bluuebunny/crossref_metadata_2025_split huggingface dataset:
Till on Overthrust Gravels
Authors: Lane Alfred C. 
Published: May 2009

The Plate which accompanies this article, showing till over-riding and overthrusting in its readvance the gravels on which the yard of Harvard University is built, is of a temporary exposure. This was made in putting in a large apartment house at the north-west corner of Arlington Street and Massachusetts Avenue, North Cambridge. The camera was pointed north. Realizing its ususal character, I got my colleague, Prefessor M. S. Munro, who is a virtuoso with the camera, to take it, and have used it as a postcard to friends. One of them, my old teacher, William Morris Davis, said it was unexcelled, and urged its publication. That is the occasion of this article, for, when I came to think of it, to obtain such a photograph required an unusual combination of circumstances:—(1) The artificial excavation;(2) A strike that suspended work at the critical time (it is an ill wind that blows no one good);(3) Just such conditions of wind and drying out as to bring out the different beds in the sands. The coarser ones dry and crumble more rapidly, while the fine hold the dampness and stand out. We might add:—(4) A man living on the street (myself) to appreciate it, and(5) A friend who is an excellent photographer.
A System of Joints on the Surface of Basalt Columns at the Giants Causeway
Authors: Rohleder Herbert P. T. 
Published: May 2009

When studying the geology of the Giants Causeway district in 1924 I noticed a strange system of well-developed joints on the surface of some basalt columns. As these only appeared on the planes of a few columns in this district, where several hundred thousand basalt columns are exposed, and as these joints were only to be found on and quite close to the surface, I firstly regarded them as a mere feature of weathering. It was only after Professor Dr. Maximilian Weber in Munich pointed out to me the striking resemblance of these joints to the photos published in Daubrée's Études synthétiques de Géologie Experimentale, and I decided to investigate this problem closer, the results of which are given as follows:–This system of joints is only to be found at one locality in the Giants Causeway district, i.e. the lower parts (sea level) of the “Grand Causeway” (west side) opposite the “wishing chair” (the spot is marked with a white X on Fig. 1, Pl. XIV).
I.—The Gulf of Suez
Authors: Ball John 
Published: May 2009

In a previous paper published in this Magazine, I gave reasons for the belief that neither the Gulf of Suez nor the valley of the Nile owes its origin to trough-faulting, as was at that time generally supposed. The skeleton of the argument was as follows:—1. Extensive faulting at the faces of the scarps of the Nile Valley and Gulf of Suez cannot be held to be evidence of trough-faulting, since the same can be observed along the scarps of the Wadi Araba, the structure of whose floor shows it to be an eroded anticline, and the faults along its scarp-faces to be merely huge landslips.2. The faulting observable immediately along the coast of the Gulf of Suez is of an exactly similar nature to that above mentioned, and along part at least of the gulf the strata dip away from the sea on the opposite coasts, leading to the inference that the Gulf of Suez is, like the Wadi Araba, an eroded anticline.3. If it be granted that the Gulf of Suez is not a trough-fault, the argument against the Nile Valley being a trough-fault is strengthened, the support of parallelism being removed.
I.—On a Preglacial Shoreline in the Western Isles of Scotland
Authors: Wright W. B. 
Published: May 2009

The preglacial platform of marine erosion discussed in the following pages was first discovered in the Island of Colonsay in the course of the geological survey of that island carried out in the summer of 1907, and the information then acquired is communicated with the permission of the Director of the Survey. The subsequent tracing of the shoreline in the adjoining islands was effected with the aid of a Government grant for scientific research in the gift of the Royal Society of London. For clearness and convenience of reference the subject will be treated under the following heads:—I. Introductory remarks indicating the aims of the investigation.II. Colonsay and Oronsay—description of the preglacial platform.III. Islay.IV. Mull and Iona.V. The Treshnish Islands.VI. Conclusion, setting forth the present state of the subject.
II.—Additional Note on the Correlation of the Rocks associated with the Devonian Limestones of the Hindu Khoosh
Authors: McMahon C. A. 
Published: May 2009

Since the publication of the joint paper by Mr. W. H. Hudleston and myself on “Fossils from the Hindu Khoosh,” in which the Devonian age of well-preserved fossils found in the limestone member of a series in Chitral was demonstrated, my attention has been called by Mr. T. H. Holland to the fact that the series in Chitral agrees very closely with the rocks known to the Geological Survey of India as the infra-Trias, and described, for the last time, in Hazara by Mr. C. S. Middlemiss.The Chitral series consists of three principal formations:— (1) A lower bed of conglomerate with rounded to subangular pebbles, varying greatly in size up to 3¼ inches in diameter, lying in an indurated, fine-grained matrix of slaty grit or arenaceous mudstone. The pebbles consist of limestone, slates, sandstones, and quartzites, with rounded, white quartz-pebbles, which recall the ‘eggs’ of the Blaini conglomerate of the Simla area. (2) A middle band described by my son, who made a hurried visit to the place, as red sandstone; and (3) an upper bed of grey, dark-blue, and creamcoloured fossiliferous limestone.In Hazara the system of rocks known to the Geological Survey as the infra-Trias, on account of its position unconformably below the Trias, consists in the same way of a lower conglomerate, a middle sandstone series, and an upper limestone formation. These rocks, originally referred to by Wynne and Waagen, were described in fuller detail by Middlemiss in 1896.According to Middlemiss, the conglomerate is composed of sub-angular pebbles of slates and quartzites, usually of about the size of a cricket ball, but varying from mere pebbles to larger lumps, and set in a fine purple sandy clay or shale.
IV.—On the Constitution, Origin and Dehydration of Laterite
Authors: Holland T. H. 
Published: May 2009

The objects of this note are three: (1) to call attention to the essential chemical similarity between laterite and bauxite; (2) to offer a theory for the formation of laterite in the moist tropics; (3) to suggest an explanation for its spontaneous dehydration.(1) Laterite has generally been referred to as a ferruginous clay; but if the term clay is restricted to substances having a basis of hydrous silicate of alumina, this definition is incorrect. The alumina in laterite exists, as it does in bauxite, in the form, of hydrous oxides. Kaolin must thus be removed finally from the list of weathering products; it is formed generally, perhaps exclusively, by the action of subterranean vapours on aluminous silicates. This conclusion necessitates a re-examination of many so-called argillaceous substances; many doubtless include the kaolin already existing in the kaolinized aluminous silicates before they are exposed to the weather. But it is probable that some of the red clays of past geological ages, formed under subaerial conditions, contain free hydrous oxides of alumina; and for those that are shown to contain hydrous silicate of alumina, it would be well to test the possibility of a secondary reunion of aluminic hydrate and free silicic acid.(2) To account for the fact that an aluminous silicate undergoes a more complete disintegration under tropical conditions than under the deep-seated and presumably high-temperature conditions of kaolinization, the writer suggests that laterite is due to the agency of lowly organisms, possibly akin to the so-called nitrifying bacteria.
I.—Woodwardian Museum Notes: Brachymetopus Strzeleckii, McCoy, 1847
Authors: Reed F. R. Cowper 
Published: May 2009

The genus Brachymetopus was founded by McCoy in 1847, and the generic characters were drawn from the Australian species Br. Strzeleckii, McCoy, which was at the same time described. The specific characters of this form were very briefly given, the leading features having been mentioned in the diagnosis of the genus. Dr. Henry Woodward in 1884 gave a new summary of the generic characters differing somewhat from that originally furnished by McCoy, being modified in such a way as to include the European or British species, Br. ouralicus, De Vern., Br. Maccoyi, Portl., Br. discors, McCoy, and Br. hibernicus, Woodw. The original type-specimens of Br. Strzeleckii used by McCoy (op. cit.) in drawing up the description of the genus, and figured by him at the same time, are in the Woodwardian Museum, to which they were presented in the year 1844 by the Rev. W. B. Clarke. They come from the Carboniferous Shale of Dunvegan, New South Wales. The specimens comprise three complete head-shields, two of which are hollow impressions and one a cast, and portions of three or four others; there are also three casts of complete pygidia, one perfect impression, and fragments of two others. This material demands a fuller description of the specific characters than McCoy furnished, particularly as this type-form of Brachymetopus shows features differing in several respects from those of the better known European species ascribed to the same genus. McCoy's description (op. cit.) of the species was as follows:—“Glabella widest at the base, with one very minute, obscurely marked, cephalothoracic furrow at the base on each side; all the segments of the pygidium with an irregularly tuberculated ridge along the middle; lateral segments forming large tubercles where they join the thickened limb, opposite each of which is a short slender spine projecting from the margin”.
II.—The Classification of the Rocks of the Western Australian Goldfields
Authors: Thomson J. Allan 
Published: May 2009

Thanks to the descriptions published by visiting mining engineers and the more detailed work of the Geological Survey of the State, the general geological features of those parts of Western Australia in which mining is carried on are now well known. A surprising degree of uniformity of geological structure and mode of gold occurrence is revealed over an extent of country unparalleled elsewhere in the world. And yet it is safe to assume that to the casual reader who has not visited the country the above publications present little else than a mass of bewildering detail.“For reasons which can be readily understood, geological inquiry in Western Australia has up to the present consisted chiefly of a series of unconnected observations to the co-ordination of which we must look to the future.”
IV.—On the Recognition of Two Stages in the Upper Chalk
Authors: Jukes-Browne A. J. 
Published: May 2009

The next step is to see if the evidence of the Echinodermata coincides with and confirms that of the Cephalopoda. The Echinoderms will be tabulated in the same way as the Cephalopoda, beginning with those of Germany. The following table has been compiled from several sources, and may not be quite complete as regards the irregular forms, though it is practically so for the Regulares, this part being taken from Schlüter's monograph on that order:—From this table it will be seen that there are two different Echinoderm faunas in Germany, just as there are two different Cephalopodan faunas, only two species passing from the lower three to the two highest zones. There is not, however, such a clearly marked line of separation; the fauna of the S. binodosus zone seems from the tabulated species to be linked as closely with the higher as with the lower zones, for it contains sixteen species, of which number ten appear to be restricted to the zone and three range both up and down, while one passes downward only and two range upward. This result, however, is deceptive, because the Emscher is so poor in Echinoderms that only six species have been recorded from it, and only eight have been found in the Marsupites zone.
II.—Memorial to Henry Alleyne Nicholson, M.D., D.Sc., F.R.S.
Authors: H. W.  
Published: May 2009

The recently erected Memorial to the late Professor Henry Alleyne Nicholson, F.R.S., of Aberdeen, raised by subscription among his friends, deserves a record in the pages of this journal, to which he was for many years a frequent contributor (see Obituary of Nicholson, GEOL. MAG., 1899, pp. 138–144, with a portrait, Plate IV).Professor Charles Lapworth, LL.D., F.R.S., of the University of Birmingham; Mr. John E. Marr, M.A., F.R.S., St. John's College, Cambridge; Dr. Henry Woodward, F.R.S., late of the British Museum (Nat. Hist.); and Professor J. Arthur Thomson, M. A., who succeeded Nicholson as Eegius Professor of Natural History in the University of Aberdeen, with very many others, decided to commemorate Nicholson's lifework by some simple yet permanent record; and after consultation with the University authorities it was decided that the memorial should take the form of a Tablet similar to that erected in Aberdeen to the memory of Macgillivray.The preparation of a design was entrusted to Miss Alice B. Woodward, and the execution to the well-known artists in metal, Messrs. Omar Ramsden & Alwyn C. E. Carr, of Albert Studios, Albert Bridge Road, London, 8.W.The Nicholson Memorial Tablet (which measures 3 feet 8 inches by 2 feet 11 inches) is executed in hand-beaten and repoussé brass, mounted upon a stout framing of oak, and is a good example of the effort now being made to improve the artistic quality of such work, and render it more worthy of its object than the ordinary hurried modern machine-produced metal-work.
III.—Upper Cretaceous Terebelloids from England
Authors: Bather F. A. 
Published: May 2009

The tubes formed of fish-debris, found throughout the Chalk of England, described by Mantell (1822) as Murœna(?) lewesiensis, referred by L. Agassiz (1844) to Dercetis elongatus, and placed among Annelida Tubicola as Terebella lewesiensis by William Davies (1879), are here described with more precise detail and retained in the position assigned to them by Davies. A diagnosis is provided and a holotype selected.A specimen from the Gault, of similar nature but larger, is made the type of a new species, ‘Terebella’ lutensis (Fig. 6).Similar tubes from the Cenomanian, built of Conifer debris and Echinoderm debris, are described, and the question whether these differences of composition indicate a difference of species is discussed, but left open for the evidence of further material. Such tubes may for the present be known as ‘Terebella’ cf. lewesiensis (Figs. 7, 8).Tubes without extraneous building material and with a cancellar ornament are also found in the Cretaceous rocks of England, and some were referred to Terebella lewesiensis by Davies. All those from the Chalk are here separated as ‘Terebella’ cancellata, n.sp. (Figs. 3–5).Two tubes made of mud bricks are discussed. One, apparently of Lower Cenomanian age, is referred to the rather doubtful genus Keckia (Fig. 1). The other, from the Gault, is referred to Granularia (Fig. 2). Both these genera are held to be of Annelid origin.
III.—The New Red (Permian) Gravels of the Tiverton District
Authors: Martin Edgar C. 
Published: May 2009

The New Red gravels of the Tiverton type extend from Warbrightsleigh and Chimney Down on the north to Thorverton and White Down Copse on the south. Further south they are replaced by breccias and sandstones or covered by the higher beds of the New Red series. Throughout the whole of this area of nearly 100 square miles the gravels contain fragments of sandstone and grit with Upper Devonian fossils. These Devonian fragments are most common in the north-east of the district, and are comparatively rare further south. They are found at the entrance of the Crediton valley, but do not appear to be present further west.All the fossils that have been identified are known to occur in the Pilton and Marwood Beds of North Devon. The only Trilobite found (Phacops latifrons, Bronn) is practically the only Trilobite occurring in the Pilton Beds, where it is very common. Spirifer Verneuili, Murch., Spirifer Urii, Flem., Rhynchonella (Camarotæchia) Partridgiæ, Whidb., and Productus prælongus, Sowerby, are the commonest Brachiopods both in the gravels and in the Pilton Beds. The little Gasteropod Euomphalus vermis, Whidb., is also common in the gravels and Pilton Beds. Bellerophon subglobatus, M'Coy, is a characteristic fossil in the Marwood Beds of the Barnstaple district; it is also common in the grits that occur further east near Wiveliscombe, and in the grit fragments found in the gravels.At Chimney Down, in the north-east of the district, fossiliferous fragments of Upper Devonian sandstone and grit are extremely common, whilst trap fragments appear to be absent. This fact, as well as the wide distribution of the fossiliferous fragments, completely disposes of the Rev. W. Downes' theory of volcanic ejection. The facts tend, rather, to prove a drift from the north-east during the period of deposition of the gravels. The grit and sandstone matrices suggest a derivation from the Wiveliscombe end of the Pilton Beds rather than from the more slaty beds found further west. The Devonian fragments in the gravels may even have been derived from a still more easterly extension of the Pilton Beds, now buried under Triassic deposits.
II.—The Old Red Sandstone of Forfarshire, Upper and Lower
Authors: Hickling George 
Published: May 2009

The Lower Old Red Sandstone of Forfar and Kincardine is upwards of 14,000 feet in thickness. No indication of a base or natural top is seen in the district. The characteristic fossils of this series have all been obtained from its middle beds within a vertical range of less than 4,000 feet. There is no palæontological evidence of the age of the beds above or below that zone. It is concluded, on physical and palæontological grounds, that the fossiliferous beds of the Orcadian area are really younger than those of Forfarshire, but there is no proof that the higher part of the Forfarshire series was not contemporaneous with the Orcadian deposits.The folding of the Lower Old Red strata into the syncline and anticline parallel to the Highland boundary fault took place subsequently to the deposition of the whole of those strata. This folding, and denudation to the extent of 8,000 feet over the anticlinal axis, were accomplished after the deposition of the Lower and before the beginning of the Upper Old Red. The surface on which the Upper Old Red rests, in Forfarshire, is broadly horizontal, but very uneven—evidently an old land-surface.
VIII.—On the Relation of the Sands and Clays of Dorset and Hants to Those of Bovey Tracey
Authors: Fisher O. 
Published: May 2009

I Have read with interest Mr. Lowe's articlel on Devonshire geology, in which he discusses the question whether the Bovey beds are Miocene or Eocene, and what may be their relation to the Hampshire and Dorsetshire Lower Bagshots.In former years I have had some acquaintance with the Hants and Dorset beds, and I have seen the Bovey deposit and was struck with their similarity. I am much impressed with the weight of Mr. Lowe's objection that the enormous amount of detritus represented by the sands and clays extending from Bournemouth—or we may even say from Whitecliff Bay, I.W.—to Bovey can hardly have been derived from so small an area as Dartmoor.
III.—Notes on Some Books from New Zealand
Authors: Rastall R. H. 
Published: May 2009

The specimens on which the following notes are based were JL collected by Mr. H. T. Ferrar, M.A., F.G.S., while on a tour through New Zealand, during the time the “Discovery” was being overhauled in Lyttelton, on her return from the Antarctic. The topographical and field notes were also supplied by Mr. Ferrar, and it must be clearly understood that only the detailed petrographical descriptions are the work of the present writer.The specimens were obtained near the middle of the North Island of New Zealand, and in the area marked “acidic volcanic rocks” in Sir James Hector's geological map of New Zealand, published in 1883. They all occur in the Taupo zone, the hot-lake district which lies roughly between Lake Taupo on the south and Lake Rotorua on the north.
VII.—Recent Marine Clays At Kuchavelli, Ceylon
Authors: Coomaraswamy Ananda K. 
Published: May 2009

Kuchavelli is twenty-two miles north of Trincomalee on the JV. east coast of Ceylon. Two miles south of Kuchavelli is the mouth of the Salape aru. On the right bank of this river, near the mouth, raised beach, consisting of shelly sandstone, is exposed. The sandstone is often full of marine shells, and there are also thick growths of oysters attached to upstanding masses of rock. The bed is from 6inches to 2 feet in thickness, and is exposed about 1 foot above high-water mark, and stretches down the sloping bank between tide-marks. This is the ordinary raised beach of Ceylon, a deposit usuallyoccurring at or below high-water mark, and now being continually eroded at numerous points on the coast of Ceylon where it is exposed (e.g. Bentota). This deposit will not now be further spoken of.The Salape aru is really the name of the estuary of several rivers; proceeding up the river inland, the Matti aru is reached, a shallow river with alluvial banks eight or ten feet above the water on either side. Extensive sandbanks are found on one side or the other of the river, alternating on the meanders with places where erosion is in progress. These banks are covered with marine shells, the large flat Placunas being most common. There are also found clayey nodules including marine shells, crabs, and it is said sometimes tortoises and fishes. The crabs are collected for use as medicine, being powdered and mixed with milk or water as a specific for diabetes.
III.—On Some Fossil Cephalopoda from North Cornwall Collected by Howard Fox, F.G.S.
Authors: Crick G. C. 
Published: May 2009

The following descriptions are based upon fossils sent to me for determination by Mr. Howard Fox, F.G.S. Excepting the specimen which is compared withOrthoceras hercynicumand is marked “E. of Cant Cove,” the fossils are from Cant Hill, St. Minver, N. Cornwall.At the end of the descriptions are added notes upon some very imperfect fossils which Mr. Fox has collected from other localities in St. Minver.