bluuebunny/crossref_metadata_2025_split huggingface dataset:
North Italian Bryozoa.—Part II. Cyclostomata
Authors: Waters Arthur Wm. 
Published: October 2009

The Chilostomata from the same localities were dealt with in vol. xlvii. (1891) p. 1 of this Journal. It is always unsatisfactory to describe Cyclostomata, as there are so few characters that can be employed in classification, nor are we yet sure as to the relative importance of those used. The difficulties are much increased by the vast number of named species based upon some slight difference in the mode of growth, and in some cases the individual state of preservation has been the ground of a new species.
I have before me a list of 424 names of Tertiary Cyclostomata, which no doubt could be increased to nearly 600, but we are certainly within the mark when we say that of these more than 200 could not be recognized again, while many are known to be only synonyms.

In the Tertiaries
Hornera, Idmonea, Filisparsa
, and
Entalophora
are by no means sharply-defined genera, and seem to run into one another.

The most interesting species dealt with is a new one, which I have called
Diastopora brendolensis
. It has a tubule to most zoœcia, but differs from the living species
D. obelia
, which also has tubules; for in the fossil they run up more by the side of the zoœcium, whereas in
D. obelia
they are on the front of the zoœcium, about the middle. The zoarium is usually erect, formed by very compressed branches with zoœcia on both sides; but there are, besides, some incrusting specimens having similar small zoœcia
Archæopneustes abruptus
, a New Genus and Species of Echinoid from the Oceanic Series in Barbados
Authors: Gregory J. W. 
Published: October 2009

I. Diagnosis of the Echinoid.
Archæopneustes
, nov. gen.—Test large, elongate; high and generally conical, with the anterior slope much the steepest. Anterior ambulacrum flush.

Apical system: ethmolysian (in cases which are certainly known; but M. Cotteau's figure leaves the matter doubtful in one species).
Ambulacra: the lateral are subpetaloid, broad and unequal; the petaloid portions extend to the ambitus. The pores are large; in the posterior pair the outer pores arc elongate or comma-shaped. The anterior ambulacrum is reduced, and contains only very small, scattered, single pores.
Peristome: very excentric anteriorly. Labiate: in a depression. Periproct: on the narrow posterior vertical margin. Fascicles: none, or possibly an imperfectly developed marginal one. Distribution.—Cainozoic (recent and fossil) in West Indies. Species I. (Type of genus) Archœpneustes hystrix (A. Agassiz). Species 2. Arvhceopneuztes abruptus, 2 n. sp.
Form: anterior margin wellrounded and with no anterior groove; the maximum width, which is greater than the length, is at a little less than a third of the length of the test from the anterior margin; from the widest part the sides taper back by a long curve tot he narrow posterior end. Seen from the sides the anterior margin is short and steep; and from the vertex there is a long backward slope which increases in steepness till it reaches the posterior margin.
Apical system: at the apex, very excentric anteriorly; details unknown, but it is probably compact.
Ambulacra: the antero-lateral pair diverge from the apex almost at right angles to the long axis of
The Pleistocene Deposits of the Sussex Coast, and their Equivalents in Other Districts
Authors: Reid Clement 
Published: October 2009

The geological survey of the district lying between the South Downs and the Sussex coast has been completed, but the time needed for finishing and engraving the maps will make it impossible to publish a memoir for several years to come. It seems advisable, therefore, to bring before this Society an outline of the general results obtained, especially as certain of these results may seriously modify our views as to the succession of the deposits, and also as to the climatic changes in late Tertiary times in the South of England. A previous communication, published in this Journal, dealt with the question of the origin of the Coombe Rock and of dry Chalk valleys; I now propose to continue this work by showing the relation of the Coombe Rock to the various Pleistocene strata which occupy the plain lying between the southern edge of the Downs and the sea. I propose also to indicate briefly the probable correlation of these strata with the glacial deposits of other parts of England.
The literature of the subject is somewhat extensive, for many good observers have examined the deposits between Brighton and Selsey Bill, especially the ‘Pagham erratics,’ the ‘mud-deposit’ of Selsey, and the Brighton ‘elephant-bed.’ It will scarcely be necessary here to speak of the whole of the writings relating to the district, but certain important memoirs and original observations must be referred to; otherwise it would be impossible to show in what respect the recently completed Survey supplements our previous knowledge
On the Lithophyses in the Obsidian of the Rocche Rosse, Lipari
Authors: Cole Grenville A. J. , Butler Gerard W. 
Published: October 2009

The Rocche Rosse lava-stream, partly filling the pumice crater of Monte Pelato, Lipari, and breaching it on the north-eastern side, was described by Prof. Judd in 1875. As recorded by him and by Cortese we find in this locality all varieties of obsidian lava, from compact black glass to the pumice of commerce, or even a honeycombed material passing into ‘thread-lace scoria’ A person who, arriving at the south-western or landward side of the crater, begins walking over the hummocky surface of the Rocche Rosse along the centre of that part which lies within the crater, cannot fail to be struck by the fact, emphasized by Cortese, that much of the lava here, as at the Forgia Vecchia, has a texture intermediate between that of pumice and compact glass. In fact, he might walk along the middle of perhaps the first third of the Rocche Rosse without finding anything that he would call obsidian. However, if he turn to the right and make his way towards the southern margin of the lava, he will find portions of it in which black glass predominates.
From one of the numerous outstanding hummocks of this part of the Rocche Rosse were obtained the specimens of black glass with vesicles, lithophyses, and spherulites, which have led to the writing of this paper, and from which the sections figured in Plate XII. have been taken. It must not be supposed, however, that the rock here differed in any essential from the lithophyse-bearing obsidian found elsewhere
On the Discovery of Mammoth and other Remains in Endsleigh Street and on Sections exposed in Endsleigh Gardens, Gordon Street, Gordon Square, and Tavistock Square, London
Authors: Hicks Henry 
Published: October 2009

Conclusions
The old land-surface under Endsleigh Street, on which the Mammoth died, is almost exactly 60 feet above the present sea-level.
The deposits which subsequently accumulated over the remains were evidently laid down in moderately tranquil water, otherwise the bones, especially those of the young Mammoth, would not have remained so near together. The epiphyses of the long bones were found close to the shafts, and unless the animal was suddenly buried in sediments accumulated in fairly quiet waters such as those of a lake, the epiphyses would have been readily moved as soon as the soft tissues and cartilage decayed. Except in caverns, where the bones in their fresh state must have been carried in by hyænas and other beasts of prey, it has been difficult in many cases to determine the exact horizon at which the Mammoth lived, since the bones have as a rule been removed from the spot where the animal died, and re-deposited in newer sediments. Here, however, we have the old land-surface, and evidence of the contemporaneous flora in the loam in which the bones were embedded.
An examination of the sections in this area, and also in adjoining areas, shows that there is a well-marked sequence in the deposits. Immediately over the bones there was, first, a fairly rough gravel; this was followed by a sandy gravel with smaller pebbles, and the latter was overlain by a fine, somewhat loamy sand with occasional seams of clay. Above this came the yellowish clay containing a
On
Delphinognathus conocephalus
(Seeley) from the Middle Karoo Beds, Cape Colony, preserved in the South African Museum, Capetown
Authors: Seeley H. G. 
Published: October 2009

The skull herein described is the only portion of the animal collected. No locality for it is recorded in the South African Museum, but Mr. Thomas Bain, the Government geologist in Cape Colony, believes it to have been collected by himself from near Beaufort West. It is slightly distorted with the folding of the strata. The preservation of the specimen leaves something to be desired, for the pre-orbital region is more or less obscured by weathering, which has destroyed the superior contour of the snout, the alveolar border, and the anterior extremity of the jaws. The occipital condyle and much of the occipital plate from the back of the skull are also lost. But, notwithstanding these defects, the skull is the most interesting Anomodont preserved in Cape Colony, and indicates a new family of fossil Reptilia.
The head is characterized by its broad, high, vertical occipital plate. The broad subpentagonal roof to the brain-case (fig. 2) ascends laterally from the inclined temporal region, and is elevated in a cone, which terminates in a large, circular, crater-like parietal foramen. The skull has large sub-circular vertical orbits, placed far backward above the hinder extremity of the lower jaw, so as to converge forward. The temporal fossæ are short and small, owing to the position of the orbits and the width of the cerebral region. The quadrato-squamosal region is directed obliquely forward, and forms a vertical articular surface to articulate with the lower jaw, which is singularly deep posteriorly, and suggests the jaw
Notes on the Geology of the Nile Valley
Authors: Pasha E. A. Johnson , Richmond H. Droop 
Published: October 2009

These notes refer to some observations on the geology of the Nile, during journeys from Cairo to Wady Halfa.
The rocks on both sides of the Nile are, speaking generally, Eocene (and? Cretaceous) from Cairo to Esneh; at Esneh, or about five miles south, we enter a sandstone region, which continues to near Assouan, where it meets the granite and basalt. A few miles south of Assouan the sandstone recommences and continues to Wady Halfa, broken only by enormous dykes of granite, which occur at Bab-el-Kalabsha and one or two other localities.

The following points are worth noticing as we follow the Nile from Cairo to Wady Haifa:—

(i)
The saturation with silica of the old sand-and-gravel beds overlying the Nummulitic Limestone near Cairo, forming sandstones of all qualities from an extremely hard stone to one that can be rubbed down to powder between the fingers.
A similar saturation, apparently from water containing silica in solution, is visible in the beds overlying the Nummulitic Limestone in Biluchistan.

(ii)
The fact that these old sands and gravels are formed from very old rocks, principally granitic. They contain great quantities of the Assouan pebbles, brown and red, wholly or semi-transparent, which were so largely used by the Romans to cut cameos and intaglios. Some minerals are found in these gravels, notably cobalt, the source of which is unknown.

(iii)
The petrified forests of the same region.

(iv)
The occurrence in greater or less quantity of titaniferous magnetic oxide of iron in the beds forming the Nile Valley;
Microzoa from the Phosphatic Chalk of Taplow
Authors: Chapman F. 
Published: October 2009

The present paper is the result of an examination of some material kindly sent me by Mr. Llewellyn Treacher, who obtained it from about the middle of the phosphatic band at Taplow.
A short list of the foraminifera of the Taplow Chalk has already been given by A. Strahan, Esq., M.A., F.G.S., of H.M. Geological Survey, with the assistance of Prof. T. Rupert Jones, F.R.S., F.G.S., and I wish at this point to express my obligation to the latter for help and advice in preparing these notes.
The material used was excessively rich in well-preserved specimens of foraminifera, forming perhaps 75 per cent. of the whole; and a series selected from it proving so extensive and interesting, there seemed good cause to communicate a list of them.
On treating the disintegrated chalk with a weak solution of hydrochloric acid, the most perfect casts in phosphate of lime are obtained, the Rotaline forms being especially noteworthy.
The total number of species and varieties of foraminifera found is 98; and to these must be added 5 species and varieties of ostracoda, represented by 11 specimens.

All the forms of ostracoda herein noted have been previously found in the Chalk. They are:—
Pontocypris triquetra
, Jones, sp., 2 specimens;
Bythocypris silicula
, Jones, sp., 1 specimen;
Cythereis auriculata
, Cornuel, sp., 1 specimen;
C. Wrightii
, Jones and Hinde, 6 specimens; and
Cytherella Williamsoniana
, var.
granulosa
, Jones, 1 specimen.

Of the 98 varieties of foraminifera, 5 appear to be entirely new to science, whilst altogether 30 are new
Contributions to the Geology of the Wengen and St. Cassian Strata in Southern Tyrol
Authors: Ogilvie Maria M. 
Published: October 2009

I. Introduction.
My interest in the Alpine Trias was first aroused by several geological excursions in Northern Tyrol during the summer of 1891. In response to a wish of mine to undertake some original research, it was kindly suggested by Freiherr F. von Richthofen, of the Berlin University, that I might make a detailed study of the Wengen and St. Cassian Beds in the valleys of Enneberg and Ampezzo in Southern Tyrol, and with these vaileys in particular the present paper deals.
I shall ever regard it as a peculiar honour that, Freiherr von Richthofen, whose early work, ‘Geognostiscbe Beschreibung der Umgegend von Predazzo, St. Cassian, und der Seisser Alpe,’ still holds the highest place in the literature of the Southern Tyrol ‘Dolomites,’ guided me in my first attempt in Alpine geology, that he himself taught me the chief points at issue concerning the district between Schlern and Ampezzo, and gave me, in a short space of time, a far clearer insight into the work which lay before me than falls to the lot of most young geologists.
In the course of my work during the two seasons of 1891–92, I have been led to extend somewhat my primary object, and to include some of the more interesting tectonic aspects of the whole group of Upper Triassic strata in the ‘Dolomite Alps.‘
My most grateful thanks are due to Herr Prof. von Zittel for the constant kindness he has shown me, and for his advice and encouragement during the two
Scandinavian Boulders at Cromer
Authors: Madsen Herr Victor 
Published: October 2009

During a visit to England in the autumn of 1891, I took the opportunity of making a short excursion to Cromer in order to study the interesting geological facts presented in the well-known cliffs near that village.
On my walks along these cliffs my attention was especially devoted to the boulders which occur there, for I thought it possible to find some which might with certainty be referred to definite localities in Scandinavia. The greater number of the boulders there originate indeed, as I expected, from disturbed portions of the Cretaceous strata which underlie the Drift in the vicinity of Cromer, so that it is only a few of the boulders which are likely to be of Scandinavian origin, and of these again only a small number can be definitely referred to their parent localities.
Among the boulders on the shore a little west of Cromer I succeeded in finding a ‘porphyry’-boulder which I supposed had been derived from the south-eastern part of Norway, and this supposition was subsequently confirmed by Herr K. O. Björlykke, of the Norwegian Geological Survey, to whom I showed the boulder and who referred it to the neighbourhood of Christiania.
This boulder measures
about 4½ × 3½ × 2 inches. The ground-mass is rather decomposed and of a grey-violet colour; in it are disseminated crystals of felspar which, on fresh fracture, show the same colour as the groundmass, while those on the surface of the boulder have become somewhat paler by decomposition. The sections of
Geological Notes on Certain Islands in the New Hebrides
Authors: Frederick G. C. , Hinde George Jennings , Teall J. J. H. 
Published: October 2009

So far as can be judged at present from the soundings obtained, it appears that the New Hebrides are probably situated on a bank lying from 350 to 400 fathoms below the surface of the ocean and running in a N.N.W. and S.S.E. direction, with a deep valley between it and New Caledonia. The only soundings obtained between these two groups are 2375 and 2730 fathoms respectively, the former within a short distance of the New Hebrides.

1.
Tanna
.—On the east side of this island is situated a volcano which has been in constant activity for many years, and on ascending its sides one is struck by the fact that so little lava is to be seen. The cone itself, which rises to a height of nearly 1000 feet above the sea, appears to be formed entirely of more or less fine ash, and there are no signs of any lava-flow.

In November 1890 the crater appeared to be about 300 feet deep, and was split into two nearly equal parts by a kind of rocky wall or partition which rose to a height of about 100 feet from the bottom.
There were five fire-holes, three on one side and two on the other side of the partition, where the molten materials were bubbling and pulsating with a subdued roaring sound; but every few minutes a tremendous explosion took place, throwing up the molten seoriæ, etc., to heights varying from 100 to 300 feet above the summit of the crater.
On the Microscopic Structure of the Wenlock Limestone, with Remarks on the Formation generally
Authors: Wethered Edw. 
Published: October 2009

I. Introduction
The general features and fossils of the Wenlock Limestone have been described by several geologists, but I am not aware of any endeavor to make a systematic examination of the microscopic structure. The value of such work has been greatly underestimated; for investigations which I have made show that, although much information as to the formation and structure of the rock may be gained by observations made without the assistance of a microscope, yet the use of this instrument brings into view important facts which are not perceived by the unassisted eye.
In this paper I do not attempt an exhaustive enquiry; to do this it would be necessary to make several visits to the localities from which specimens for examination were collected, and this I have been able to accomplish only in the case of the Wenlock Limestones exposed within a convenient distance from Cheltenham. I have therefore selected what I regard as typical sections of the limestone in the neighbourhood of May Hill in Gloucestershire, and in the adjoining portion of the county of Hereford.
The procedure has been to take samples from several beds in each exposure of the rock, and to grind down the usual thin sections for examination under a microscope. These I prepare myself, and I mention the fact because it seems to me important for this reason: very many slides require to be made for a paper like the present one, and each must be adjusted, with regard to actual thinness,
On the Dwindling and Disappearance of Limestones
Authors: Rutley Frank 
Published: October 2009

There are probably few instances in nature in which limestone–beds are so protected that water cannot gain access to them. A limestone-bed to which water charged with carbonic acid gains access becomes gradually dissolved, and, furthermore, the solvent action of humus acids must also, in some cases, be taken into account. The question whether such a bed will completely vanish is one which involves merely the magnitude of the bed, the duration and energy of the solvent action, and the freedom of the limestone from foreign matter of a more or less insoluble nature. If unlimited time be conceded, there seems no reason why very thick beds of limestone should not wholly disappear; at all events thin ones may easily do so.
The formation of caves, chasms, and pinnacles, the general sculpturing of limestones, and the thick deposits of calcareous tufa which occur in many localities sufficiently attest the activity with which the erosion of limestones has been carried on in recent times, and there appears to be no reason to doubt that similar work has been constantly in progress during bygone ages, under like conditions. Given like conditions, the greater the age of any limestone-deposit, the more will it have been wasted away. Granted sufficient time, its disappearance is inevitable.
Any argument adduced in support of the probable disappearance of very ancient beds of limestone may be applied with additional force in the cases of rock-salt and gypsum.
Where limestones occur at the surface, their erosion is due not
On Raised Beaches and Rolled Stones at High Levels in Jersey
Authors: Dunlop Andrew 
Published: October 2009

The valuable paper of Prof. Prestwich on ‘ The Raised Beaches, and ‘ Head ’ or Rubble-drift, of the South of England,’; which has thrown so much light on the Quaternary geology of that area, is especially interesting to me. for in Jersey there are well-marked post-Glacial deposits which have hitherto received little attention from geologists. The brick-clay or brick-earth, which covers so much of the island, I have already described, and I am now desirous of directing attention to the higher raised beaches, and to other evidences of alteration in the height of the land, more especially of considerable and probably long-continued subsidence.
Several writers have already described or mentioned the low-level raised beach, found in places all round the island —as, for example, Mr. Trevelyan, Lieut. Nelson, Prof. Prestwich, and Father Noury The last-named geologist, however, seems to doubt its being a raised beach in the proper sense of the term. Mr. T. W. Danby, on the authority of the late Dr. M. Bull, mentions a raised beach on the west coast of the island, said to be about 100 feet above the level of the present beach and in Latham and Ansted's work on the Channel Islands it is stated that a raised beach about 30 feet above the present mean level of the sea was laid bare during the construction of Fort Regent.
The most elevated raised beach which I have as yet observed is that on the top of the soutehrn part of the
On Composite Dykes in Arran
Authors: Judd J. W. 
Published: October 2009

I. Definition and Classification of Composite Dykes.
Those dykes which are filled with materials differing one from another in chemical composition or mineralogical constitution may be conveniently spoken of as ‘composite dykes.’ In some cases the diverse rocks found in the same dyke may be only varieties of a single type, exhibiting dissimilarities in the proportions or arrangement of their several mineral constituents; but in other cases two or more rock-species, absolutely distinct, may be found to enter into the constitution of a single dyke. A careful study of these composite dykes shows that they fall naturally into two classes, as follows :—

(A)
Composite dykes in which a differentiation has gone on in the material that has filled the dyke
.—This differentiation usually results in the separation, or partial separation, of the vitreous base of the rock from the crystals scattered through it ; but in some cases the crystallizing process, acting selectively within the dyke, has led to the formation of rocks which, in different parts of the dyke, show marked variations in chemical composition or texture, and even in mineralogical constitution. The separation of the glassy from the crystalline materials in this variety of composite dykes takes place in various ways ; the vitreous material may form lateral bands (‘ selvages ’) or irregular patches, or it may fill ‘ amygdaloidal’ cavities. But in all cases there is found to be a more or less perfect gradation from the one type of rock to the other.

(B)
Composite