necessarily opposed by teeth or swellings, but they would have been more or less filled as the opening continued, when the hinge plates apparently rolled against one another.(d) In a community of small shells there is evidence to suggest that in several cases the hinge margin of the left valve slightly overlapped that of the right for a short distance anterior to the umbo.(6) The range of variation of hinge characters in a community is very large. Collections from different horizons, however, may indicate individual peculiarities or tendencies in the variation. Whether these owe their origin to local conditions or evolution is not yet clear.(7) The hinge of Anthracomya from the Lenisulcata Zone is as yet little known. What evidence there is points to a hinge similar to that of small Carbonicola showing the same type of variation.
Some Grits and Associated Rocks in the Etruria Marls of North Staffordshire
Authors: Williamson W. O. 
Published: May 2009

The grits and conglomerates in the Etruria Marls of North Staffordshire include types with a chamosite-rhombohedral carbonate cement containing interesting spherulitic and concentric structures. Manganese appears in this cement and in certain calcareous bands in the argillaceous fades of the Marls. The clastic fragments suggest derivation from Pre-Cambrian and Cambrian rocks. The heavy mineral suite resembles that listed by Fleet for similar horizons in the Midlands, but staurolite is recorded also.There is no new evidence bearing on Robertson’s hypothesis that basic igneous rocks of Carboniferous age have contributed to the formation of the Etruria Marls.
Subterranean Penetration by a Desert Climate
Authors: Bailey E. B. 
Published: May 2009

The subject matter of the present note is furnished by the abnormal redness of many parts of the Arran Carboniferous. W. Gunn, in his invaluable memoir, records this colouration without particular comment; but, as Scottish geologists are aware, B. N. Peach, under whose supervision Gunn carried out his survey, has long claimed that the Arran Carboniferous is stained by solutions that have percolated down from overlying New Red Sandstone. After a careful consideration of the exposures, I feel convinced that two features of Peach's proposition are secure:—(1) The red colour of much of the Arran Carboniferous is not original.(2) It must be in some way connected with the New Red Sandstone.
Submarine Erosion off the Holderness Coast.
Authors: Thompson C. 
Published: May 2009

Summary1. Submarine erosion off Holderness is a fact, as pointed out by Winn.2. The rate is greatest between H. and L.W.M.'s.3. Between L.W. and 20 feet it is much less rapid.4. Below 20 feet it still further diminishes to the 30-ft. line; outside which it apparently dies away.5. Groynes—taking the long view—are unfortunately only a temporary safeguard for this district of easily eroded clay.The writer's sincere thanks are due to Mr. G. W. Lamplugh, F.R.S., for his very kind and keen interest in the work.
The Base of the Devonian, with special reference to the Welsh Borderland
Authors: Stamp L. Dudley 
Published: May 2009

The main thesis of this paper is to show that the Ludlow Bone-bed forms the true base of the Devonian System. This is urged on several grounds.(a) Priority. It was the limit originally used by Murchison. Although subsequently altered by him, one finds if one attempts to use his later limit:—(i) That the Old Red Sandstone was not re-defined accordingly.(ii) That Dumont's Rhénan (Devonian) System, defined in 1845, has priority over Murchison's later definition (1848).(iii) That the later limit adopted by Murchison does not form a true horizon and has been very differently interpreted by later writers.(b) Palæontology.(i) There is a marked faunal change at the Ludlow Bone-bed. The Bone-bed marks the first appearance of fossil fishes, and thus the Devonian marks the dawn of an age of vertebrates. There is only one old record of a pre-Devonian fish in the British Isles; one doubtful one in Gotland, and an anomalous one in the Ordovician of America. The Shropshire succession forms a standard of comparison for all areas of the Old Red Sandstone type of deposit.(ii) The limit adopted after a detailed study by other writers of an uninterrupted marine series is on the same horizon. The succession at Liévin (Northern France) forms a standard for comparison of all areas of the Devonian (marine) type of deposit.(c) Stratigraphical. In England the Ludlow Bone-bed marks also a change in physical conditions, more noticeable elsewhere as an unconformity. Physical breaks or unconformities on the same horizon occur in Scotland, Belgium, Brittany (slight), Norway, Sweden, and Spitsbergen.(d) Practical Considerations. The Downtonian rocks, i.e. the strata from the Ludlow Bone-bed horizon upwards, form a stratigraphical and palæontological entity, incapable of broad or even of rough separation below the Dittonian. The Ludlow Bone-bed, on the other hand, forms an horizon which can be recognized and mapped all over North-Western Europe. In England there appears to be a slight faunal break between the Downtonian and Dittonian, but this is less marked elsewhere.
The Connemara Serpentine Rocks
Authors: Cronshaw H. B. 
Published: May 2009

The serpentine rocks belonging to the metamorphic region of Connemara, West of Ireland, fall into two classes, the ophicalcites and the serpentinized basic igneous rocks.The existence of exceptionally beautiful pale green and yellow serpentine and variegated ophicalcites is well known. At one time these deposits were quarried at several points, notably at the Lissoughter Quarry near Recess, the Derryclare Quarry on the eastern shores of Derryclare Lough, the Barnaoran Quarry near the head of the Owenglin River which flows into Clifden Bay, and at the Streamstown Quarry situated at the head of Streamstown Bay. There are, however, a number of other localities scattered through the region where small occurrences of ophicalcites and serpentinized igneous rocks are to be found.
The Zonal Position of the Elsworth Rock and its Alleged Equivalent at Upware
Authors: Arkell W. J. 
Published: May 2009

(1) The Elsworth Rock of Elsworth and St. Ives is a condensed deposit belonging to the plicatilis zone.(2) There is no evidence that it contains any ammonites derived from earlier zones. Statements that it does are based on misidentifications.(3) The Elsworth Rock at Elsworth overlies at least 8½ feet of ironshot clays with thin bands and nodules of limestone, the clays containing abundant ammonites of the cordatus zone and no others.(4) The so-called Elsworth Rock at Upware is the equivalent of the ironshot cordatus zone developed below the Elsworth Rock at Elsworth.(5) The true Elsworth Rock (plicatilis zone) is represented at Upware by the Coralline Oolite and Lower Coral Rag.(6) For convenience in stratigraphical nomenclature it is desirable to group together the condensed ironshot cordatus and plicatilis beds of Elsworth as the Elsworth Series.(7) The Elsworth Series, as defined in 6, corresponds with the Oolithe ferrugineuse and the greater part of the Oolithe de Trouville on the Normandy coast. At Trouville the plicatilis zone to some extent combines the developments at Elsworth and Upware.(8) The ironshot cordatus zone was proved in the Upware well to rest directly upon normal clays of the mariae zone, and the same zone was proved in the vale below Elsworth in the Fen Stanton brewery boring.I am greatly indebted to Mr. E. E. L. Dixon and Mr. A. G. Brighton for criticisms and suggestions, and especially to Mr. Brighton for the trouble he has taken in sending me all the fossils on loan and supplying the relevant information.
The Floor of the Arabian Sea
Authors: Wiseman John D. H. , Sewell R. B. Seymour 
Published: May 2009

During the course of the John Murray Expedition some 22,000 miles of the floor of the Arabian Sea and the neighbouring areas of the Indian Ocean were mapped by means of the Echosounding apparatus. The region between India and Africa was crossed four times, namely:(i) from Aden to Karachi,(ii) from Bombay to Mombasa,(iii) from Zanzibar to Colombo, and(iv) from Colombo to Aden,while more detailed surveys were carried out in the Gulf of Aden, the Gulf of Oman, and the region off Zanzibar.
A Xenolithic Pegmatite in the Dalbeattie “Granite”
Authors: MacGregor Malcolm 
Published: May 2009

SUMMARY AND CONCLUSIONA pegmatite cutting granodiorite contains abundant xenoliths which are in various stages of assimilation. Assimilation involved the conversion by the process of “reciprocal reaction” of the minerals of the xenoliths into species which were in equilibrium under the prevailing magmatic conditions, and the subsequent “mechanical disintegration” of the xenoliths with the strewing of their minerals in the pegmatite. Solution of xenolithic material was not important, probably only affecting potash-felspar. The fact that the active magma was a pegmatite suggests that high temperatures were not available, and its assimilating power must be attributed to its large volatile content. The xenoliths were probably derived from the walls of the pegmatite vein both in the granodiorite and in the country-rocks.
New Light on Sedimentation and Tectonics
Authors: Bailey E. B. 
Published: May 2009

1. The Loch Awe Nappe succession was correctly stated in 1922.2. The Iltay Nappe succession was correctly stated in 1922.3. The Ballappel Foundation succession was wrongly stated in 1922.4. The recumbent-fold structure of the Ballachulish district is due to rotation of middle limbs by drag from above or from below.5. Graded bedding is as important as current bedding in marking a facies group among sandstones. It often indicates accumulation in rather deep water, to which sandy material has penetrated, perhaps as a result of seaquakes.
Intra-Jurassic Movements and the Underground Structure of the Southern Midlands
Authors: Cox Arthur Hubert , Trueman Arthur E. 
Published: May 2009

Summary1. The occurrence of anticlinal folding during Jurassic times has been demonstrated by Mr. Buckman's detailed zonal work in the Vale of Moreton and in the North Cotteswolds. These anticlines are indicated on the map by marked bends in the outcrops of the Lower Jurassic formations.2. Similar bendings of outcrops are seen at several localities in the Eastern and Southern Midlands, and the structure at one such locality—Melton Mowbray—has recently proved to be anticlinal.3. Intra-Jurassic folding betrays itself by non-sequences and reduced thicknesses of Lower Jurassic zones along anticlinal axes. Such evidence suggests the existence of anticlinal structures in the neighbourhood of Banbury, Weedon, and perhaps also Market Harborough, in addition to the cases mentioned above.4. Movement was probably almost continuous along some or all of these axes, at least from Rhætic to Bajocian times. Outcrops of post-Bathonian formations are not affected by the flexures, although the folding was perhaps renewed in later Jurassic or even Tertiary times.5. Several of these lines of Jurassic folding probably follow the lines of earlier and more powerful movements. The bearing of such flexures on the structure of the Palæozoic floor is discussed.6. Attention is called to a curious symmetry in the disposition of the Palæozoic formations on either side of a prolongation of the Pennine axis.
The Heavy Minerals of the Plutonic Rocks of the Channel Islands: 2. Guernsey, Sark, and Alderney
Authors: Groves A. W. 
Published: May 2009

Summary of ResultsThe method attempted of correlation of plutonic masses by their accessory minerals is successful, and particularly so with the acid rocks. The results effected in the Channel Islands are as follows:—1. Confirmation of the existence of granites of two ages in Jersey, and correlation of the Fort Regent and Gorey masses for the first time.2. Correlation of the Cobo Granite of Guernsey with the “Older” Granite of Jersey (Gorey and Fort Regent).3. Conclusive evidence to show that the Cobo Granite is the last stage of the Differentiation Series of North Guernsey, previously thought improbable.4. The probable occurrence of both “Newer” and “Older” Granites in Alderney, making a Pre-Cambrian age for the “Newer” Granite highly probable.5. The dissimilarity of the heavy residue of the “Newer” Granite to that of the Dartmoor Granite.6. The similarity of the residue of the “Older” Granite with that of the Granite Gneiss of the Lizard and their suggested correlation.7. The individuality of the gneisses of South Guernsey.8. The occurrence in hybrid rocks of the mineral suites (particularly the zircons) of both rocks involved, consequently we have here a new method of demonstrating the hybrid nature of a rock.Many rocks previously termed diorites in Jersey, Guernsey, and Alderney are shown petrographically not to be true diorites, some being gabbros, others hybrids.The occurrence of acid-soused basic rocks in Jersey, Guernsey, and Alderney is pointed out, and their petrography described.The occurrence of amphibolites in Roselle Bay, Alderney, is made known for the first time, and their petrography described.In the course of the whole work sixty-three rock specimens have been crushed and passed through bromoform according to the method of procedure previously outlined, making an aggregate of about 15 lb. of rock crushed. From this crushed rock nearly four hundred slides of grains have been prepared, and of these about 90 per cent are nonmagnetic. In addition eighteen thin sections have been prepared.I wish to thank Mr. A. E. Mourant, B.A., for some of the specimens of gneisses from southern Guernsey, and also Dr. G. H. Plymen for the specimens from Alderney. The rest of the material. was collected by myself.
The Chief Heavy Detrital Minerals in the Rocks of the English Midlands
Authors: Fleet W. F. 
Published: May 2009

SummaryThe chief features exhibited by the heavy mineral residues from the various formations will now be summarized, but it is difficult to show, by tabulating or otherwise, the differences or resemblances between residues, although such may be quite obvious to the investigator. This is because the differences consist of a sum total of variations in size, shape, colour, and frequency of the mineralscontained in the residues under examination, and it is scarcely possible to indicate such differences in writing, without frequent repetition of words, there by involving a loss in clarity of expression, or if tables be employed, without losing sight of other connected data.