bluuebunny/crossref_metadata_2025 huggingface dataset:
A Comparison of the Red Rocks of the South Devon Coast with those of the Midland and Western Counties
Authors: Hull Edward
Published: October 2009

In September last I found it possible to carry out a long-standing engagement with the Rev. Dr. Irving to visit South Devon in his company, and to form an opinion upon his views regarding the age and succession of the great series of red rocks which are exposed to view in such magnificent sections along the coast to the east and west of the estuary of the River Exe. On reading Dr. Irving's paper, published in this Journal in 1888, it appeared to me that he had gone very far towards establishing his proposition that the brecciated beds forming the base of the whole series, and resting discordantly on the Devonian rocks, were really the representatives of the Lower Permian breccias of the Midland and Western counties, but I was little prepared for the—I might almost say—overwhelming evidence that such is the case upon an examination of the coast sections extending from Oddicombe Bay to and beyond Teignmouth and Dawlish.

Having examined these basement-beds of the series, we continued our survey of the coast and inland sections of the succeeding strata eastwards to Sidmouth—terminating with the Keuper marls underlying the Cretaceous beds which form the cap of Salcombe Hill, and which break off in a lofty and precipitous cliff seawards; so that the whole structure of the ridge is laid open from the summit to the water's edge. The result of this
reconnaissance
has been to enable me to confirm in all the main points Dr. Irving's view, and to
The Subterranean Erosion of the Glacial Drift, a Probable Cause of Submerged Peat- and Forest-beds
Authors: Shone Wm.
Published: October 2009

The Drift of the N.W., N.E., and Central England covers a large area of the Triassic Series, composed of interstratified hard and soft rocks, giving rise to very unequal denudation of the various members of the series. The Triassic area is consequently of an undulating character, and the Drift which covers it like a mantle partakes of the undulating nature of the rocks it overspreads. The Drift upon the sides of the valleys has, at short intervals, been cut into minor valleys by the rain coursing down their slopes. The minor valleys
cut out of the Drift
should be carefully distinguished from the larger valleys
covered with Drift
, for the latter appear to follow the contour of the pre-Glacial land surface.

Every minor valley has its small streamlet, which in dry weather is most frequently a very insignificant watercourse; during heavy falls of rain, however, such tiny rivulets become swollen into large and rapidly-flowing brooks, charged with densely turbid water derived from the clays, sands, and gravels of the Drift.

The section (fig. 1) is across two such minor valleys. At the S.S.E. end is situated the sandpit, with a face of the pit at right angles to the line of section. Under the surface-soil the pit has a covering of Upper Boulder Clay (varying from 2 to 6 feet in thickness) resting upon Middle Sands and Gravels. About 6 feet beneath the base of the Upper Boulder Clay there was a band of clay a few inches thick in
On Part of the Pelvis of
Polacanthus
Authors: Lydekker R.
Published: October 2009

Among the specimens lately acquired by the British Museum from the collection of the late Mr. Beckles, of Hastings, is one to which my attention has been directed by my friend Mr. A. Smith Woodward. It bears the number R. 1926 in the Museum Register; and, like the majority of Mr. Beckles's specimens, is evidently from the Wealden. Mr. Charles Dawson, who has had so much experience in Wealden fossils, has been good enough to examine the specimen, and considers that it is almost certainly from the Isle of Wight, and not from Hastings.

One glance at the specimen is sufficient to show that it is the central part of a Dinosaurian ilium, with portions of the sacral ribs still attached to its inner surface. It belongs to the right side, as proved by the position of the ischial tuberosity; and while both extremities of the ilium are wanting, the acetabular region is fairly well preserved. The pre-acetabular portion of the ilium forms a roof-like expansion; while the post-acetabular process is compressed and comparatively thin. The upper border of the ilium is straight. The broken portions of the sacral ribs (five in number) are triangular in section, and have deep indentations between them; so that they form buttress-like structures of great strength. The whole contour of the ilium and sacral ribs is quite unlike that obtaining in
Iguanodon
and its allies. It appears most likely that the pre-acetabular portion of the ilium when entire was greatly expanded laterally, as is
On the Rocks mapped as Cambrian in Caernarvonshire
Authors: Blake J. F.
Published: October 2009

Conclusions

The above observations prove that there is a definite succession in the Cambrian series, which is the same in the isolated portion east and south of Bangor as in the main mass. Whether we see the base or not depends on the age assigned to the Dinorwig felsite. If that be Cambrian there might be beds of the same system below it, but there probably are none, since we certainly see the base at Beaumaris. Whether we see the top or not depends on whether the Bronllwyd Grit, which belongs to the overlying group, is conformable or not, and there is no evidence tat it is. In any case, no intervening beds above the Purple and Pale Slates are known in North Wales.

It is also proved that the rocks to the west of the felsite belong to the lower part of the series, and those to the east to the upper, both being determined in areas where the felsite is absent, and hence it appears probable that the felsite mass is a volcanic complex belonging to the middle of the Cambrian period.

Thus my former conclusions, though somewhat modified, are shown to be substantially correct.
The New Railway from Grays Thurrock to Romford: Sections between Upminster and Romford
Authors: Holmes T. V.
Published: October 2009

This railway, which has been in process of construction during the last two or three years and is still incomplete, diverges, from the London and Tilbury line about a mile west of Grays Thurrock station. Thence its range is either northerly or north-westerly. It crosses the Mardyke about half a mile west of Stiffbrd, and its course lies westward of the villages of North and South Ockendon and eastward of Stubbers and Cranham Hall. From Cranham Hall to Romford its direction is more westerly. At Upminster it joins the railway from Barking to Langdon Hills and Pitsea, and then, leaving it again close to Upminster station, keeps on the northern side of the road between Upminster and Hornchurch, and crosses that ranging northward from the last-named village at Butts Green. Then, passing close to, but southward of, the farmhouse called Great Gardens, it joins the Great Eastern Railway about half a mile east of Romford station. The portion of the line south of Upminster is in a more advanced state than that between Upminster and Romford, the mile nearest Romford being at present (Feb. 1892) in the most backward condition.

Having described elsewhere the sections seen between West Thurrock and the Mardyke, I will only remark with respect to that part of the line that the junction of the Chalk with the Thanet Sands was once visible where Back Lane crosses the railway. Thence, to the end of the cutting north of Back Lane, Thanet Sands (below gravel) appeared. The
On the Microscopic Structure and Residues Insoluble in Hydrochloric Acid in the Devonian Limestones of South Devon
Authors: Wethered Edw.
Published: October 2009

The complicated nature of Devonian Geology in South Devon is well known. In this paper I shall confine my remarks to the microscopic examination of the limestones, and shall not enter on the stratigraphical and palæontological problems which have been worked out by such geologists as De la Beche, Jukes, Godwin-Austen, Holl, Champernowne, Etheridge, Ussher, Davidson, Whidborne, H. B. Woodward, and others.

For the purpose of collecting specimens of limestone to be examined I spent a mouth in South Devon during the summer of 1890, and I desire to express my thanks to Mr. W. A. E. Ussher, of H.M. Geological Survey, for the very ready assistance and friendly advice which he gave me.

2. Detailed Examination of the Organic Structure

(a)
Hope's Nose Limestones
.—At Hope's Nose, near Torquay, there is a quarry opened in limestone of varying light and dark colour, and this is capped by a shaly limestone, which Mr. Ussher regards as belonging to the Calceolen Kalk, “apparently completely inverted upon massive bedded limestone containing
Heliolites porosus
.”

Commencing with the
Calceola
Beds, as representative of the basement limestones, thin sections, seen through a microscope, show a light grey, finely-crystalline groundmass traversed by fissures filled with calcite. In the groundmass are ferruginous patches and minute rhombohedral crystals, apparently of dolomite.

Passing to the limestones below—which, it must be remembered, are assumed to be above the
Calceola
Beds when in their normal position—thin sections of the lowest beds exposed show them to be composed of broken calcareous fragments, the structure
On the so-called ‘Gneiss’ of Carboniferous age at Guttannen (Canton Berne, Switzerland)
Authors: Bonney T. G.
Published: October 2009

As a text precedes a sermon, so two quotations may fitly begin this communication. The first comes from a letter written by Dr. Heim, and printed in this Journal as a part of the discussion on my paper entitled ‘On the Crystalline Schists and their relation to the Mesozoic Rocks in the Lepontine Alps’:—“In the Central
massifs
occur rocks which exactly resemble true crystalline schists in mode of occurrence. Petrographically, they are related to them by passage-rocks: at least the line of separation is not easily distinguished. Such rocks are
phyllites, chlorite-schists, felsite-schists, mica-schists
, and especially
sericite-gneisses
, all of which we regard with certainty as Palæozoic. The proofs are the following:...Traces of fossils have been often found (trunks of
Calamites
from Guttannen, in the Haslithal, &c.) . . . The
Palæozoic
formations mostly show an intimate tectonic relation to the crystalline schists, and have been converted petrographically into crystalline schists.” The second quotation is from the reply which I was permitted to append to the above letter:—“Some of these [Carboniferous rocks] I have examined, and think I know them well enough to demur to Dr. Heim's statements concerning them. I have seen, in the Berne Museum, the specimen with ‘the Calamite-like stem.’ When this rock is proved to be a gneiss I shall be prepared to consider the propriety of extending this name to the
Grès Feldspathique
of Normandy, or that of mica-schist to some rocks of Carboniferous age at Vernayaz, in Canton Valais, or of calling the Torridon Sandstone
The Rise and Fall of Lake Tanganyika
Authors: Carson Alexander
Published: October 2009

After alluding to certain observations of Cameron, Livingstone, and Stanley on the changes of level of Lake Tanganyika, the writer states that the most interesting point in connexion with the rise and fall of the lake is the question:—How is it possible for a great lake to rise 30 feet above its normal level by the blocking up of its outlet?

This is to a large extent accounted for by Cameron. He says: “On going down the river [Lukuga] we found that it was blocked by vegetation similar to that on which we had crossed the Sindi, and also to that over which we had had to pass to reach the shore from our boats at the southern end of Lake Tanganyika, and which I afterwards found existed on Lakes Kassali and Mohrya. The presence of this mass of vegetation is easily accounted for. Every day that there is a gale of wind, and the consequent sea on the lake, blocks of this peculiar growth are detached, and such as survive the passage to the outlet getting jammed together commence to grow, and form a sort of porous stopper in the neck of the outlet.” He then quotes Sir Samuel Baker's experience on the Nile when the whole channel “was blocked up and the expedition to Gondokoro impeded for a year, the country above the stoppage having been converted into a series of swamps and shallow lakes, while Egypt was suffering from all the evils of a low Nile.”

Only
The Geology of the Gold-bearing and Associated Rocks of the Southern Transvaal
Authors: Gibson Walcot
Published: October 2009

I. Introduction. (1)
General Sketch of the Geeology of the Southern Transval
.
The
rocky floor of the Transval is very distinct from that of South Africa in general. Travelling for several hundred miles through the northern parts of Cape Colony and the Orange: Free State, such strata as are seen consist of horizontal sandstones and shales of Karoo and Stormberg age. These are injected and overflowed in numberless directions by masses and thin sheets of igneous matter, while worn-down stumps of volcanic necks can be frequently recognized. But in the Transvaal the nature of the strata undergoes a complete Change. Instead of flat-lying sandstones and shales of the wide-spreading Karoo formation, we find twisted and highly inclined quartzites and conglomerates of undetermined geological age. The igneous rocks occur more in the form of bosses than sheets, and make rugged hills with precipitous slopes which are almost bare of vegetation.

At first sight the geological structure of the southern part of the Transvaal appears quite simple, the impression being that the rocks merely form an ordinary basin. So far, however, from this simplicity being real, the geological structure of the country is in fact highly complex, and is rendered still more difficult to unravel from its being apparently impossible to find any distinctive petrological band, available as a means of mapping the grounc), or any group of fossiliferous strata, which might be used as a straggraphical index. The difficulties of mapping the district are also increased by the fact that most
On Further Evidence of
Endothiodon bathystoma
(Owen) from Oude Kloof in the Nieuwveldt Mountains, Cape Colony
Authors: Seeley H. G.
Published: October 2009

I am indebted to Mr. Thomas Bain, Geologist and Irrigation Officer to the Government of Cape Colony, for two bones collected by him in the Oude Kloof, a picturesque mountain-valley which traverses the Nieuwveldt range north of Tamboer, on the road towards Fraserburg.

The remains consist of the left ramus of the mandible, which is almost complete, and what I regard as the left squamosal bone underlapped by the malar in front, but fractured at both ends, so that only the external zygomatic bar is preserved. Small as the cranial fragment is, it is important as showing that the back of the head probably conformed to the type of skull seen in some of the Dicynodonts. The skull was as large aa that of
Dicynodon leoniceps
.

The Zygomatic bar

The longitudinal squamosal bar is 20 centim, long, compressed from side to side and flattened, with the superior border convex in length. The convexity is most marked in the hinder part, where the edge of the bone is about 0Å75 centim, thick and rounded, and the depth of the bone in front of its hinder termination is 6⋅25 centim. A wide shallow concavity extends along the external surface, and appears to be defined inferiorly by a rugose condition of the bone. Anteriorly the depth of the bar is a little less, but its thickness augments; this is due to the strong malar bone, 2⋅5 centim, thick, which forms its infero-anterior border, and extends behind the thin, external, zygomatic prolongation forward of
Notes on Recent Borings for Salt and Coal in the Tees District
Authors: Tate Thomas
Published: October 2009

Since the publication of Mr. E. Wilson's exhaustive paper on the Durham Salt-district, commercial enterprise has given an impulse to exploration, so that now the number of boreholes is over sixty. Most of these simply emphasize the knowledge derived from earlier work, with which they coincide. Three or four, however, may possibly contribute a few geological facts of interest, in relation to (
a
) the area of the Tees Salt-field and (
b
) the determination of the southern limit of the Durham Coal-basin.

1.
Whitehouse, Norton, No. 1 borehole
.—This borehole is twenty two and a half miles due west of Messrs. Watson and Scrafton's Stone Marsh borehole, the most westerly boring shown on Mr. Wilson's map. 2 Its site is 76 feet above sea-level, as proved by a neighbouring bench-mark. Full details of the strata bored through will be found in the Appendix to the present communication. The horizon of the roek-salt in this district lies at the base of the Saliferous Marls, and the layer of salt invariably has above it a bed of anhydrite, usually underlain by a stratum of red marl left in a rotten state by the dissolving out of some constituent: this is the ‘rotten marl’ of the workmen, to the presence of which is due the collapse of many brine-wells. below the beds of pure and impure rock-salt comes the lower anhydrite, so that the salt-bearing stratum, wherever present, is sandwiched between two layers of anhydrite, and its horizon is never a matter of doubt for anyone practically acquainted therewith.
The Dioritic Picrite of White Hause and Great Cockup
Authors: Postlethwaite J.
Published: October 2009

This rock is exposed on both sides of Hause Gill, which separates White Hause from Great Cockup; the exposure on the former measures from 12 to 15 yards square, that on the latter mountain being somewhat smaller. The two masses are about

mile apart, and are doubtless connected beneath the till which forms the floor of the little valley, the only visible connecting-link being a group of blocks jutting out on the northern bank of the stream, which may or may not be in place. The area here indicated is shown in J. Clifton Ward's 6-inch ‘Geological Map of the Lake District’ (now in the Keswick Museum of Local Natural History) and coloured as diorite; it is also shown as diorite in ‘Section I. through Skiddaw,’ in Ward's ‘Physical History of the English Lake District;’ but, so far as I have been able to ascertain, there is no description of the rock in any of his published works, owing in all probability to the fact that it lies a little to the north of Quarter Sheet 101 S.E., which embraces the area treated of in ‘The Geology of the Northern Part of the English Lake District.’ The area is shown in the accompanying map, which is based on that of the Ordnance Survey, Sheet 23 (formerly 101 N.E.).

My first visit to White Hause took place in the spring of 1890, when I was engaged in the preparation of a paper on ‘The Deposits of Metallic and other Minerals
The Tertiary Microzoic Formations of Trinidad, West Indies
Authors: Guppy R. J. Lechmere
Published: October 2009

General Conclusions

The Eocene molluscan faunas of Trinidad show no near alliances with any other known faunas. In this they differ from the well-known and easily recognized Miocene fauna found in Haiti, Jamaica, Cuba, Cumana, Trinidad (Caroni Series), and other localities. Nevertheless a few of the forms have been found elsewhere. The
Echinolampas ovumserpentis, Terebratula carneoides
, and
Ranina porifera
of the Naparima Beds recur in the Eocene of St. Bartholomew's (north-eastern West Indies), and I have already noted that the same beds have a
Nucula
and a
Leda
in common with Barbados. It is only with doubt that the name of
Natica phasianelloides
, a Miocene fossil of Cuba and Jamaica, can be assigned, to the imperfect casts found near San Fernando in Trinidad. Of these casts some are fully 6 inches long. Some
Pinna
-like shells, also in the state of casts, found in these beds are still larger than this.
Erycina tensa
, a near ally of
E. obliqua
, Caillat, of the Paris Eocene, was described by me from the Manzanilla Beds in Trinidad. Gabb included the name in his list of the Miocene fossils of Haiti. When dealing with the fossils of that island I passed over this observation, but I have since seen reason to believes, that Gabb's shell was not
Erycina tensa
, but the flatter valve of a species of
Corbula
. These corrections leave us with a single molluscan species (
Corbula vieta
) in common between the Eocene and the Miocene of the West Indies. The foraminifera of the shallow-water
Notes on some New and Little-Known Species of Carboniferous
Murchisonia
Authors: Donald Jane
Published: October 2009

Every student of the Carboniferous rocks must be struck by the number of keeled gasteropoda they contain, many of which are so small and also so strongly resemble one another that only the study and comparison of a large series can afford means for anything like an accurate determination of different species. As a help towards their elucidation, I am about to figure and define the characteristics of some of the more marked forms of
Murchisonia
. Several of these have been previously described, but I think it well to reproduce them with more detailed notes.

In a previous paper the various sections into which it has been considered advisable to group different species of
Murchisonia
have been noticed. Of the species here described two alone can undoubtedly be referred to
Goniostropha
, Œhl., as possessing the characteristics of that section: namely, the turriculated form, angular whorls, and sinual band situated on the summit of the angle. In
M. quadricarinata, M. quinquecarinata, M. elongate M. Kirbyi, M. plana
, and
M. conula
, var.
convexa
, the sinus is situated above the angle; in other respects these shells resemble species of
Goniostropha
. It is therefore a question whether they should be referred to that section or whether the position of the sinual band be considered sufficiently distinctive to necessitate their being grouped together in a new section. In the latter alternative I should suggest the name
Hypergonia
, and take
M. quadricarinata
for the type.

With regard to
M. pentonensis
, it is somewhat difficult to decide
On a New Reptile from Welte Vreden (Beaufort West),
Eunotosaurus africanus
(Seeley)
Authors: Seeley H. G.
Published: October 2009

When I visited Welte Vreden, near Beaufort West, Cape Colony, in August 1889, Mr. L. Pienaar gave me a small ovate concretion which contained the dorsal region of a new reptile. As preserved it is 7·5 centimetres long and 5·75 centimetres wide.

It shows on the ventral aspect the under surfaces of seven consecutive dorsal vertebræ. These centrums are more slender and elongated than in any South African fossil previously known. They decrease in length from front to back. The first (which may be the first dorsal) is fully 1·25 centim. long, while the seventh is 0·75 centim. long, and is probably the last dorsal or lumbar vertebra, since the pubis is found immediately behind it. These vertebræ in form and number suggest the Chelonian type. They are of an elongated hour-glass form, and relatively longer than in Teleosaurs. The centrum appears to be hollow, but this condition is probably the effect of deep penetration of the conical notochordal substance, as in
Mesosaurus
, and the vertebræ referred by Sir R. Owen to
Tapinocephalus
. A conical cavity penetrates the posterior end of the sixth centrum, and apparently the anterior end of the first, so that the constriction in the middle length of the centrum is due to the tapering away of these conical cups. The articular faces are not exposed, but are inferred to be approximately circular, and the under surface of the centrum is rounded from side to side. In the seventh vertebra a slight lateral widening is seen in
The Base of the Keuper Formation in Devon
Authors: Irving A.
Published: October 2009

In my two previous communications to the Society on the Devon Red Rocks I have recognized the insufficiency of the evidence then available for drawing a clear and well-defined boundary-line between the Keuper and the Bunter in the country lying west of Sidmouth; and now that the Permian age of the lower breccia-series has been definitely recognized by the Director-General of the Geological Survey in his Presidential Address of last February, this may be said to be the only remaining dubious point of importance in our new classification of the Red Rocks of Devonshire, and their correlation with the Permian and Trias of the Midlands and the Severn country. The difficulty I found in drawing the basement-line of the Keuper in my 1888 paper seems to have been felt by Mr. Strahan in the Cheshire area, for, after discussing the evidence on both sides, he seems inclined to think that there are about as good reasons for drawing the basement-line of the Keuper at the bottom of the ‘Waterstones’ (as I did in Devon four years ago) as for drawing it at the base of the ‘Lower Keuper Sandstones‘ of Prof. Hull. Briefly, these seem to resolve themselves into two :— (1) overlap in places of the Waterstone series; (2)lithological similarity of the Keuper basement-beds to the mottled, current-bedded soft sandstones of the Upper Bunter—a similarity which, as I showed in my paper of last year, is even stronger than he has made it out to be in Cheshire, for
Note on the Nufenenstock (Lepontine Alps)
Authors: Bonney T. G.
Published: October 2009

A Change for the worse in the weather, as mentioned in my paper en ‘Crystalline Schists and their relation to Mesozoic rocks in the Lepontine Alps,’ prevented :Mr. J. Eccles and myself from completely examining the Nufenen Pass. In the summer of 1891 we were enabled to make an excursion thither from Ulrichen in the Rhone Valley. Though our visit was necessarily a brief one, for even to the top of the pass it is nearly three hours’ steady walking and an ascent of over 3600 feet from Ulrichen, yet, as the present paper does something to finish off an obviously ‘ragged edge’ in my former communication, I venture to bring the results before the Society.

The upper part of the Nufenen Pass (8006 feet) is a nearly level ‘corridor,’ north of the Nufenenstock (9400 feet), the highest point being at the western end, though the eastern one, above the ascent from the Val Bedretto, is not many feet lower. We were obliged on the former occasion to give up work soon after entering the ‘corridor’ from the latter end. On our second visit we found that the rain had begun at a very inconvenient moment, for another hour of fine weather would have sufficed for clearing up our principal difficulties.

On the northern side of this ‘corridor,’ as stated in the above-mentioned paper, is a gneiss, south of which is a little rauchwacke. This can be traced some distance westward down the slopes. It contains rather numerous fragments of
On some Schistose ‘Greenstones’ and allied Hornblendic Schists from the Pennine Alps, as illustrative of the Effects of Pressure-metamorphism
Authors: Bonney T. G.
Published: October 2009

That a rock originally augitic may become hornblendic is well known, but the cause of the change is less certain. Some authors seem disposed to attribute it, almost as a matter of course, to the direct effects of pressure; that it is so in some cases can hardly be doubted, but that this explanation universally applies must not be hastily assumed. It may, for instance, be demonstrated, as in the classic case of the Scourie Dyke, that a dolerite has been converted into a hornblende-schist, but the question of the efficient cause may still remain open. At the Lizard, as the present author has endeavoured deavoured to show, augite is replaced by hornblende, as in certain of the gabbros, under circumstances which make it highly improbable that pressure has been operative to any appreciable extent. Hence, although schistose ‘greenstones’ have already attracted considerable attention, it may be worth while to describe certain cases in which pressure must have been an important agent of change, in the hope of ascertaining some mineral or structural characteristics which may help us in recognizing metamorphism due mainly to mechanical causes.

The first group of specimens to be noticed in the present paper was obtained in the summer of 1891, when Mr. J. Eccles and myself spent some time at Saas Fee, in the Vispthal. The structure of the great mountain-mass drained by the two branches of the Visp is rather complicated. The rocks are almost wholly crystalline; gneisses appear to occupy the lowest position
On a Secondary Development of Biotite and of Hornblende in Crystalline Schists from the Binnenthal
Authors: Bonney T. G.
Published: October 2009

Pressure is one agent in mineral change. In some eases, as when a shale is converted into a phyllite, the constituents become rather larger, but more commonly the result of oppression is degradation. This is especially true of the crystalline rocks. The effects of earth-movements on granites, gneisses, marbles, mica- and other schists are familiar to all workers in such districts as the Alps or the Scottish Highlands—we might say in almost any great mountain-chain, whatever be its date. Sometimes, indeed, an original constituent has ‘gone through the mill’ comparatively unscathed. Its weaker associates have been crushed to powder, which has acted like a packing-material. But cases occur where new minerals of considerable size are developed here and there from the débris of the original constituents. The greater part of the rock is little more than reconsolidated detritus; it still retains the marks of the
peine forte et dure
to which it has been subjected; but nevertheless it has set up a structure which might be termed porphyritic. The process is analogous to the formation of chiastolite in contact-metamorphism. The mass of the rock is little changed, but a large mineral has been developed: for the one millimetres, for the other centimetres are appropriate standards of measurement.

Still, so far as my experience goes, this secondary development on an important scale is very rare; commonly when large minerals occur in a catathlastic rock, as the garnets in certain Alpine schists, or the sahlite in the fine-grained limestone of Tiree, they
The Marls and Clays of the Maltese Islands
Authors: Cooke John H.
Published: October 2009

I. Introduction

In the year 1843 the late Admiral Spratt published a brief notice on the above subject, and a few years afterwards the late Prof. Gulia and Capt. Hutton alluded to the Marls and Clays in their sketches of Maltese geology. The late Prof. Leith Adams published in 1870 a short account of them in his ‘Notes of a Naturalist,’ but the amount of information that he gives as to the nature of the beds and of their fossil contents is neither very extensive nor very exact. In 1874 the Islands were visited by Thos. Fuchs, of the Imperial Geological Museum of Vienna, and by him the first attempt was made to correlate the Maltese formations with those of Central Europe. In the first of the two pamphlets on the subject that he published he tells us that he was inclined to consider the Maltese Marls as being analogous to the ‘Badner Tegel’ of the Vienna Basin; but two years later, after having examined the marls of Bologna and compared their fossil contents with those of the Maltese beds, he changed his opinion and referred them to the Austrian Schlier. In 1889–90 Dr. John Murray, of Edinburgh, visited the Islands; and in the paper which was published on his return to Scotland he gave the first detailed account that had so far appeared of the nature and constitution of the Maltese rocks. His descriptions were, however, exclusively lithological; and, excepting the list of 122 species of foraminifera which is
Variolite of the Lleyn, and associated Volcanic Rocks
Authors: Raisin Catherine A.
Published: October 2009

I. Introduction.

Although much has now been written about the igneous rocks of the Lleyn, especially in Mr. Alfred Harker's valuable essay, yet, as he expressly excludes most of the district of which I am treating, and as it receives only slight mention in other writings, some of the most interesting examples from the part coloured on the Geological Survey map as ‘metamorphosed Cambrian’ have remained unnoticed. I have therefore put together a few notes on the rocks which I have collected in the course of many visits during the last six years. The specimens not hitherto described include a variolite —a spherulitic, somewhat basic rock. A short summary of its occurrence will at least serve to show that we have on the mainland of our island (apart from any example in Anglesey) a mass of variolitic diabase with characters very similar to those of German and Alpine localities, corresponding closely in many particulars with that graphically described by Mr. J. W. Gregory from the Fichtelgebirge, and also, although perhaps less markedly, with that of the Durance, as shown by Prof. Cole and Mr. Gregory. I am limiting myself mainly to the rocks which can be clearly recognized as igneous, and have given only a short notice of others in the last section of the present paper. The extensive masses of a rather indefinite and schistose character in many parts are ashy or agglomeratie, but include crushed examples of igneous origin. The exact nature of some rocks, however, even when
On some Additional Remains of Cestraciont and other Fishes in the Green Gritty Marls, immediately overlying the Red Marls of the Upper Keuper in Warwickshire
Authors: Brodie P. B.
Published: October 2009

So brief a notice on so limited a subject may seem hardly worthy of the Geological Society, but as a supplement to my former paper published in this Journal in 1887 on the section and fossils from the Upper Keuper Sandstone at Shrewley, three miles north-west of Warwick, it may perhaps be acceptable.

Immediately below the lowest bed of rock, the best and thickest of the sandstones, about 9 feet of grey and green, coarse, sandy marls succeed, resting on red marls. In these green marls no fossils had been hitherto found, except the tests of
Estheria minuta
, often in good preservation; but I have now to record the discovery of numerous large and small spines (ichthyodorulites) of cestracionts, besides palatal teeth of
Acrodus keuperinus
, which are abundant, ganoid fish-scales, and many broken bones, including a fragment of a cranial bone, some of which may belong to fishes and others to labyrinthodonts. These occur in a very thin band of marly, friable, gritty sandstone, full of many small rolled pieces of grit, lying between two beds of green marl; but at a little distance east the same bed is a green marl without any intermixture of sand, containing similar fossils.

The entire length of the section exposed is 115 yards: the green marls predominate, but alternate with six thin layers of sandstone, a thicker one coming just below the ‘bottom-rock.’ The total thickness of these strata, between the latter and the underlying red marls, is about 8 or 10 feet;
Notes on some Coast-sections at the Lizard
Authors: Fox Howard , Teall J. J. H.
Published: October 2009

I. Introduction

The well-known serpentine of the Lizard may be seen in contact with hornblende-schist, and also with the rocks for which Prof. Bonney proposed the term ‘Granulitic Series.’ The object of the present communication is to describe two small portions of the western coast, where phenomena which throw important light on the nature of the relations of the serpentine to the adjacent rocks may be observed. The first is in the neighbourhood of Ogo Dour, and the second east of the Lion Rock, Kynance.

II.
Relation Of Serpentine To Hornblende-schist At Pol Cornick

In his classic ‘Report on the Geology of Devon, Cornwall, and West Somerset,’ De la Beche says (p. 30) :—" It [the hornblendesate] supports the great mass of the Lizard serpentine, with an apparent passage of the one into the other in many places . . . . . In contradiction to this apparent passage, we find a mass of serpentine amid the hornblende-slate between Dranna Point and Porthalla, on the north of the principal mass of serpentine, which has every appearance of having been thrust up among the hornblende-slate, twisting and contorting the laminæ adjoining it in directions which we should consider consistent with the passage of the serpentine in a state of igneous fusion through them." In these sentences De la Beche shows that he had observed facts which apparently contradicted each other, and with characteristic candour he states the two more or less opposed views, leaving the question undetermined.

In 1877 and 1883
Note on a Radiolarian Rock from Fanny Bay, Port Darwin, Australia
Authors: Hinde George Jennings
Published: October 2009

About two years ago, Capt. Moore, of H.M.S. ‘Penguin,’ brought home to this country and forwarded to the Admiralty block of a white rock obtained from the cliffs at Fanny Bay, Port Darwin, in the Northern Territory of the Colony of South Australia. The specimen was forwarded by Capt. W. J. Wharton, F.R.S., the Hydrographer to the Admiralty, to Sir Archibald Geikie, For. Sec. R. S., Director-General of the Geological Survey, who, with Capt. Wharton's consent, kindly allowed me to make a microscopical examination of it, and the results seem of sufficient interest to communicate to the Society.

The rock in question is of a dull-white or yellowish-white tint, in places stained reddish with ferruginous material; it has an earthy aspect, like that of our Lower White Chalk, but it is somewhat harder than chalk, though it can be scratched with the thumb-nail. There are no signs of stratification, and it appears as a fine-grained, homogeneous material. Unlike chalk, however, it gives no reaction either in cold or heated hydrochloric acid. When thoroughly dry it readily breaks up into flakes with uneven surfaces. Though somewhat soft, thin microscopical sections of it can be prepared without much difficulty, and these show a fairly transparent groundmass containing numerous very minute granules and subangular mineral-fragments ranging up to .075 mm in breadth. The groundmass itself is quite negative in polarized light, and appears to be made up of amorphous silica, but the minute grains and angular particles with which it is filled readily
The Pambula Gold-Deposits
Authors: Power Frederick Danvers
Published: October 2009

The Pambula Goldfield is situated in the parish of Yowaka, county of Auckland, in the south-eastern corner of New South Wales, and is about 11 miles north of Twofold Bay.

Most so-called ‘practical’ miners, especially those accustomed to well-defined quartz-reefs, acknowledge that these deposits are quite different from anything they have ever met with, and admit that they do not understand them. This is not surprising, for, if the observer takes a cursory view, without giving due weight to minor details, these lodes do indeed appear different from the general run of auriferous deposits, chiefly owing to the fact that the material filling the ore-chanuels does not differ much in appearance from the enclosing rock (‘ country ’), and is but slightly impregnated with metallic sulphides.

The ore-deposits of Australasia are for the most part confined to certain belts of country, running more or less parallel with the sea-coast and with the main ranges of hills. The rocks which contain the Pambula gold-deposits are no exception to the general rule, their average strike being 12 deg. W. of N. The enclosing rock or ‘country’ is pyrophyllite-schist, interbedded with felsparporphyry, sometimes merging into quartz-porphyry, the whole of which is tilted at a high angle ; near the surface the rocks dip considerably to the east, while deeper down they are almost perpendicular. The planes of cleavage and the planes of bedding of the ‘country’ appear to be coincident.

Examined microscopically, the structure of the schist is lenticular, and this is repeated
On the Jaw of a New Carnivorous Dinosaur from the Oxford Clay of Peterborough
Authors: Lydekker R.
Published: October 2009

I am indebted to my friend Mr. A. N. Leeds, of Eyebury, near Peterborough, for the opportunity of bringing under the notice of the Society a very interesting, although unfortunately imperfect, Dinosaurian jaw, recently obtained from the brick-pits in the Oxford Clay near the town named.

The specimen comprises the anterior and posterior extremities of the left ramus of the mandible, showing the alveoli of the teeth and the cavity for the articulation of the quadrate. The fractured surfaces are fresh, and it is thus evident that the present imperfect condition of the specimen is due to a blow from the pick of the workman by whom it was disinterred. When entire, its total length was probably about 1 foot. The anterior fragment (Pl. XI. figs. 1, 1
a
)comprises the greater portion of the dentary bone, with the symphysis entire; while the hinder moiety (
ibid.
figs. 2, 2
a
) includes the articular, and portions of the angular and surangular elements.

The dentary bone is somewhat roughened and pitted on its external surface, with a broad symphysial channel; while the symphysis itself is oblique, and in life was evidently united by ligament. Superiorly the outer surface is concave from above downwards, while below the concavity it is traversed by a prominent longitudinal ridge, dividing the proper lateral from the inferior aspect. The alveolar margin is characterized by its abrupt deflection near the middle of its length: the deflected portion falling away continuously to the extremity of the shallow symphysis. The whole
On some Palæozoic Ostracoda from Westmoreland
Authors: Jones T. Rupert
Published: October 2009

§1. Introduction

In 1865 the Author determined for Prof. Harkness some fossil Ostracoda which he had obtained from the Lower-Silurian rocks of S.E. Cumberland and N.E. Westmoreland, and subsequently other specimens mentioned by Harkness and Nicholson in 1872. In 1891 Prof. Nicholson and Mr. Marr submitted a series of similar microzoa from the same district; and the Author now endeavours to determine their specific alliances, and revises the list of those previously collected. He has to notice about eleven forms of
Primitia, Beyrichia, Ulrichia, Æchmina
, and
Cytherella
—several of them being closely allied as varieties, but all worthy of study as biological groups, such as have been illustrated from other regions by writers on the Ostracoda, with a view to the exact determination, if possible, of species and genera, of their local and more distant or regional distribution, and of their range in time.

§2. References to Figures and Descriptions of Groups of Mutually-related Ostracoda of Palæozoic Age

1. J.
Barrande
. Syst. Sil. Bohême, vol. i. Supplem. 1872. Various.

2.
Fr. Schmidt
. Mém. Acad. Imp. Sc. St.–Pétersbourg, sér. 7, vol. xxi. 1873,
Leperdiœ; ibid.
vol. xxxi i . 1883,
Leperditiœ
.

3. G.
Reuter
. Zeitschr. Deutsch. geol. Gesellsch. vol. xxxvii. 1885, pp. 621-679, pls. xxv., xxvi.

4. M.
Verworn
.
Ibid
. vol. xxxix. 1887, pp. 27-31, pl. iii.

5. J.
Kiesow
.
Ibid
. vol. xl. 1888, pp. 1-16, pls. i., ii. ; Jahrb. Geol. Landesanst. u. Bergakad. Preuss. 1889, pp. 80-103, pls. xxiii., xxiv.

6. A.
Krause
. Zeitschr. Deutsch. geol. Gesellsch. vol. xli. 1889
On some Palæozoic Ostracoda from the District of Girvan, Ayrshire
Authors: Jones T. Rupert
Published: October 2009

§ 1. Introduction.

This paper aims at the completion of the palæontological account of the Girvan district, so far as the Ostracoda are concerned; and follows up the researches indicated in the 'Monograph of the Silurian Fossils of the Girvan District in Ayrshire,' by Nicholson and Etheridge, Jun., vol. i. 1880.

In about a dozen pieces of the fossiliferous shales, submitted for examination some few years ago, the writer finds nearly thirty specimens (chiefly casts) of
Primitia
,
Beyrichia
,
Ulrichia
,
Sulcuna
, and
Cypridina
, which show interesting gradations of form, not always easy to be defined as specific or even varietal, but valuable as illustrating modifications during the life-history of individuals, thus often leading to permanent characteristics of species and genera. Like those formerly described in Nicholson and Etheridge's' 'Monograph,' the specimens have all been collected by Mrs. Elizabeth Gray of Edinburgh.

Excepting a small cast of a
Beyrichia Kleedeni
, M'Coy, B.
Kloedeni
, var.
scotica
, Jones & Holl, and
Ulrichia Grayce
, Jones, which are of Llandovery age, from the Burn leading to Bargany Pond, all the specimens here described are from the dark-grey Lower-Silurian (Middle-Bala) shales of Whitehouse Bay. See Dr. C. Lapworth's Memoir on 'The Girvan Succession,' Quart. Journ. Geol. Soc.vol. xxxviii. 1882, pl. xxv. fig. 3 (map); fig. 16 at p. 595; and pp. 597, 603, 606, 612, 621, and 661.

The numbers attached to Mrs. Gray's little hand-specimens are here inserted, together with the character of the shale in which the Ostracoda occur, for each species.

§ 2.
Description
On the Occurrence of Boulders and Pebbles from the Glacial Drift in Gravels south of the Thames
Authors: Monckton Horace W.
Published: October 2009

I.
Introduction

In Hertfordshire, Middlesex, and Buckinghamshire the Glacial Drift consists of Boulder Clay and also of extensive sheets of gravel. The reasons for classing this gravel as Glacial Drift are given by Mr. Whitaker in his ‘Geology of London,‘ 1889, vol. i. pp. 299–300. In this gravel we frequently find numerous pebbles or boulders of red quartzites and sandstones, black cherty pebbles, blocks of white quartz; and occasionally we meet with boulders of igneous rock. Now all these materials are characteristic of the Glacial Gravel or Northern Drift, but are practically absent from the Southern Drift, as has been pointed out by Prof. Prestwich. Not only are materials of this sort wanting or very rare in the Southern Drift, but also in the valley-gravels of what I may call the ‘Southern Drift country,‘ in which I include large parts of Kent, Surrey, North Hampshire, and Berkshire. It is true that very rarely boulders of white quartz occur in these gravels, and pebbles of various old rocks may occasionally be found; these last are, however, quite unlike the red quartzite and sandstone-pebbles so common in the Glacial Drift, and probably are derived from Tertiary pebble-beds.

The southern limit of distribution of the Northern Drift materials in hill- and valley-gravels very nearly coincides with the River Thames, at least in the country east of Pangbourne, but not absolutely so, and the object of the present paper is to show where and to what extent the Glacial Gravels or their débris are
On the Plateau-gravel South of Reading
Authors: Shrubsole O. A.
Published: October 2009

The gravel of the Easthampstead-Yateley plateau, to which this paper refers, has already been fully described in the Quarterly Journal of this Society and elsewhere. It is therefore proposed now to submit only a few supplementary observations.

The gravel may be briefly described as consisting principally of rolled and subangular flints. With these is a small proportion of flint-pebbles, with fragments of chert, sandstone, etc., and a few very small quartz-pebbles. The flint-material, excluding the pebbles of flint, has usually a worn and altered appearance (noted already by Dr. Irving), and consists chiefly of nodular flints of small size, the nodules frequently being entire. Internally the flint is usually of a bright brown or amber colour. It is generally understood that these ordinary materials of the gravel have had a local and southern origin. There is a small element, however, which cannot be so readily referred to the same source. The finding of boulders of quartz and a specimen of quartzite at various points on the plateau has been already referred to by Mr. H. W. Monckton.²

I have at different times found several fragments of white veinquartz varying in longest diameter from 2 to 6 inches, the larger specimens being less rolled than the smaller. They were found chiefly in the gravel-pits near Cæsar's Camp (Easthampstead) and at Finchampstead Ridges, lying on the heaps of gravel, in the former case at about 400 feet, and in the latter case at about 330 feet above sea-level. I also found, under