bluuebunny/crossref_metadata_2025 huggingface dataset:
The Marble Beds of Natal
Authors: Draper David
Published: October 2009

I.
Introduction
.—Early explorers in Natal mention the occurrence of marble along the lower course of the Umzimkulu river. Mr. C. L. Griesbach (Quart. Journ. Geol. Soc. vol. xxvii. 1871, p. 56) described the position of this “ crystalline limestone of enormous thickness,” but could not determine its relation to the neightouring rocks. During his visit to the colony, that portion in which the marble is situated was entirely occupied by natives, and covered by dense bush; consequently exploration was difficult. Since then roads have been cut through the country, and numerous farmsteads have been built by the whites on the more fertile tracts of land.

The settlers along the banks of the Umzimkulu have endeavoured to establish an industry in connexion with this marble, several limekilns and a small cement-fact0ry having been erected; and small shipments of the marble are occasionally sent to Durban, for building or statuary purposes. Still more systematic attempts might be made to develop this valuable marble, the only one known to exist in South Africa.

II.
Situation
.—The area occupied by the marble is in the county of Alfred, the southernmost county of the colony of Natal. The Umzimkulu river, rising in the Drakensberg and flowing eastward, enters the Indian Ocean about 30 miles north of the southern boundary of Natal; about 7 miles from its mouth it is joined by the Umzimkuluana river. The marble area occurs in the two rivervalleys, and is about 16 square miles in extent.

III.
Physical Features of the Country
.—Along
On a Collection of Fossils from Madagascar obtained by the Rev. R. Baron
Authors: Newton R. Bullen
Published: October 2009

ntroduction

The fossils contained in this collection were procured from a number of localities in the northern and north-western parts of Madagascar by the Rev. R. Baron, during an extensive journey which he undertook in 1891, as an officer of the London Missionary Society. They may be regarded as supplemental to those that he collected some few years previously in the north-western districts, fossils which were described in 1889 before this Society as representative of Eocene, Cretaceous, and Jurassic rocks.

The present collection, besides comprising organic remains from these different horizons, contains a few terrestrial shells referred to
Achatina panthera, Achatina
like
A. Layardi, Buliminus
(
Rachis
)
punctatus
, and
Pomatias
(
Tropidophora
)
virgata
. These were found in a Quaternary deposit capping the hill of Ambohimarina at a height of over 1400 feet above sea-level, and they are known to exist on the island at the present day. The Tertiary (Eocene) specimens consist entirely of foraminifera. They were obtained from the island of Antanifaly (N. W. coast) and have been determined as
Nummulites
allied to
N. Bellardii, N. perforata, N. complanata
, and
Assilina spira
; species which have a wide distribution, though mostly confined to South European countries, Egypt, West Asian localities, and India.

The Cretaceous fauna contributes one specimen of
Lampadaster Grandidieri
?, found in a red limestone, immediately beneath the subsoil of Ambohimarina Hill, which also contains
Frondicularia
, etc., and dense masses of
Globigerinæ
; while examples of
Belemnites pistilliformis
prove the presence of Neocomian rocks north of Andranosamonta village.

Among Jurassic fossils a
On the Eastern Limits of the Yorkshire and Derbyshire or Midland Coalfield
Authors: Gresley W. S.
Published: October 2009

The Author attempts to throw light on the question of the easterly extension of the Yorkshire, Derbyshire, and Nottinghamshire coalfield beneath the newer rocks. He notices the general trend of the strata, the sizes of other British coalfields, the question of the origin of mountains, stratigraphical considerations, and the faults of the North of England. His object is rather to suggest what he believes to be novel ways of treating the subject than of reaching conclusions or locating limits.

The Author calls attention to the previously established fact that an anticlinal exists in the Secondary rocks near the southern end of the Lincolnshire Wolds. The existence of this anticlinal has been demonstrated by Mr. A. J. Jukes-Browne (Quart. Journ. Geol. Soc. vol. xlix. 1893, p. 467). Following the reasoning of M. Marcel Bertrand, he infers that an anticlinal in the Carboniferous rocks probably underlies this, and that the easterly termination of productive Coal Measures under Lincolnshire may be formed by this anticlinal.
Carrock Fell: a Study in the Variation of Igneous Rock-Masses.—Part II. The Carrock Fell Granophyre. Part III. The Grainsgill Greisen
Authors: Harker Alfred
Published: October 2009

9. I
ntroduction
.

I
n
a former paper I have given a general sketch of the geology T of the Carrock Fell district, and discussed the remarkable variations observed in the gabbro which is there exposed. The present communication deals with the granophyre, which is closely associated with that gabbro, and with another interesting acid rock, not far distant, but belonging to a different group of intrusions.

The granophyre occurs in several distinct masses, which, from their general eye-shaped outcrop and parallelism of strike with the adjacent rocks, must be regarded as laccolitic intrusions (see sketchmap, F1. IV.). The similarity of these neighbouring masses justifies us in considering them as a connected group. The one most easily studied is that which builds Carrock Fell itself, and extends westward in a tongue nearly as far as Round Knott. The exposures about: Rae Crags, farther north-west, probably belong to a mass distinct from the preceding, separated from it by diabase, and faulted ou the north against the Eycott Hill lavas and the Drygill Shales. Granophyre is seen at certain points o~ the moorland of which Great Lingy is the centre: if these outcrops belong to one connected mass, its extent from Roughten Gill eastward must be nearly 2 miles. There are smaller intrusions in Arm o' Grain and other gills, but we may confine our attention chiefly to the mass first indicated, which is well exposed about Carrock Fell and the Pike and in the cliffs known as the Scurth.

The question
The Whitehaven Sandstone Series
Authors: Kendall J. D.
Published: October 2009

The Whitehaven Sandstone, with its associated shales, is a purple-grey deposit sometimes having a thickness of 500 or 600 feet. The Author gives details of a large number of sections of the series, which also contains thin coal-seams and occasionally
Spirorbis
-limestone.

He combats the view that it is stained Middle Coal Measure deposit, and gives his reasons for believing that it rests unconformably upon the Middle Coal Measures, and also that it has not received its colour by abstraction of colouring-matter from the Permian beds, but that the colour actually belongs to the deposit. He describes sections which lead him to suppose that the deposit has a wider distribution over the Cumbrian district than is allowed by previous writers.
A new Ossiferous Fissure in Creswell Crags
Authors: Duckworth W. L. H. , Swainson F. E.
Published: October 2009

The fissure explored by the Authors is about 30 feet above the level of the artificial lake at Creswell Crags. At the top occurred a white earth (with human and other remains), passing down into a red sand with remains of fox, badger, roe-deer, and other mammals. Beneath the latter deposit, and separated from it by a fairly sharp line of demarcation, came the cave-earth proper, with Palæolithic implements and bones of
Rhinoceros tichorhinus, Bison priscus, Ursus spelæus, Hyæna crocuta
var.
spelæa
, and
Cervus tarandus
.

The Authors suppose that this cave-earth is derived from an older deposit and has been transported to its present place by water, though there is evidence that the transport has been from no great distance. Consequently they followed the fissure inwards, until brought to a stop by a mass of travertine, which they penetrated with a small hole. They hope to explore the fissure beyond this travertine on a future occasion.
A Comparison of the Permian freshwater Lamellibranchiata from Russia with those from the Karoo System of South Africa
Authors: Amalitsky Wladimir
Published: October 2009

S
ome
palæontologists, such as Owen (1876), Twelvetrees (1880), Trautschold (1884), and others, have pointed out the resemblance which exists between the reptilian fauna of Perm, in Russia, and that of the Karoo formation of South Africa. This similarity was based on the fact that the reptiles of Perm described as
Rhopalodon
, Fisch.,
Brithopus
, Kut.,
Orthopus
, Kut.,
Deuterosaurus
, Eichw.,
Cliorhizodon
, Tul.,
Oudenodon
, Traut., and others were referred to the Theriodontia, a group represented in the Karoo Series of South Africa. The Russian Permian reptiles referred to have been recently studied by Seeley, who has come to the conclusion that they are closely allied to the South African types, but cannot be placed in the same subordinate groups. This author considers them as a new group, Deuterosauria, exhibiting a strong affinity with both the Placodontia and Theriodontia.

In 1892, when describing the lamellibranchiate fauna from the Oka-Volga basin, I pointed out that the typical shells called
Palæomutela
from these deposits were also known from the Karoo Series of South and Central Africa, and had been described as
Iridina
by Daniel Sharpe and Prof. T. Rupert Jones. At that time, not being in possession of the original forms from the Karoo Series, I, of course, could answer only for the identity of the genus, though, judging from the description given by Daniel Sharpe and Rupert Jones, it was easy to observe that they possessed characters corresponding to those which I referred to the group of
Palæomutela Inostranzewi
. I then expressed the opinion that,
The Physical Features and Geology of Mauritius
Authors: de Haga Haig H.
Published: October 2009

I. P
hysical
F
eatures
.

T
he
Island of Mauritius is the centre of a line of three—Réunion, Mauritius, and Rodriguez—some hundreds of miles apart ; they are all volcanic, and in reality quite unconnected, except in so far as they are on a line of volcanic action. Mauritius is about 40 miles long and 27 miles broad, and it consists essentially of a mass of volcanic d6bris thrown up from craters now extinct. A central ridge, which is the main watershed of the island, and in which are situated all the more recent craters, commences at the south, where it has an elevation of about 2000 feet, and runs northwards, gradually curving to north-east. The gentle slopes on each side are stopped, round the greater part of the circumference, by ranges of mountains up to nearly 3000 feet in height, so thin and steep as to resemble walls. From the outer precipices of these, comparatively level plains of variable width stretch to the sea. There are three wide gaps in these mountains, through which the slopes from the main watershed fall gently to the sea. The northern part of the island—the pointed end of the pear—is cut off from the rest by these mountain-walls, but the general direction of the watershed continues across it at a much lower level, and is even prolonged under water by a bank extending 14 or 15 miles before it sinks to 100 fathoms below the sea : the general depth of the sea-bottom around being about
The Shelly Clays and Gravels of Aberdeenshire, considered in Relation to the Question of Submergence
Authors: Bell Dugald
Published: October 2009

The high-level shelly gravels and clays of Aberdeenshire were described in some detail by Mr. T. F. Jamieson, of Ellon, in two valuable papers read to this Society in March 1882. They have also been treated of at some length by the Geological Survey of Scotland, in their published memoir relating to the district. As these deposits have been frequently, and quite recently, referred to as proving a submergence in Scotland during Glacial times, to the extent of 500 feet or upwards, I would ask leave briefly to review the facts, for the purpose of showing that they do not lead to or warrant such a conclusion.

1. There are, first, certain beds or undulating ridges of sand and gravel which, according to Mr. Jamieson, contain fragments of shells of Crag species. These extend along the sea-shore and for some distance inland, a few miles north of the river Ethan, and are found up to a height of 225 feet above the sea, but chiefly between 100 and 200 feet. They rest on the grey Boulder Clay of the district, which is formed of the ddbris of the gneiss, granite, and mica-schist rocks prevailing there ; but they are different from it, containing many pieces of yellow limestone and calcareous shale belonging to some Secondary formation not found in situ in Aberdeenshire. ‘ The shelly material occurs generally in the form of fine pounded ddbris and small worn crumbs, with here and there a larger bit, generally a hinge.’ The
The Stirling Dolerite
Authors: Monckton Horace W.
Published: October 2009

A glance at the Geological Map of Scotland will show that Stirling Castle stands on one end of a very large mass of intrusive igneous rock. Its continuity has been broken by a long east-and-west fault a little south of St. Ninian's, but if we ignore this break the mass of igneous rock has a length of about 8 miles and a width varying from about ¼ to nearly 2 miles.

The rock has been intruded into strata of the lower part of the Carboniferous Limestone Series, and it forms not one, but a number of irregularly-shaped intrusive masses or group of sills, all more or less connected with one another. The hardness of the igneous rock has in many places been sufficient to arrest denudation, and the result is a number of crags, which often resemble Salisbury Craigs, near Edinburgh. Sometimes these crags face the north or north-west, as in the case of Stirling Castle and King's Park, but in other cases they face in a different direction, at Sauchieburn, for instance, the north-east.

As I shall show from the character of the rock, we can have little doubt that the mass of the Abbey Craig north of the river Forth is connected underground with the Stirling Castle rock, from which it is only divided by alluvium, and there is reason to think that the igneous rocks of Cowden ]~ill and of the hills around Kilsyth are also outlying portions of the Stirling rock. It is not meant that
Ice-plough Furrows of a Glacial Period
Authors: Gresley W. S.
Published: October 2009

The furrows described in the paper occur in the Coal-Measures of North-western Leicestershire. The Author considers that they were formed about the time of the Glacial Period by floating ice.
Geological Notes of a Journey round the Coast of Norway and into Northern Russia
Authors: Boulger G. S.
Published: October 2009

The Author accompanied the Jackson-Harmsworth Polar Expedition as far as Archangel, and returned by way of the River Dvina. His observations relate mainly to four points:—the origin of the foliation of the Norwegian gneiss; the question of raised beaches on the North-western coast of Norway; the boulders and boulder-formation of Northern Russia; and the Trias of the Dvina valley.

Between Christiansund and Tromsö the Author was struck with the wide-sweeping folds of the foliation-planes of the gneissose rocks, which appeared to him more readily explicable on a theory of dynamo-metamorphism of rocks originally in part igneous, than by any process of diagenesis. He notes that the terraces observed in the transverse fjords would be perfectly explained by the formation of ice-dammed lakes, though the terraces of the Gulf of Onega seemed less dubious raised beaches than those of the North-west of Norway. He confirms the views of previous writers that many of the boulders of the boulder-formation of Northern Russia are of Scandinavian origin. The beds on the Dvina consist of sands and loams, often coloured red, with bands of alabaster and anhydrite. The strata are horizontal or inclined at a low angle. North of Ustyug Veliki the strata are marked as Permian on the Russian maps, and those to the south as Trias, but the Author saw no perceptible break in the succession.
On the Shingle-beds of Eastern East Anglia
Authors: Howorth Henry H.
Published: October 2009

These well-known beds have been variously named the Westleton Beds, the Bure Valley Beds, and Pebbly Beds. Their centre of distribution and focus, however, is near Southwold, and they might well have been called the Southwold Beds. The following remarks are limited entirely to the actual beds of pebbles as they are displayed in Eastern Norfolk and Suffolk, where they have been studied and described by Prestwich, Whitaker, and others.

First a few words about the recent strand. This consists of shingle precisely like that in the cliff-sections. A fact about it which has not apparently been hitherto noted is that this shingle on the beach travels in and out, not with the wind, but against the wind. Thus during easterly gales the whole strand is free from stones, while in westerly winds the pebbles are again piled up. So far as we know, there is no shingle like this anywhere on the bed of the German Ocean. Wherever it came from, therefore, it cannot have come from the east. As a matter of fact, it is obviously the product of the disintegration of the cliffs.

The cliffs on this coast are really the truncated ends of a series of promontories projecting from the main plateau of the county and fringed round by low land. It is from these truncated promontories, which are capped with similar pebbles, and from these alone, that the shingle on the beach has been derived, and not from a general erosion of the coast.

The
On the Occurrence of
Spirorbis
-limestone and thin Coals in the so-called Permian Rocks of Wyre Forest; with Considerations as to the Systematic Position of the ‘Permians’ of Salopian Type
Authors: Cantrill T. Crosbee
Published: October 2009

I. I
ntroduction
.

T
he
occurrence of a band of
Spirorbis
-limestone associated with a thin coal-seam in red rocks which have hitherto been regarded as Permian in the district of Wyre Forest and Enville cannot but affect our ideas as to the systematic relationships of these beds, and may also have some influence on the mining prospects of that virgin strip of red ground which, narrowing from 14 miles broad at Madeley and Wolverhampbon to 6 between Compton and Stoutbridge, separabes the coalfields of Coalbrookdale and Wyre Forest on the west from that of South Statfordshire on the east.

This red ground Consists of the ‘ Permian ’ rocks and all the members of the Trias. Crossing from west to east we pass successively from Coal Measures at Madeley on to ‘ Permian ’ [e
1
of the Geological Survey map],Lower, Middle, and Upper Bunter, Keuper Sandstone, and Marl, till we reach Codsall, when we again pass over the same series in inverse order—omitffng the Lower Bunter—fill we reach the Coal District of Wolverhampton.

At the base of the Trias in this district there seems to be a marked unconformity, for at Bridgenorth the base of the Lower Bunter [f
1
] is represented on the Geological Survey map, 61 S.E.,as approaching the base of the Permian, whereas between Enville and Claverley it rests on the highest beds of the Permian ; and Prof. Hull estimates the overlap as equivalent to about 1000 feet of strata. The horizontal extent of the overlap appears to be
The Crush-Conglomerates of the Isle of Man
Authors: Lamplugh G. W.
Published: October 2009

Concluding Summary

The chief points brought forward in this paper may be epitomized as follows:—

(i)

In the Skiddaw Slates of the Isle of Man strata of considerable thickness have been locally broken up under shear-pressure, and re-arranged in the form of a crush-conglomerate or friction-breccia.

(ii)

This crush-conglomerate occurs in definite bands striking with the surrounding rocks, sometimes continuous for many miles.

(iii)

The brecciation has usually taken place along the junction of arenaceous with argillaceous strata, and has chiefly affected the passage-beds between such rocks.

(iv)

The formation of the crush-conglomerate has occupied one stage only in a series of earth-movements which had previously folded the rocks and afterwards impressed a shear-cleavage upon them.

(v)

There is reason to believe that the crush-conglomerate marks a definite stratigraphical horizon; and that it was originally dispersed in a rude zone which afterwards suffered contortion.
Appendix.—Petrographical Notes on the ‘Crush-Conglomerates’ of the Isle of Man
Authors: Watts W. W.
Published: October 2009

As most of the rocks collected in the Isle of Man by Mr. Lamplugh have passed through my hands, it has fallen to my lot to describe the specimens of ‘crush-conglomerate’ for him. At his request I add to his paper a few notes on the macroscopic and microscopic characters of selected examples of these specimens. The microscopic observations appear to confirm, in all essential points, the deductions drawn by him from the field-evidence. They even enable us to go a little further on some points:—to trace the disintegration of the grit-bands; to watch the process of ‘pebble’-making on a small scale; to see the breaking-up of the ‘pebbles’ themselves into miniature ‘crush-conglomerates’; to follow the erosion of the ‘pebbles’ into single grit-particles involved in slate; and, finally, to state the amount of secondary change which the rocks have undergone.

It will be convenient to divide these notes under the following heads:—

(1)

Sedimentary rocks outside the great area of movement and crush.

(2)

The ‘crush-conglomerates’: (
a
) as a whole; (
b
) their contained fragments.

(3)

The dykes penetrating the conglomerate.

(4)

Metamorphism of the ‘crush-conglomerate.’

(1) The Sedimentary Rocks.

It is very rare to find in the Skiddaw Series of the island any sedimentary rocks, except those of very coarse grain, which have not been crushed and sheared by earth-movements.Outside the principal zone of crush and brecciation the rocks still possess their original dastie structure, but they begin
On the Occurrence of Radiolaria in Chalk
Authors: Hill W. , Jukes-Browne A. J.
Published: October 2009

The rarity of radiolaria in rocks of Upper Cretaceous age is a remarkable fact, and one for which it is not easy to account, seeing that they are not uncommon in Lower Cretaceous rocks on the Continent, and that they have been found in beds of Jurassic age in France, Hanover, and Bavaria. One would moreover have expected the physical conditions of the Upper Cretaceous period to have been more favourable to their existence than those of Lower Cretaceous or Jurassic times. It will be seen, from the descriptions which follow, that one cause of their rarity is undoubtedly the facility with which the siliceous skeletons of
Polycystina
disappear, when they are embedded in rocks which contain a large proportion of carbonate of lime.

Our knowledge of Upper Cretaceous radiolaria comes chiefly from Germany. In 1876 Prof. Zittel described six species, occurring in a Greensand of Senonian age in Westphalia and Brunswick.

In 1888 Dr. Rüst described some well-preserved forms which he had detected in phosphatic nodules from the Gault of Saxony, Hanover, and Southern France, and in material filling the body-chambers of ammonites from the same formation.

He also described
Dictyomitra anglica
from flints in the Upper Chalk of England (
op. cit.
p. 211 & pl. xxviii. fig. 16) and
Dictyospyris chlamydea
, same occurrence (
op. cit.
p. 204).

Besides those in the English flints mentioned by Riist there are only two records of the occurrence of radiolaria in English Cretaceous deposits.Prof. W. J. Sollas, in 1873, describing the coprolites
Additional Notes on the Tarns of Lakeland
Authors: Marr J. E.
Published: October 2009

The following notes form a supplement to a paper on ‘The Tarns of Lakeland’ read before the Society in 1894. I have had the opportunity during the present summer of devoting more time to the study of Watendlath Tarn, and have examined three other tarns of some interest.

(a) Watendlath Tarn

In my former paper, I stated that in the case of Watendlath Tarn ‘a great mass of drift is plastered against the east side of the valley, and may have filled the old valley.’ I have since ascertained that there is no old valley there, but that the solid rock runs all round the northern, eastern, and southern ends of the tarn: I furthermore stated that ‘ on mountaining some way above the tarn I saw indications of the possible existence of a moraine–filled depression’ on the western side. I have now examined this depression and satisfied myself that beneath it lies buried the old valley, the stream from which ran down into Borrowdale near Rosthwaite—that is, anbout 3 miles south of the present junction of the Watendlath valley with Rosthwaite, near Lowdore. This moraine–filled depression runs close to the path from Rosthwaite to Watendalth Tarn. The watershed here is about 200 feet deep, it requires a barrier of drift over 250 feet in thickness to account for the tarn; but, as the valley is evidently a narrow one, and its course lay at right angles to the direction of the ice, the occurence of this somewhat thick mass
The Serpentine, Gneissoid, and Hornblende Rocks of the Lizard District
Authors: Bonney T. G.
Published: October 2009

I.
Introductory

In 1891 a communication on the rocks of the Lizard fron General McMahon and myself was honoured with a place in the Society's Journal. As therein stated, we were of opinion, at the time of our visit to Cornwall (August, 1890), that to regard the banded members of the ‘the hornblendic group’ as stratified basic tuffs, subsequently metamorpohosed, was ‘ the better working hypothesos.’ But, even in that interval, as will be seen by a note appended to the paper, some doubts as to the correctness of this conclusion had already arisen in my mind, for a visit to Sark in the spring of 1891 had suggested explanations of certain difficulties which hitherto had seemed insuperable in an alternative hypothesis. Accordingly I became anxious to see how the old puzzles looked in the new light, and besides this a very important paper by my friends Messrs. Howard Fox and J.J. H. Teall, subsequently published in this Journal, made it a necessity for me to study the sections of which they had given so lucid a description. for, if their interpretation of these were correct, the geology of the crystalline rocks of the Lizard peninsula would be thrown (as it seemed to me) into hopeless confusion. The authors, indeed, restricted their conclusions to the sections which they had described; but it appeared to me, for reasons which will be given hereafter, that no such limitation was possible, and that if they were right I must have misinterpreted the evidence
The Mollusca of the Chalk Rock: Part I.
Authors: Woods Henry
Published: October 2009

The Chalk Rock is a bed of hard, usually cream–coloured limestone, occurring at the top of the Middle Chalk; it succeeds the zone of
Holaster planus
and is followed by the zone of
Micraster cor–testudinarium
. Noticeable features in the bed are the presence of grains of glauconite and numerous green–coated nodules of phosphatic chalk. Under the microscope it is characterized by the abundance of foraminifera, especially
Globigerina
, and by numerous fragments of the tests of mollusks and echinoids; the bright green grains of glauconite are also conspicuous. The insoluble residue, obtained by treating with hydrochloric acid, was found by Dr. W. F. Hume to consist mainly of quartz and glauconite; augite, hornblende, and tourmaline occur very rarely. Frequently the Chalk Rock is not hard throughout, but contains irregular cavities filled with soft mealy chalk or with red sandy clay. Analyses of the rock have been made by M. Duvillier, Dr. Frankland, Mr. C. W. Meanwell and Mr. P. G. Sandford, and they show from ·20 to ·713 per cent. of phosphoric acid—a large amount compared with that usually found in chalk.

The best development of the Chalk Rock occurs in Berkshire, Oxfordshire, Buckinghamshire, and Bedfordshire; its average thickness is about 3 feet. In the Isle of Wight it varies from 8 inches to 2 feet 7 inches. In Dorset and Devon it consists of a layer of green–coated nodules only.Near Winchester (at Twyford) the zone can be traced by means of the characteristics fossils, but the rock is not hard
On the Speeton Series in Yorkshire and Lincolnshire
Authors: Lamplugh G. W.
Published: October 2009

I. Introduction.

In describing the clays which underie the Chalk at Speeton on the Yorkshire coast in a paper communicated to this Society in 1889, I attempted to show the necessity for a fresh classification of these deposits.Further investigation of this section has fully confirmed the views then advanced. It has also indicated the desirability of a corresponding revision of the inland exposures of the rocks of the same age in Yorkshire and Lincolnshire, since it is only by means of the knowledge of the full sequence to be acquired on the coast-section that the true relationship of the limited and isolated exposures of the interior can be unravelled.

Using such opportunities as have at intervals occurred, I have therefore more or less closely examined the base of the Chalk escarpment throughout its whole length in Yorkshire and Lincoln-shire, and desire in this paper to put on record the result of my investigation. It will be shown that the divisions proposed for the Speeton section are readily applicable to the inland exposures, and indeed afford the most convenient and natural means of palæ-ontological classification, albeit some modification of the systems, usually applied is thereby required.

It may be well at once to state that, while my chief aim will be to establish the correlation of the deposits by means of their palæontology, no attempt will, for the present, be made to carry the palæontological research further than is necessary for this purpose. Hence the fossils dealt with herein will only
On some Podophthalmatous Crustacea from the Cretaceous Formation of Vancouver and Queen Charlotte Islands
Authors: Woodward Henry
Published: October 2009

Some time since I received from my friend Mr. J. F. Whiteaves, F.G.S., Palæontologist to the Geological Survey of Canada, several interesting crustaceans from the Cretaceous coal-bearing formation of Vancouver and Queen Charlotte Islands, and, as they offer a close affinity with forms from our own Gault and Greensand, they are deserving of special notice.

The existence of Cretaceous strata in Canada has long been known, and the coal–fields of Nanaimo and Comox on Vancouver Island have been correlated with this formation as well as those of Queen Charlotte Island and Alberta, eastward of the Rocky Mountains.

Mr. F. B. Meek in 1857 gave a description of new organic remains from the Cretaceous of Vancouver Island, including
Baculites ovatus
? Say;
Ammonites (Scaphites) ramosus, A. Newberryanus, Dentalium nanaimoensis, Thracia(?) occidentalis, Thr.(9) subtruncata, Trigonia Evansana, Pholadomya subelongata, Ph, (Goniomya) borealis, Cardium scitulum, Area vancouverensis. A, (Cucullæa) æquilateralis, and Nucula Traskana
. Dr. B. F. Shumard in 1858 added
Inoceramus vancouverensis, Pinna calamitoides
, and
Pyrula glabra
to the Nanaimo fauna.

In Prof. H. Y. Hind's ‘Report on the .Assiniboine and Saskatchewan Expedition’ (1859) further lists of fossils are given, 13 in number, all referred to Cretaceous forms, namely

In 1861 Dr. (now Sir) James Hector instituted a comparison between the strata east of the Rocky Mountain with those of Vancouver Island (Capt. Palliser's Exploring Expedition, 1857–60).The list of Cretaceous fossils contributed by Mr. Etheridge from east of the Rocky Mountains comprised

Inoceramus Crippsii
(Roemer) and
Baculities compressus
(Say) are stated to be common to
On the Morte Slates, and Associated Beds, in North Devon and West Somerset.—Part I
Authors: Hicks Henry
Published: October 2009

Hitherto the Morte Slates have received but scant attention from geologists, owing to the fact that in all text–books, and in geological papers on North Devon, they have always been referred to as unfossiliferous; and all that was known with regard to them up to the year 1887 is well summarized in the following paragraph taken from the second edition of Mr. H. B. Woodward's well–known work,‘The Geology of England and Wales’ p. 127:—‘This division, termed the Morte Slates by the Rev. D. Williams, derives its name from Morte Point, on the north–west coast of Devon. The term Mortehoe Group, from the village of that name, was used by John Phillips. The Morte Slates, or “grey slates,” comprise pale greenish–grey and silvery grey glossy slates, much veined with quartz, and having a thickness estimated at from 3000 to 4000 feet. No fossils have been found; nor have any limestone–bands been recognized in them. The beds rest on the Ilfracombe Beds at Lee Bay, and the subdivisions which can be traced are noted by Mr. Etheridge (in ascending order) as the Lee, Rockham Bay, and Morthoe Beds. The Morte Slates pass downwards into the Ilfracombe Beds, and in Mr. Ussher's opinion they are simply an upper unfossiliferous portion of this lower division, since it is impossible to fix any definite boundary between them. Simonsbath is situated in the valley of the Barle, between the Ilfracombe and Morte Beds.Eastwards they extend to near Wiveliscombe, where they are exposed at the Oakhampton Slate
Observations on the Geology of the Nile Valley, and on the Evidence of the Greater Volume of the River at a Former Period
Authors: Hull Edward
Published: October 2009

1. Introductory.

The evidence in favour of the view that the Nile was at one period a river of vastly greater volume than at the present day is so remarkable that it has forced itself on the attention of several writers, amongst whom maybe specially mentioned the late Prof. Leith Adams,.Prof. Zittel, and Capt. Lyons; and to the statements coming from such competent observers I should hardly have thought it necessary to add any of my own, were it not that I find from personal intercourse that geographers have failed as yet to grasp the full significance of the phenomena bearing on the subject and described by the above–named authors. When about to leave for a recent visit to the Nile Valley, I wrote to Prof. (now Sir) Joseph Prestwich, enquiring whether he thought there were any problems to which a travelling geologist might give attention with some prospect of enlarging our knowledge of the physical conditions of that remarkable line of country, and in reply he recommended me to pay special attention to the terraces. This advice I endeavoured to keep before my mind during my ascent as far as the First Cataract and the return journey; and I venture to lay before the Society the impressions that I then received, and the conclusions that I have drawn from them regarding the volume and dimensions of the river at a prehistoric period. But, before entering upon this special subject, I wish to note a few points connected with the
On certain Granophyres, modified by the Incorporation of Gabbro–Fragments, in Strath Skye
Authors: Harker Alfred
Published: October 2009

The district of Strath in Skye, which has so often formed the subject of geological description, has been assigned to me to be mapped in detail for the Geological Survey; and while engaged in this duty, during the past summer and a portion of the autumn, I had occasion to study the complex series of eruptive rocks which extends from Loch Slapin on the west to the Sound of Scalpay and Broadford Bay on the east. Among the features of interest connected with these igneous rocks, special importance attaches to their relations one to another, and this subject has received due attention. The full details will be fitly deferred until the appearance of the official Memoirs; but, with the sanction of the Director-General, I now present to the Society the following brief account of certain minor intrusions of granophyre illustrating a peculiarity which, I believe, has not yet received notice.

The granophyres of Skye have been described, as a whole, by Maccullocch, Oeynhausen and von Dechen, J.D. Forbes, Sir Archibald Geiki, Prof. Judd. Despite mineralogical and textural variations, these rocks have a general community of characters, which they share also with rocks of various ages in other regions. The examples to be described, however, present quite exceptional features, which seem to be worthy of examination. They form five distinct intrusions lyinh north and west of Loch Kilchrist and 2 or 3 miles south–west of Broadford (see Map). At this locality occurs a large tract of massive volcanic agglomerate, which has
The Fauna, of the Keisley Limestone.–Part I
Authors: Reed F. R. Cowper
Published: October 2009

During a recent rearrangement of the fossils from this limestone in the Woodwardian Museum my interest was especially aroused by the number of peculiar and unnamed specimens amongst them; and I was thus led to examine them with particular care, and subsequently to visit Keisley myself and collect more in the field, as well as to inspect Prof. Harkness's collection at Carlisle, and the specimens in some small private collections. The following descriptions have therefore been based on the examination of as large an amount of material as was available. Prof. Harkness's collection at Carlisle and that of Prof. Nicholson and Mr. Marr at Cambridge are those upon which the well-known lists of Keisley Limestone fossils have been founded; the last list was published by Prof. Nicholson and Mr. Marr in 1891.

By carefully removing the matrix I have been able to bring out many minute characters previously invisible, and have also discovered several entirely new species, which make an important addition to our knowledge of the bed.

Many thanks are due to Mr. Marr, Prof. Nicholson, Mr. Goodchild, Chancellor Ferguson, of Carlisle, Mr. E. T. Newton, and others for help and information.

In this first past of my communication the tribolites alone are dealt with, being the largest and most characteristics section of the fauna. In the second and concluding part the rest of the fossils will be described, and the general relations of the fauna discussed.

Crustacea
—
Trilobita

A list of fossils from the Keisley Limestone was published in
Descriptions of new Fossils from the Carboniferous Limestone. I. On Pemmatites constipatus, sp. nov., a Lithistid Sponge. II. On Palæacis humilis, sp. nov., a new Perforate Coral, with Remarks on the Genus. III. On the Jaw-apparatus of an Annelid, Eunicites Reidiæ, sp. nov.
Authors: Hinde George Jennings
Published: October 2009

I. On Pemmatities Constipatus, SP. Nov., A Lithistid Sponge from the Yordale Beds of Yorkshire. (Pl. XXII. figs. 1. 1
a-m
.)

Although the thick beds of chert in the Yoredale Series of North–west Yorkshire are largely composed of the remains of siliceous sponges, it is a matter of extreme rarity to meet with an entire specimen of these orgainisms, and hitherto one has had to be content with describing the detached spicules of various forms with which the beds are crowded. The discovery therefore by Mr. J. Rhodes of a fairly complete sponge in this series of beds is, in itself, of some interest,a nd still more when the sponge proves on examination to belong to the genus
Pemmatites
, Dunikowski, a genus which, up to the present, has been known only from the Permo–Carboniferous strata of Spitzbergen.

The sponge in question, of which only a single specimen has, as yet, been found, is discoidal, oval in outline, having both upper and under surfaces nearly equally convex, and the margins comparatively sharp. There are no indiactions of a point of attachment on the underside , nor any traces of a cloacal funnel or depression on the upper. It is 63 mm. in length, 48 mm. in width,and 22 mm. in thickness.

The canal system is very faintly shown; but on the convex upper surface there can be traced canal–apertures, about 0·5 mm. in width, disposed in rows extending from near the centre to the margins (Pl. XXII. fig. 1). These appear
On an Alpine Nickel-bearing Serpentine, with Fulgurites
Authors: Aston E. , Bonney T. G.
Published: October 2009

The rocky peak of the Riffelhorn (9616 feet), well known to all who have visited Zermatt and the Gornergrat, forms part of a large mass of serpentine which seems to vary slightly in composition and is generally more or less schistose, becoming in places quite slaty—the effect of pressure. On the summit of this peak the compass, as is well known, exhibits the most extraordinary variations, and the rocks appear to be not seldom struck by lightning. Specimens exhibiting fulgurites were collected on it by both Prof. W. Ramsay and Mr. J. Eccles in 1890, the examination of which has led to ,some, interesting results.

The geologist, in working over different parts of. this large mass of serpentine, observes that, where the original structure is not obscured by subsequent pressure, the rock is not quite uniform in character—one variety being an ordinary dark green bastite-serpen-tine (sometimes also containing augite), the other being a little tougher and harder under the hammer and slightly rougher when handled; in short, it is not quite so normal a serpentine as is the other variety. Of this harder kind the upper part (at any rate) of the Riffelhorn peak is composed.

It will be convenient to speak of the microscopic structure and chemical composition of the rock before describing the effects of the lightning, though the latter was the reason that induced Prof. Ram say to ask the present authors to investigate the former questions.

Slices for microscopic examination were prepared from
Contributions to the Stratigraphy and Palæontology of the Globigerina-limestones of the Maltese Islands
Authors: Cooke J. H.
Published: October 2009

A Bibliography of the
Globigerina
–limestones is followed by some remarks on the physical features and general distribution of the strata. The limestones are divided into nine subdivisions, lettered A to I, the former being uppermost. Four seams of phosphatic nodules form the subdivisions B, D, G, and I, and local nodule–bands also occur in E. The subdivision G serves as a line of demarcation between the Langhian Series (Miocene) and the Aquitanian (Oligocene). Details of the lithological and palæontological characters of the various subdivisions are given, and the Author concludes that I and the lower part of H were laid down on a sinking sea–floor, in about 300 fathoms of water; that the upper part of H and G, F, E, D, composed to a large extent of
Globigerina
and other pelagic organisms, were probably deposited in about 1000 fathoms; while C, B, and A were probably laid down, like I and the lower part of H, in about 300 fathoms of water.
On a Phosphatic Chalk with Holaster planus at Lewes
Authors: Strahan A.
Published: October 2009

In 1891 I described before this Society a phosphatic chalk which occurred near the top of the Upper Chalk of Taplow, and resembled the deposits long known and worked in Belgium and the North of France, but not up to that time recognized in this country. Up to the present, in spite of much searching, no other occurrence of this rock has been recorded in England, but during the summer of 1895 Mr. John Rhodes, fossil collector to the Geological Survey, while engaged in collecting from the great chalk-pits near Lewes, noticed a thin band bearing a strong resemblance to the Taplow phosphatic chalk. At the request of the Director-General I visited the spot ,and made the following notes.

The pit, which is marked on the 6–inch and 1–inch (new series) Ordinance maps as the Southerham Pit, lies on the south–western side of the high downs of Upper Chalk which overlook Lewes from the east. A somewhat marked syncline traverses the central part of these hills in an east–and–west direction. Thus Lewes, situated nearly on the synclinal axis, stands on Upper Chalk, but both to the north and south of the Downs the Middle and Lower Chalk emerge with southerly and northerly dips respectively. The Southerham Pit extends from the Middle to high up in the Upper Chalk, but the workings in the Middle Chalk have been abandoned and are partly obscured. A small bank, however, at the eastern end of the long line of limekilns affords a good view
Discovery of Mammalian Remains in the Old River-gravels of the Derwent near Derby. —Part I.
Authors: Arnold-Bemrose H. H.
Published: October 2009

These remains were discovered under the yard of the Crown Inn at Allenton, not quite 3 miles south of Derby. In March, 1895, Messrs. Offiler & Co. were sinking a well there for drinking-water. When it was partly bricked in, a strong unpleasant smell was noticed, several large bones were discovered, and the well was, in consequence, abandoned. The water rose very rapidly, and only twenty-one bones or fragments were taken out. These included the left femur of an artiodactyle, several vertebræ or portions of vertebræ, and fragments of ribs. The writers obtained them from Messrs. Offiler & Co., and after examination decided to excavate for the remainder. The funds necessary to defray the expenses were readily obtained from a few local gentlemen, on condition that the bones should be finally placed in the Borough Museum. The work was commenced on April 8th and entrusted to Mr. Durant, builder. During the day a hole, 8 x 6 feet, was dug through the clay, and the water rose in it to within 6 feet of the surface. On the second day the hole was deepened through the clay and sand to the top of the gravel (9 feet 8 inches below the surface). One complete bone and twelve small pieces, probably from the head, were obtained.

On the third day the clay was tunnelled on the eastern and northern sides, the total area excavated at the bottom being about 11 by 9 feet. The tunnelling was rendered necessary because of the
The Lingula-Flags and Igneous Rocks of the Neighbourhood of Dolgelly
Authors: Lake Philip , Reynolds S. H.
Published: October 2009

I. Introduction.

The magnificent section displayed in the precipitous northern face Cader Idris has attracted the attention of many geologists, and has proved so seductive that the lower-lying country to the north has been almost neglected. It is with the latter that we are concerned. Here the
Lingula
-Flags are well developed, and are associated with contemporaneous volcanic rocks and with remarkable intrusive masses of diabase.

But little has yet been published concerning these rocks. Belt in his classical paper upon the
Lingula
-Flags has dealt with the general sequence in the district, and refers to several localities in the neighbourhood of Dolgelly. Cole and Jennings have examined the rocks immediately south of the area covered by our map, and they were led to believe that the volcanic eruptions of this region began at least as early as the Tremadoc period; but, as they remark, the point requires further investigation. We are able to justify their belief, for we have discovered a well-defined band of andesitic :lava in the
Lingula
-Flags themselves.

Several references to the region will also be found in the Geological Survey Memoir on North Wales; and the account of the
Lingula
-Flags in the Palæontological Appendix is in this respect of particular interest.

II. Description of the Area.

The area with which this paper deals lies south and west of Dolgelly, between the Arthog road and the hill called Mynydd Gader, which stands in front of the precipices of Cader Idris.

The town of Dolgelly stands in the valley of