bluuebunny/crossref_metadata_2025_split huggingface dataset:
Palichthyologic Notes. No. 8. On some Ichthyolites from the Nummulitic Limestone of the Mokattam Hills, near Cairo
Authors: Egerton Philip de M. Grey 
Published: October 2009

T
he
fish-remains contained in the six specimens submitted to me by Mr. Homer for examination are derived from not fewer than sixteen individuals.

With the exception of one mutilated tail, the posterior portions of all are deficient. The cranial bones are for the most part in good preservation; some of the fins are also well shown, more especially those parts composed of hard spines. The teeth and scales are also in perfect condition. The anterior portion of the endo-skeleton is displayed in several of the specimens, together with the dermal apparatus for supporting the dorsal and anal fins. Unfortunately the precise character of the dorsal fin is not recognizable, nor can the soft rays of any of the fins be counted with accuracy. The branchiostegous rays are also indefinable, both as to form and number; and the vomer and palatine bones are not visible.
These deficiencies render doubtful the determination of the family or genus to which the species is to be referred. Enough, however, is preserved to afford, if not conclusive evidence, at all events an approximation to the truth.
There is no question but that all the specimens belong to one and the same species, and the crowded position of their remains warrants the conclusion that it was a gregarious species. The characters of the scales and fin-rays determine it to be a true Ctenoid of Agassiz, or Acanthopteroid of Müller, and belonging to one of the most typical families of the Order.
In the absence of the
On the Pegmatite of Ireland
Authors: Delesse M. A. 
Published: October 2009

Abstract

T
he
author observes that the Pegmatite of the Mountain of Mourne in Ireland is very remarkable for its cavernous structure. This structure is especially found in pegmatites which contain topazes; it is therefore probable that the cavities in the pegmatite are owing to the separation of fluoric gases, the fluor of which is subsequently fixed in the topaz and mica.

The Irish pegmatite is also very remarkable for the presence of fayalite and of ferruginous peridote; for peridote is the characteristic mineral of rocks of igneous origin which have not an excess of quartz.
M. Delesse remarks, in conclusion, that cavernous pegmatite is formed under circumstances markedly different from those under which granite properly so called is produced.
On the Structure and Affinities of the Hippuritidæ
Authors: Woodward S. P. 
Published: October 2009

Abstract

T
hese
fossils were regarded by the author as bivale shells, forming a distinct family, related most nearly to the
Chamidæ
and the Cardiadæ.

The Hippurite was shown to have its valves articulated by a hinge essentially like that of the Radiolite. The internal ligament or cartilage is divided into two portions, situated at the sides of the first or most anterior of the three inflections of the outer shell-wall; this ligamental inflection is very prominent in the
Hippurites cornuvaccinum
, but obsolete in
H. bioculatus
. Two prominent straight teeth are developed from the upper valve, parallel with the hinge-margin, in
H. bioculatus
and
H. radiosus
, transverse to it in
H. cornuvaccinum
. The anterior tooth supports a curved horizontal muscular apophysis, shaped like the adductor impression in the lower valve, the posterior tooth has a long vertical process, sometimes more prominent than itself, which is received by the cavity between the first (or ligamental) and second (muscular) inflection, which corresponds to the muscular ridge in
Diceras
and
Cardilia
. The third ridge in the lower valve of the Hippurite, which meets a corresponding inflection of the upper valve, was compared to the siphonal ridge of certain bivalves, which divides the inhalent from the exhalent current of water.

In a series of specimens of
Radiolite, Hoeninghausii
, presented by Mr. Pratt to the British Museum, there was evidence that the
umbo
of the upper valve was marginal when young; and the ligamental inflection, though obsolete externally, was always manifest inside the upper valves which had
On the Correlation of the Lower Tertiaries of England with those of France and Belgium
Authors: Prestwich Joseph 
Published: October 2009

Abstract

I
n
this paper Mr. Prestwich treated of those Tertiary beds which, commencing immediately above the Chalk, are in England limited superiorly by the Bracklesham Sands; in France, by the
Calcaire grossier
, and in Belguim, by tne
Système Bruxellien
of Mr. Dumont; and he endeavoured to show the exact correlation of the several divisions of these lower tertiaries, and claimed for the “London Tertiaries,” as a group, a distinct and separate position beneath that of the Paris group, of which latter the
Calcaire grossier
may he taken as the centre and type. The chief points of importance are—that the Lower Bagshots are the equivalents of the
Lits coquilliers
; and that the well-known
Sable de Bracheux
, with its marine fossils, corresponds with the lower part of the Woolwich series.

The author first pointed out that the known equivalents among the Tertiary beds in question are—

1.
Calcaire grossier, France = Bracklesham Sands, England = Système Bruxellien, Belgium.

2.
Lits coquilliers, France = Syst. Ypresien supérieur, Belgium. (The zone of Nummulites planulatus.)

3.
Lignites of the Soissonnais = Fluviatile beds of Woolwich and Lewisham.

Mr. Prestwich then described in detail the grouping of the tertiary strata in France, Belgium, and England respectively; and, having pointed out the local differences and peculiarities exhibited by these deposits, he entered upon a detailed comparison of the different divisions of the tertiaries of the several districts.
On the Geology of portions of the Turko-Persian Frontier, and of the Districts adjoining
Authors: Loftus William Kennet 
Published: October 2009

Abstract

T
he
geological researches detailed in this memoir were made in the years 1849–52, during the progress of a joint commission appointed by the English, Russian, Turkish, and Persian governments for the demarcation of the Turko-Persian frontier.

The line of country investigated during the Survey hears in a N.N.W. direction from Mohammerah, at the head of the Persian Gulf (Lat. 30° 26′ N.), to Mount Ararat (Lat. 39° 42′ N.); a direct distance of rather more than 600 geographical miles.
The first 250 miles, from Mohammerah to near Mendali, is an arid and deserted waste, infested by plundering parties of Arabs and Kurds, but capable for the most part of extensive cultivation.
From Mendali to Zohab (50 miles) the exterior tertiary chain of low gypsiferous ridges, which everywhere skirt the west flank of the Zagros, is crossed; and at the latter place the nummulitic limestone and cretaceous rocks are first reached.
From this point to near the Lake Zerribar (60 miles) is a succession of regular, saddle-formed, limestone anticlinals, with alternate synclinals, containing disconnected portions of the gypsum series, and underlaid by older blue schists.
The remainder of the frontier exhibits a lofty range composed of igneous rocks, which, bursting through the stratified deposits, constitutes the axis of the vast barrier ridge nearly as far as Bayazid, at the south foot of Mount Ararat, a distance of 270 miles.
Other traverses were made as far south as Shiraz (Lat. 29° 36′ N.), and many valuable sections obtained, which are referred to
On the Occurrence of Copper in Tennessee, U.S.
Authors: Bray W. 
Published: October 2009

Abstract

T
he
gneiss and mica-schist of Eastern Tennessee strike south-west and north-east (about 47° E. of N.), and dip to the south-east (at angles of about 25°), running parallel to and forming an outer range of the Alleghany Mountains. Veins of copper and iron ores, with occasional quartz veins, lie in the schists, dipping parallel with them, and consisting of porous oxide of iron at top, with iron pyrites and carbonate and sulphuret of copper lower down. The veins are described as being sometimes 45 feet wide, and traceable for upwards of 70 miles ; but they are worked chiefly in the extreme south-east corner of Tennessee, in the township of Duckton, in the county of Polk, a district ceded by the Indians to the States about four years ago.
Additional Remarks on the Skull of the
Baphetes Planiceps
, Ow
Authors: Owen  
Published: October 2009

Since the communication of the notice of the portion of cranium of the Labyrinthodont Reptile above-named (Quarterly Journal of the Geol. Soc. May 1854), I have been favoured with the view of some other fragments of the same cranium, including parts of the interior or under-surface, with several teeth buried in the coal-matrix, and exposed at the fractured surfaces.
In the ordinary Labyrinthodont Reptiles of the European Trias, one or two teeth at the fore-part of the jaws have the form and proportions of large canines, the rest are smaller and more slender pointed teeth.
One of the present fragments includes the fore-part of the right maxillary and premaxillary bones, and shows a single large laniariform tooth descending from the fore-part of the maxillary into the substance of the subjacent matrix: in front of the tooth is one of the smaller, pointed, serial teeth: of which teeth other fragments show other examples, the base of the teeth being anchylosed to shallow sockets in the bone.

So much, therefore, of the dental system of the
Baphetes
, as is here exhibited, accords in the general characters of shape and relative size, of disposition and mode of fixation to the jaw, with the dentition of the Labyrinthodonts.

A transverse section was taken from about the middle of the large tooth, and exhibited the usual labyrinthic structure: rather less complex than in the
Labyrinthodon Salamandroides
.

The character of the exterior surface of the cranium was indicated in the specimen originally submitted to me by
On the Occurrence of Glacial Traces on the Rock of Dumbarton
Authors: Brickenden L. 
Published: October 2009

A
s
the very peculiar and remarkable positions in which glacial striæ and abrasions are sometimes observed on the surface of rocks in Scotland may tend, if carefully examined, to explain the particular mode in which such phænomena have been produced, it is probable that the occurrence of glacial traces beneath an overhanging rock bordering a fissure at Dumbarton Castle is, amongst others, worthy of being recorded.

The hard whinstone, which here rises up abruptly from the alluvial shores of the River Clyde, exhibits in a very interesting and beautiful manner the crystalline arid prismatic structure peculiar to such trappean effusions, but the lines of fracture or divisional planes of the Rock of Dumbarton are observed to incline generally at an angle of about 70° giving to the Rock on one of its sides a rather precipitous and overhanging appearance. The effect of denudation or abrasion has therefore been to wear or score it in certain parts into fissures, the sides of which have a parallel inclination; and across the centre of the Dumbarton Rock there is one of considerable depth, dividing the hill into two parts or summits, as shown in fig. 2.
It is on the sides of this fissure, which now forms a passage, and the only mode of approach to the buildings on the Rock, that striaæ and abrasions are observed, which constitute the subject of this notice.
The fissure intersects the Rock from south to north, pointing directly up the valley of the Leven, through which
Additional Observations on the Occurrence of Pipes and Furrows in Calcareous and Non-calcareous Strata
Authors: Trimmer J. 
Published: October 2009

T
he
following observations, which are necessary for the full understanding of the views I have taken on the origin of sand-pipes and furrows in and on the surface of strata, are offered in support of some positions I have taken in my former papers on the subject, and which, from their not having been fully elucidated, require some explanatory remarks in their defence.

1. It was not my intention to assert in a former paper‡ “On Pipes and Sand-galls in the Chalk of Kent” that the Thanet Sands are calcareous, as Mr. Prestwich has been very naturally led to infer in his memoir read before the Society, Jan. 18, 1854, from the expression, “The sand with which the pipes are filled contains much calcareous matter.” This calcareous matter was chalk, redeposited near the lining of the pipe from water charged with bicarbonate of lime. Having sent a specimen of it with the paper, I did not think it necessary to enter into fuller explanations.
2. I have stated § that I saw miniature pipes actually forming by the mechanical action of water on blocks of siliceous sandstone, on the sea-shore near Reculver. Mr. Prestwich replies, that this sandstone contains some carbonate of lime. It appears by Mr. Prestwich's papers ‖ on the Eocene Tertiaries, that the cliffs at Reculver yield two sandstones, the one belonging to the Thanet Sands, the other to the London Clay series,--the former calcareous, the latter but slightly so. On blocks of one of these, I
On a Fossiliferous Drift near Salisbury
Authors: Prestwich Joseph , Brown John 
Published: October 2009

T
he
great extent of bare and clean-denuded chalk hills forms a very striking feature of the scenery around Salisbury. But, although the more prominent parts of the country are so free from drift, the small valleys which traverse these great undulating downs contain, scattered along their base and often extending for a short distance up the slopes of the adjacent hills†, a considerable quantity of gravel, flint- and chalk-rubble, and brick-earth. This drift is, in greater part, of local origin, and is very irregular in its structure and distribution; one material predominating at one spot, and another taking its place close by. Flint-rubble and sandy clays preponderate usually in the lower parts of the valleys, chalk-rubble being more common on the hill-slopes, whilst the brick-earth is irregularly and only occasionally patched on the base of the hills, alternating with and replacing the flint- and chalk-rubble.

Three of these small valleys are confluent at Salisbury. It is on the north-easteru side of the one through which the Willey flows that one of the best exhibitions of the Drift is obtained. The following section shows the prevailing relation and structure of this deposit, which here rises about 30 to 40 feet above the level of the Willey*.
The railway-cuttings between Salisbury and Wilton expose some good continuous sections, whilst several brick-fields give a few deeper excavations. In a cutting adjoining Wilton, large subangular gravel, chalk-rubble, and coarse rubbly brick-earth alternate and pass laterally one into the other. The following section of a
On the Causes producing Foliation in Rocks; and on some observed cases of Foliated Structure in Norway and Scotland
Authors: Forbes David 
Published: October 2009

T
he
study of the metamorphic and crystalline rocks has of late years attracted much attention, and the researches of Darwin, Sharpe, and others have brought forward many facts particularly interesting and important.

It will probably, however, be admitted, that, notwithstanding the labours of these geologists, great difference of opinion exists as to the formation and structure of these rocks, and that at present we are not in possession of sufficient data to enable us to place the question upon a firm basis. It is therefore of importance that as many observations as possible be laid before geologists working at this subject; and it is consequently hoped that the present communication may not prove unserviceable in advancing the inquiry.
The observations here brought forward have with a few exceptions been made during a residence of some years in Norway, where the foliated rocks play so important a part. The others are the result of some short excursions in Scotland made for the express purpose of comparison.
For a long period, and it may be said until late years, it was the generally received opinion that the lines of foliation in rocks were lines corresponding in direction or identical with the lines of stratification, and were produced by the alteration of these lines by metamorphic action. This view of the case can no longer be considered tenable, and the observations of many geologists have shown that foliation frequently takes place at a different angle to that of stratification.
Darwin seems to consider
On the Occurrence of Angular, Subangular, Polished, and Striated Fragments and Boulders in the Permian Breccia of Shropshire, Worcestershire, &c.; and on the Probable Existence of Glaciers and Icebergs in the Permian Epoch
Authors: Ramsay Andrew C. 
Published: October 2009

The sedimentary strata which contain the fragments of striated and polished rocks to which I am about to call attention belong to the inferior portion of that which has been defined as the “Permian Group” by Sir Roderick Murchison, the true geological horizon of which in England was first explained by Professor Sedgwick, in his celebrated memoir, “On the geological relations and internal structure of the Magnesian Limestone and the lower portions of the New Red Sandstone series,” &c. It is of the last-named division of this series that they probably form a part.
The speciality of the subject of this memoir scarcely requires me to enter upon points connected with descriptive geology further than may be needful to explain the true position of the Breccias alluded to; and the detailed sections subsequently given, having that object in view, should therefore be considered chiefly as explanatory of the general relations of the subdivisions of the Permian and Bunter strata to each other. It is, however, proper to state that the general position of the Permian rocks skirting the coal-fields of North Wales, Coalbrook Dale, and Staffordshire was first indicated in Sir Roderick Murchison's Map, published in 1839. They are there coloured as Lower Red Sandstone with subordinate calcareous conglomerates; and their lower boundary he defined by the outcrop of the Coal, while the upper he shaded off into the New Red or Trias properly so called. The line of demarcation between the Permian and Bunter rocks has, however, lately been
On the Occurrence of Obsidian Bombs in the Auriferous Alluvia of New South Wales
Authors: Clarke W. B. 
Published: October 2009

I
n
Mr. Darwin's ‘Geological Observations on the Volcanic Islands visited during the voyage of H.M.S. Beagle’ (p. 38), that author describes and figures a volcanic bomb of green obsidian from the plain between the Rivers Darling and Murray, and which he received from Sir T. L. Mitchell.

The explanation given by Mr. Darwin appears to be satisfactory as to the origin of that individual specimen, and it is confirmed by the parallel examples cited from M. Beudant. Sir T. L. Mitchell's specimen would seem either to have been drifted from a very long distance, or, which is more likely, from the known habits of the aboriginals, to have been dropped by one of them, who probably found it in the trap-hills of the Lachlan to the north-eastward. This specimen was unique as to Australia, until recently.
During the last two years, several similar specimens have been found in the auriferous detritus of the western and northern Goldfields.
The first which I met with was found in the cradle of a gold-washer on the Turon River, who dug it from a depth of 30 feet below the surface. This was a small, irregular, roundish substance, 0·6 inch in diameter, having a specific gravity of 2·7 at a temperature of 66°.
It was undivided, and more like those examples described by M. Beudant than tile figure given by Mr. Darwin. A similar specimen, but of a rude elliptical form, ½ inch diameter in the major axis, and having a sp. gr. of
On the St. Cassian Beds between the Keuper and the Lias in the Vorarlberg Alps
Authors: Merian  
Published: October 2009

I
have
lately visited, with my friend Escher von der Linth, the Alps of the Vorarlberg, and the neighbourhood of the Lake of Lugano and the Lake of Como. In the Vorarlberg we found immediately under the Lias, which is well developed, the beds of the Dachstein Limestone, characterized by numerous Corals and a large bivalve (
Megalodon scutatus
of Schafhäutl, “Dachstein bivalve” of the Austrians). Below the Dachstein limestone are the Gervillia-beds (lately called Kössen-beds by Von Hauer). The
Cardita crenata
, Goldf., the Aviculæ of the family of the
Gryphæatæ
, and small turrited univalves, contained in these beds, induced me to refer them to some of the St. Cassian beds. Lower still are thickly developed masses of dolomite, under which sandstones with impressions of Keuper plants occur.

The exact relation of the Salzburg beds containing
Ammonites globosus
with the Gervillia-beds has not yet been made out. We have not hitherto been able to find in the Alps of the Vorarlberg this characteristic family of Ammonites.

In the vicinity of the Lake of Como, the dolomitie masses change their appearance ; but beneath the lias the Gervillia-beds form a good geological horizon, which can be found in numerous places when once one has become accustomed to its position. This bed is also found under the Lias of the chain of the Stockhorn, Canton Berne ; and Escher has found it in the neighbourhood of Geneva.
We have called the whole of the beds situated between the Lias and the Keuper
Notice of some Cretaceous Rocks near Natal, South Africa
Authors: Garden R. J. 
Published: October 2009

Abstract

T
he
discovery of these fossiliferous rocks, near the Umtafuna (on some maps spelt “Umtavooma”) River, on the coast of South Africa, was made by Mr. H. F. Fynn, in 1824. About three miles to the southward of the river commence certain excavations in the cliffs, formed by the action of the sea, and called by the natives “Izinhluzabalungu.” These caves extend for about 800 yards. In 1851 Capt. Garden visited the spot with Mr. Fynn, and, with the aid of his servant (the late Private Thomas Souton), and the natives, collected a suite of fossils from the walls of the caves and from the adjoining cliffs. The cliffs vary considerably in height, and their tops are covered with vegetation; the
Strelitzia alba
grows abundantly in the hollows. The lowest rock visible is a hard shelly rock with pebbles; above it is a brownish-red sandstone, traversed in every direction with white veins, which are the broken edges of colossal bivalve shells (
Inoceramus
). These shells are thin, and too easily broken to be extracted from the rock; the corrugated surface of a portion of one was exposed to the extent of 2 feet in length by 1 foot in breadth, and the author estimated others to be nearly 3 feet in length. This shell is common to all the strata in the cliff. Alternate layers of the above-mentioned two rocks occur to the height of about 18 feet ; above which are hard bluish-black, brown, and greenish argillaceous and sandy beds.

Shells were found in all these clay-beds, and Ammonites at different heights and in certain of the strata. Many fossils are exposed on the cliffs, and washed out on to the shore by the action of the sea.
Fossil trees are seen at low water on a reef of fiat rocks near these caverns ; and about three miles to the southward Capt. Garden found at the extreme point of the left bank of the Umpahlanyani* stream a piece of fossil wood, imbedded in a rock similar to that at the caves.
About half a mile beyond the caves runs the Umzambanit River, across which the cretaceous rocks are continued, appearing on its right bank ; after which they are lost sight of, except at a few places: the author, however, believes this ibrmation to extend as far as the Umtata River, having been informed by the late Mr. W. H. D. Fynn that fossil Turtle remains were to be procured from the rocks at the mouth of that river.