bluuebunny/crossref_metadata_2025_split huggingface dataset:
Odontocaulis Lapworth, a synonym of Callograptus Hall
Authors: Bulman O. M. B. 
Published: May 2009

The original generic diagnosis is as follows:—“Polypary cyathiform, composed of numerous independent and frequently bifurcating polypiferous branches, originating from the distal extremity of a short stem, which is likewise polypiferous and is terminated proximally in an irregular corneous expansion. Hydrothecae of the type of those of Dictyonema, biserial, sub-alternate.“The chief peculiarity of this genus is afforded by the character of the stem, which is identical in every respect with the main branches, and, like them, is denticulate or polypiferous throughout the whole of its extent. It commences proximally in a flattened expansion, with irregular or frayed-out edges, possibly the remains of a disk or bulb of attachment.“The mode of branching is rigidly dichotomous, the first two branches being formed by the sub-division of the main stem itself. Each arm branches and rebranches again and again in the same manner, at frequent and close intervals, composing an elegant cyathiform or fan-like polypary, very symmetrical in form. The branches retain their original width to their final division, which gives rise to two minute branches less than one-tenth of an inch in length.
Metamorphism in the Upper Devonian of N. Cornwall
Authors: Phillips F. Coles 
Published: May 2009

The geological succession and structure of the district are briefly summarized. Evidence of stress conditions becomes increasingly abundant as one passes from south to north towards the boundary of the Carboniferous.The thermal alteration due to the Bodmin Moor granite is definitely delimited by tracing the outer limit of spotting in normal pelitic sediments.Petrographical study of phyllites from outside this limit shows considerable mineralogical reconstruction in the sediments, with crystallization of white mica, chlorite and chloritoid; in some instances garnet is developed. The distribution of these types shows no relationship to the granite outcrop, but accords with the main structural features of the area.Analogous changes are prominent in the igneous horizons, with the formation of schists of the general type of prasinite.Within the aureole thermal effects can be traced superposed on the earlier dynamic changes.From these lines of inquiry it is concluded that many of the changes in the phyllites, notably the formation of porphyroblastic white mica, chlorite and chloritoid, hitherto ascribed with greater or less finality to the action of the granite, are due to an earlier dynamic metamorphism.
The Carboniferous Limestone Series of West Cumberland
Authors: Edmonds Charles 
Published: May 2009

SummaryThe examination of the fossil fauna, the chief forms of which are shown in Tables I and II and Fig. 1, shows that the beds commence at a high horizon of the Seminula Zone and extend to the top of the Dibunophyllum Zone. Also, the “life-zones” established by Professor Garwood in his North-Westem Province Paper can be readily recognized in our area and the series includes the sequence from the Nematophyllum minus sub-zone of the Productus corrugatohernisphericus Zone to the Dibunophyllum muirheadi sub-zone of the Dibunophyllum Zone. It can further be established that the limestones of our area do not persist up the horizon of the Botany Beds with Aulina mtiformis S. Smith. The Saccammina Band occurs in our area, but Saccammina occurs also in the limestones immediately above and below. The Girvanella Band of the North-West Province has been recognized and forms a constant horizon throughout the area. It occurs associated with a calcitemudstone and never as a nodular bed. Other bands also appear to be algal. The Spiriferina cf. laminosa Band of Garwood forms a constant horizon between the Seventh and Sixth Limestones.
The Petrology of the Pennant Series, East of the River Taff
Authors: Heard A. 
Published: May 2009

SUMMARYThe occurrence of iron carbonate as a part of the cement in the Pennant Sandstone is not extraordinary, when the large amount of entombed organic matter is taken into consideration. The presence of organic material and the products of decay, the so-called humus acids, acting as reducing agents, would aid in the formation of iron carbonate and prevent its oxidation. Much of this carbonate probably owes its presence to a metasomatic replacement of calcium carbonate. The granules of siderite may have been derived from rocks similar to those of the Lower Coal Series of South "Wales. The alkaline carbonates which hold the humic substances in solution would readily dissolve silica, thus becoming effective agents in the solution and redeposition of silica in the rock. A solvent of this kind would be formed by the impregnation of alkaline salts by carbonic acid.1 The occurrence of so much secondary silica in the rock is probably the result of a redeposition of silica from such a solution. No oxides of iron have been found in any of the numerous separations, either by means of heavy liquids or the electro-magnet; their absence is easily explained when we consider the strongly reducing environment of the deposition and consolidation of the Pennant Sandstone. The perfectly rounded globules of sphserosiderite may have been precipitated whilst the sandstones were being deposited, but more probably derived from the denudation of fireclays similar to those of the Lower Coal Series of South Wales.2 The dominant mineral chlorite, existing as perfect cleavage flakes, is entirely distinct from the secondary aggregates of chlorite in the rock, and was probably deposited in its present form. I have examined a powdered specimen of the Delabole Slates of Cornwall (Upper Devonian), and have found in it a large proportion of chlorite flakes, exactly like the detrital chlorite of the Pennant Sandstone. The very few flakes of biotite found show little trace of alteration. The paucity of heavy minerals indicates that the Pennant sediments had not a granitic source; they were mainly derived from pre-existing sediments which were rich in chert, had abundant chloritic material present, and yet were capable of furnishing fairly fresh biotite. Metamorphosed shales would account for the presence of cordierite and corundum.
III.—The Purbeck Beds of the Vale of Wardour
Authors: Jukes-Browne A. J. 
Published: May 2009

The paper written by the Rev. W. R. Andrews and myself, published in 1894, gave a more complete account of these beds than had previously been attempted; we showed that they were divisible into Lower, Middle, and Upper groups, comparable with those established by Professor E. Forbes in the Purbecks of Dorset, and characterized by the same species of Cyprides. This paper was based on the joint examination of exposures visible in 1890, though one of us, being then resident at Teffont, had observed and collected from these exposures for many years.In the following year (1895) Mr. H. B. Woodward's memoir on the “Middle and Upper Oolitic Rocks” was published, and his account differed from ours in several particulars, notably as regards the thickness of beds referable to the three several divisions, as to the interpretation of the section near Dinton Station, and as to the total thickness of the formation. We refrained from comment at the time, partly because we were prepared to accept such corrections as were based on the freshly cut exposure near Dinton, and partly because the mapping of the distriot had not then been completed, and we were content to wait till this was done, in the expectation that Mr. Woodward would then reconsider some of the points on which we were not in agreement with him.The mapping of the area was completed in 1900 by Mr. C. Keid, and this year (1903) the map (Sheet 298, new series), together with an explanatory memoir prepared by Mr. Reid, have been published.
III.—Notes on new or imperfectly known Chalk Polyzoa
Authors: Brydone R. M. 
Published: May 2009

Zoarium small, highly conical, slightly compressed in one direction, very fragile.Zoœcia rather bluntly hexagonal, subradially arranged in straight rows which from time to time diverge to admit a new row, length ·35–·4mm., width about the same; the area varies from distinctly elliptical to practically circular; maximum length ·33 mm., breadth ·3 mm.
I.—The Functions of Geology in Education and Practical Life
Authors: Watts W. W. 
Published: May 2009

At the Leeds Meeting of the British Association in 1890, my old friend Professor A. H. Green delivered an address to the Section which has generally been regarded as expressing an opinion adverse to the use of the science of geology as an educational agent. Some of the expressions used by him, if taken alone, certainly seem to bear out this interpretation. For instance, he says: “Geologists are in danger of becoming loose reasoners”; further he says: “I cannot shut my eyes to the fact that when geology is to be used as a means of education there are certain attendant risks that need to be carefully and watchfully guarded against.” Then he adds: “Inferences based on such incomplete and shaky foundations must necessarily be largely hypothetical.”Such expressions, falling from an accomplished mathematician and one who was such an eminent field geologist as Professor Green, the author of some of the most trustworthy and most useful of the Geological Survey memoirs, and above all one of the clearest of our teachers and the writer of the best and most eminently practical textbook on physical geology in this or any other language, naturally exercised great influence on contemporary thought. And I should be as unwise as I am certainly rash in endeavouring to controvert them but for the fact that I think he only half believed his own words. He remarks that “to be forewarned is a proverbial safeguard, and those who are alive to a danger will cast about for a means of guarding against it.
V.—What is Laterite?
Authors: Fermor L. Leigh 
Published: May 2009

1. The term laterite is used in two ways, namely, stratigraphically as the name of a geological formation, and petrographically as the name of a tropical superficial rock. This discussion relates only to the use of the term as a rock name.2. Laterite (or rather some varieties of it) is formed by a process, the modus operandi of which is not discussed here, by which certain rocks undergo superficial decomposition, with the removal in solution of combined silica, lime, magnesia, soda, and potash, and with the residual accumulation, assisted, no doubt, by capillary action, metasomatic replacement, and segregative changes of a hydrated mixture of oxides of iron, aluminium, and titanium, with, more rarely, manganese. These oxides and hydroxides of iron, aluminium, titanium, and manganese are designated the lateritic constituents.3. This residual rock is true laterite, and the presence of any considerable proportion (> x10 per cent) of non-lateritic constituents requires expression in the mime, as it always indicates want of completion in the process of lateritization. True laterite contains, then, 90 to 100 per cent of lateritic constituents.
VI.—On the Recent Tufaceous Deposit of Totland Bay, Isle of Wight
Authors: Kennard A. Saxter , Warren S. Hazzledine 
Published: May 2009

On the top of the cliff between Headon Hill and Widdick Chine, in Totland Bay, there is a Recent tufaceous deposit containing land and fresh-water shells. It extends along the cliff for nearly 350 yards in a north-easterly direction from the base of Headon Hill, and is about 60 feet above the sea-level.It was first described by Mr. Joshua Trimmer, and subsequently by Professor Edward Forbes and Mr. H. W. Bristow. In the more recent memoir on the Isle of Wight the earlier descriptions are quoted, but the section is described as being then almost entirely overgrown.
II.—Further Notes on the Mammals of the Eocene of Egypt
Authors: Andrews C. W. 
Published: May 2009

The skull of one species (A. Zitteli) of this remarkable ungulate has already been figured by Mr. Beadnell, and also in this Magazine (December, 1903), where its general form is well shown. Details of the structure of the skull and skeleton will be given in the monograph, so that only a few of the more important characters need be referred to here.The pedunculate occipital condyles are very large and prominent; the occipital surface slopes strongly forwards and is bordered by a massive lambdoidal ridge, which on either side (in old animals at least) rises into a prominent backwardly directed boss of bone, almost like a blunt horn. The parietal region of the cranial roof is flat and is at right angles to the side walls of the skull, being sharply marked off from them by well-defined ridges, which form the upper limits of the temporal fossæ. The suture between the parietals is obliterated in the youngest skull examined. The pair of small posterior horns over the orbits are borne exclusively by the frontals, while the great anterior pair seem to be formed entirely by the enormously developed nasals.
VI.—The Salt Deposits of Dax and the Pyrenees
Authors: Stuart-Menteath P. W. 
Published: May 2009

On the rail to Biarritz the roots of the Pyrenees first appear at Dax, and are accompanied by those ophites and thermal springs which are special features of the entire chain. Vast deposits of salt, to whose first development I contributed, have added an important industry to the resources of this ancient capital of Aquœ Tarbelliœ, where the exact harness depicted on Roman medals is still characteristic of every cart. Beneath the existing ditch of the Roman fortifications rock-salt was accidentally discovered by a boring for mineral water, and the salt is now worked at three miles to the south-east, and is indicated by springs for a distance of seven miles. The deposit is known to be about 100 feet in thickness, but is of unknown depth beneath the existing borings.Along the entire outskirts of both sides of the Pyrenees similar salt deposits abound, and they are often similarly accompanied by igneous rocks.The salt formation of Dax is distinctly limited by the valley of the Adour, which here ceases to wander among the sands of the plain, and is suddenly and sharply diverted along a tectonic depression, running towards the Pyrenees in a south-west direction. Precisely parallel to this course, in the Cretaceous and Tertiary rocks of the Pyrenees, there runs, at a dozen miles to the north-west, the most remarkable example known of a tectonic valley sunk beneath the ocean. The Gouf de Capbreton, sinking with steep sides to over 3,000 feet beneath the even bottom of the Atlantic skirt, and affording evidence of igneous rocks in its surroundings and in the irregularities of its floor, is a perfect analogue of the neighbouring tectonic portion of the Adour.
I.—Sedgwick Museum Notes. New Fossils From the Haverfordwest District. II
Authors: Reed F. R. Cowper 
Published: May 2009

There is one complete individual of a species of Phacops from the Orthis-argentea zone of Prendergast Lane, Haverfordwest, showing certain interesting characters which make it worthy of notice. The head is somewhat crushed and imperfect, but the glabella is seen to be large and broad and to expand regularly towards the front; the frontal lobe is transversely rhomboidal and nearly half the total length of the glabella; there are three pairs of lateral lobes, of which the anterior pair is the largest; the second pair is narrower, and the third pair is subequal to the second in size. The first pair of lateral furrows is oblique; the second pair is horizontal and slightly arched forwards; the third pair is slightly oblique and the most strongly marked of all; the occipital furrow is strong and curved forwards in the middle. There is only a narrow median strip of the glabella not crossed by the lateral furrows, for they are rather long and all reach inwards to about the same extent.The thorax has a prominent axis about three-fourths the width of the pleuræ, which are bent downwards and backwards beyond the fulcrum, which is situated at about half their length. Their extremities are slightly bent forwards and apparently rounded or bluntly pointed; a deep diagonal furrow traverses the whole length of each pleura.The pygidium is nearly semicircular, with a regular rounded margin, except behind the axis, where there is developed a long, pointed, straight posterior spine, about two-thirds the length of the pygidium.
XI.—The Glaciation of Holyhead Mountain
Authors: Greenly Edward 
Published: May 2009

The bare and rocky hill known as Holyhead Mountain is of considerable interest in connection with recent geological events, standing as it does some thirty miles out from the highlands of Carnarvonshire into the Irish Sea Basin; and in such remarkable isolation, for it is much the highest of the five hills which rise above the general level of the platform of Anglesey.Its height is only 721 feet, but so strongly featured is it, especially towards the west, that one feels the term ‘mountain’ to be no misnomer, and can hardly believe it to be really lower than many of our smooth wolds and downs of Oolite and Chalk. Being composed, moreover, of white quartzite (or more properly of quartzite-schist), and being so bare of vegetation, it recalls much more vividly certain types of scenery in the Scottish Highlands than anything in those Welsh mountains that one sees from its sides. Towards the east it slopes at a moderate angle, but a little west of the summit it is traversed by a very strong feature, due to a fault, running nearly north and south, along which is a line of great crags, facing west, and prolonged northwards into the still greater sea cliffs towards the North Stack. Beyond this the land still remains high, but is smoother in outline, a somewhat softer series of rocks extending from the fault to the South Stack, where the high moors end off in great cliffs above the sea.
II.—Note on the Lower Culm of North Devon
Authors: Vaughan Arthur 
Published: May 2009

In the Geological Magazine, August, 1904, pp. 392–403, Dr. Wheelton Hind describes the Lower Culm beds of North Devon and assigns them to the ‘Pendleside’ series.From the original paper dealing with that series I gather that in the North of England the ‘Pendleside’ beds lie above the uppermost zone of the Carboniferous Limestone, and are the equivalents of the Millstone Grit of the South Wales and Mendip areas. Dr. Hind's contention is, then, that the Lower Culm of North Devon was laid down at a time subsequent to the deposition of the whole of the Carboniferous Limestone of the Mendips and South Wales.
III.—Notes on the Rhætic Rooks Around Charfield, Gloucestershire
Authors: Richardson L. 
Published: May 2009

The object of this communication is to record some recently-made notes on the Rhætic beds of the neighbourhood of Charfield.In 1876 Mr. H. B. Woodward, F. R. S., wrote: “Turning to the esearpment of Penarth beds between Tites Point and Wickwar, we find them exposed in many places. Long ago Sir Roderick Murchison stated that ‘passages from the Lias into the underlying New Red Sandstone can be observed in the sides of Whitecliff Park Hills, south of Berkeley; but the clearest and best instances are to the east of Wickwar, near Sturt Bridge, on the sides of the new road ascending to Wotton.'” This is all that has been written on the area now under consideration. As is well known, the junction of the Rhætic and Keuper Series is usually marked by a low but distinct escarpment. Between Tites Point and Berkeley Road Station this physical feature is not pronounced, but becomes gradually more prominent to the south of the Junction.
IV.—The Devonian Rocks of Cornwall
Authors: Ussher W. A. E. 
Published: May 2009

Sedgwick and Murchison, the Rev. D. Williams, and Dr. Holl, taking the Plymouth limestones as a middle division, placed them below the rocks to the south and above those to the north. The prevalent southerly dips of schistosity were regarded as ample evidence of a downward succession proceeding northward.The Staddon grits and other Lower Devonian rocks were thus placed above the Middle Devonian, and the slates in which I have at various times since 1892 found Upper Devonian fossils (between Menbeniot and St. Budeaux) were relegated to a position below the Middle Devonian.
I.—Notes on British Dinosaurs. Part III: Streptospondylus
Authors: Nopcsa Francis Baron 
Published: May 2009

After having studied a bipedal and a quadrupedal Orthopodous Dinosaur I thought it desirable to turn my attention to a bipedal representative of the Saurischian order.Though Streptospondylus is by no means an exclusively British Dinosaur, since the type-specimen is preserved in the Jardin des Plantes in Paris, and was described, under the names Streptospondylus and Megalosaurus by Cuvier and Gaudry, still, the only other specimen known, and by far the best, is in Mr. J. Parker's private collection at Oxford. It is to Mr. Parker's kindness that I owe the possibility of studying and drawing what may be called one of the most complete Theropods ever found, while in the Paris Collection Streptospondylus is only represented by several vertebrae, a fragment of the femur, and the distal part of the tibia with the corresponding astragalus. Mr. Parker's specimen includes the skull, most of the cervical, dorsal, sacral, and some of the caudal vertebræ, the scapulo-coracoid, parts of both humeri, the ilium, ischium, parts of the pubis, both femora, tibiæ, and fibulæ, some tarsal and all the metatarsal bones, and several phalanges.
VII.—The Geological Physics of the Shallow Seas
Authors: Hunt A. R. 
Published: May 2009

Since the year 1871 I have been much impressed with the interest and importance of one of the byways of science, the problem of the Geological Physios of the Shallow Seas. Recent discoveries in raised beaches have brought this subject again to the front, and the object of the present paper is to plead for further inquiry by specialists.I may briefly mention my own now antiquated papers, viz., “Notes on Torbay” (Trans. Dev. Assoc., 1878); “The Formation of Ripple-mark” (Proc. Roy. Soc., 1882); “The Action of Waves on Sea Beaches and Sea Bottoms” (Roy. Dublin Soc., 1885); and “On the Influence of Wave-currents on the Fauna inhabiting Shallow Seas” (Journ. Linn. Soc., 1884). With the exception of the Dublin paper, the MSS. were, as a matter of fact, perused by eminent mathematicians, who kindly guarded me against any conflict between observation and theory.
I.—The Recent Geological History of the Baltic. Part II: The Ancylus Sea and the Baltic Breach
Authors: Howorth H. H. 
Published: May 2009

In the previous paper I ventured to trace the history of the Baltic back to the time when the latest of its raised beaches were laid down, and to show that it was then considerably larger in size, and that its waters were more salt than they are now, although they were even then brackish (see Map I, Pl. XIX).This conclusion was derived mainly from an examination of the molluscan remains in the more recent shell-beds. It is confirmed by other evidence; thus, Munthe mentions the occurrence in the so-called Litorina beds of three species of Rhizopods, whose present and former distribution in the Baltic is shown in the following table:
I.—Eminent Living Geologists
Authors: Geikie James 
Published: May 2009

The name of Geikie has become as familar to present-day geologists as those of Murchison, of Sedgwick, or of Lyell were to our immediate prodecessors.Notices and portraits of his elder brother, Sir Arehibald Geikie, K.C.B., the President of the Royal Society, have already appeared in the Geological Magazine (see Vol. for 1890, Pl. II, pp. 49–51, and 1907, Pl. I, pp. 1–2); it is high time to present that of the younger brother, Professor James Geikie, who occupies the leading place in our science and in geography in Edinburgh and itys University, and is known every where also by his published works, especially by his contributions to Glacial Geology.