bluuebunny/crossref_metadata_2025_split huggingface dataset:
On two Chimæroid Jaws from the Lower Greensand of New Zealand
Authors: Newton E. Tulley 
Published: October 2009

H
aving
been working for some time past at the Cretaceous Fishes, my interest has been especially centred in the group of the Edaphodontidæ; for the specimens belonging to this group, which have been brought to light within the last few years, have much enlarged our knowledge of these peculiar forms of fossil fishes. The general results of my examination of this group, will shortly be published; and in the present communication it is only proposed to consider two specimens from the Lower Greensand of New Zealand, which have been deposited in the British Museum by Dr. Hector. My attention was first directed to these specimens by Mr. W. Davies, of the British Museum, when I was examining the fine series of Chimæroid jaws now in the national collection.

One of these New-Zealand specimens is the right mandible of a species of
Ischyodus
already known to us from the Gault of Folkestone; and the second is a small right maxilla, which is altogether new and appears to be generically distinct from any of the fossil forms hitherto described.

Before considering the peculiarities of the mandible, it will be necessary to enter into some explanation and description of the species to which it is referred.
It appears that, the late Prof. Agassiz, some years ago, saw in the Earl of Enniskillen's collection of fossil fishes, a Chimæroid mandible from the Gault of Folkestone, which he named, in manuscript, Chim0œra brevirostris. Subsequently, in his ' Poissons Fossfles' (1843), he alluded to this specimen
On a Bone-bed in the Lower Coal-measures, with an Enumeration of the Fish-remains of which it is principally composed
Authors: Davis James W. 
Published: October 2009

N
ear
Bradford and Clifton, in Yorkshire, a peculiar stratum of shale, which contains so great a number of remains of fossil fishes that I venture to call it a bone-bed, occurs immediately above the Better-bed coal, and is known to extend over a surface four or five miles in length by about two in average breadth.

The Better-bed coal is a member of the Lower Coal-measures, or Gannister series. It occurs about 700 feet above the Rough rock, the uppermost bed of the Millstone grits, and is separated from the Black-bed coal by overlying strata of an average thickness of 120 feet. It is extensively worked by the Low-moor Iron Company, and used by them in smelting the clay-ironstone of the district. It is peculiarly valuable for this purpose on account of its freedom from sulphur, the excellence of the iron manufactured by this firm being in a great measure ascribed to the use of the Better-bed coal.
The following section (p. 333) will explain the position of the bone-bed. The section extends from the thick series of sandstones known as the Elland Flag rock, below the Better-bed coal, to the Black-bed coal above.
The beds vary very much in thickness within even a small area, the sandstones and shales often thinning out from a thickness of from twenty to forty feet in less than a mile, and altogether disappearing. The most persistent beds are the coals and the fireclays, or seat-earths on which they rest. The section may be
On the Metamorphic Rocks surrounding the Land's-End Mass of Granite
Authors: Allport S. 
Published: October 2009

I
n
the following notes I propose to lay before the Society the results of a microscopical examination of certain metamorphic rocks surrounding the Land's-End granite. In doing so my principal object will be to point out the structural and mineralogical changes produced in clay-slates and certain igneous rocks by the intrusion of a mass of granite, and also to compare the phenomena of contact-metamorphism with those produced by other agencies in rocks of similar character at a distance from the granite.

On referring to the map of the Geological Survey of Cornwall, it will be seen that in the vicinity of Penzance the granite is surrounded by a belt of altered Devonian slates extending from St. Ive's Bay on the north coast to a point a little beyond Mount's Bay on the south; they also occur along the coast north-east of Cape Cornwall, and reappear in the same direction at Porthmear Cove and near Zennor. The so-called greenstones occur in four distinct groups, also round the outskirts of the same mass of granite, vizaround Penzance and in the other localities just mentioned. In all cases they are represented as occurring in the altered slates either at a short distance from the granite or in actual contact with it.
A microscopical examination of both these groups shows at once that they have all been highly metamorphosed, and that the alteration varies greatly in character and extent according to the nature of the rock and its distance from the granite. The change
On the Miocene Fossils of Haiti
Authors: Guppy R. J. Lechmere 
Published: October 2009

A
very
important memoir “On the Topography and Geology of Santo Domingo” has recently been published by Professor Gabb. Whatever tends to elucidate the geology of the island of Haiti must of course contribute to our knowledge of West-Indian and American geology generally, and may also throw further light upon some of the problems connected therewith which have not as yet been solved.

Santo Domingo is a republic occupying two thirds of the Island of Haiti. A very large portion of the territory comprised within its boundaries has been geologically surveyed and mapped out by Prof. Gabb and his assistants. The formations examined by them are classified as Postpliocene, Miocene, and Cretaceous. Eruptive rocks are also developed to a largo extent.
It is not my intention to speak of the geological part of Prof. Gabb's labours. That could only be done usefully by those acquainted with the country and conversant with its structure. My present business is with the palæontological portion of the work.
The Geological Society possesses the first regular collection of fossil Tertiary shells and corals made in Haiti, and, indeed, I might almost say, in the West Indies. This collection contains the types of the species described by Sowerby for Mr. Carrick Moore, and by Prof. Duncan. I have from time to time, when treating of the West-Indian Tertiary rocks and fossils, alluded to the fact that several of the species contained in that collection were unnamed.
Most of those species have now been described by Prof.
The Cephalopoda-beds of Gloucester, Dorset, and Somerset
Authors: Buckman J. 
Published: October 2009

Every student of the geology of the Cotteswolds has recognized a band at the base of the Inferior Oolite under the name of the “Cephalopoda-bed,” so named from the important list of Ammonites,
Nautili
, and Belemnites which it has been found to contain.

To quote from Mr. Hull's ‘Memoir on the Geology of the Country around Cheltenham,’ “This bed had been long known to geologists as ‘the ammonite bed;’ but the ammonites were supposed characteristic of the Inferior Oolite, and its true importance was overlooked. Dr. Wright, however, found that the species were identical with specimens from the Upper Lias of Whitby, in Yorkshire. About the same time the work of M. D'Orbigny made its appearance, wherein nearly all the cephalopoda from the ammonite bed are figured and described as ‘
Toarcien
,’ or Upper Lias forms, while even in our own district several of the species……were known to be characteristic of the Upper Lias Shale” (p. 26).

Mr. Hull refers to a paper by Dr. Wright in the ‘Proceedings of the Geological Society,’ vol. xii., in support of the view that the Cotteswold Cephalopoda-bed belongs to the Upper Lias and not to the Inferior Oolite, and, further, that the learned Doctor had traced it to the Dorsetshire coast; and, indeed, in this very paper we find the following remarks upon sections at Half-Way House and Bradford Abbas, which we quote, as showing that Dr. Wright had at this time identified the Dorset Cephalopoda-bed with the one in Gloucestershire.
“Between Yeovil and
Observations on the Later Tertiary Geology of East Anglia
Authors: Wood Searles V. , Harmer Frederic W. 
Published: October 2009

In writing the Introduction to the ‘Supplement to the Crag Mollusca,’ issued by the Palæontographical Society (for 1871), our object was, with the help of the Map and Sections accompanying it, to give only such a compressed or synoptical account of the researches on which we had for several years been engaged as would enable geologists to perceive the results at which we had arrived respecting the succession of the beds posterior to the Crag in the East of England. We considered that as the officers of the Geological Survey had commenced the examination of the district, and would eventually publish a detailed account of the sections and other evidence bearing upon that succession, we should have only encumbered scientific publications by bringing forward in greater detail the physical evidence which we had collected, and which had led us to the conclusions of which we thus gave a representation, the evidence of organic remains which we had collected being given by the author of the ‘Crag Mollusca’ in the tabular lists which accompany the Supplement to that work.
There are, however, some subjects referred to in that „Introduction„ upon which we have made subsequent observations that we desire to bring forward; and there is one in particular upon which we touched only slightly, the break between the Lower and Middle Glacial deposits, which from its geological importance it is desirable should be shown in some detail, in order that while the officers of the Survey are engaged upon the district
Note on the Red Crag
Authors: Whitaker William 
Published: October 2009

My work on the Geological Survey in the Crag District has led me to think that previous observers have made a slight error in the classification of a certain ferruginous sand that is often to be seen above the shelly Red Crag, the line of junction being mostly very irregular.
This sand has been described by Prof. Prestwich as an “upper division” of the Red Crag, or, to quote his own words, “owing to the want of all fossils in the neighbourhood of Ipswich, as the ‘unproductive sands’ of the Red Crag”; and he goes on to speak of the “erosion of the lower division” underneath this, afterwards classing the upper with the Chillesford sands.
Mr. S. V. Wood, Jun., has referred the ferruginous sand in question to various horizons in the Glacial Drift, I believe with a constant tendency to lower its horizon; but his former views need not be dwelt upon, as that tendency has continued until he has accepted my classification, and now regards this sand simply as Red Crag, not separated stratigraphically or palæontologically from the shelly mass below.
The so-called “eroded” surface of the shelly Crag, noticed by various observers, is, indeed, apparently so only; but I must say that in many sections there is little or nothing to throw doubt on the reality of the appearance, which is somewhat analogous to the “mimicry” sometimes seen in insect life, though in our case one cannot see any object to be served by the delusion, unless
On the Kessingland Cliff-section, and on the Relation of the Forest-bed to the Chillesford Clay, with some Remarks on the so-called Terrestrial Surface at the base of the Norwich Crag
Authors: Harmer F. W. 
Published: October 2009

In the “Outline of the Geology of the Upper Tertiaries of East Anglia,” given by Mr. S. V. Wood, jun., and myself in the volume of the Palæontographical Society for the year 1871, we called attention to the beds at the base of the Kessingland cliff and their relation to the Crag and Chillesford clay, and gave a section of them. Up to that time the cliff had been, at the time of our visit, more or less obscured by talus, so that some uncertainty existed as to the super-position of the different beds. After a storm in the month of November 1874, however, I was fortunate enough to find the section perfectly clear; and the result of my examination of the cliff was laid in the same month before the Geological Society of Norwich; but that body does not publish any record of its proceedings.
In all respects, so far as the sequence of the beds is concerned, this recent exposure confirmed the representation given by Mr. Wood and myself in 1871; but in one matter of detail, then left doubtful, some correction is necessary.
As Mr. Gunn has recently submitted to this Society a paper describing his view of the section, which, in my opinion, differs entirely from what was then so clearly revealed, I think it desirable to give a short account of the facts as they then appeared to me.
The beds present in the cliff-section I take to be, in ascending order, as follows:
On the Intrusive Character of the Whin Sill of Northumberland
Authors: Topley W. , Lebour G. A. 
Published: October 2009

1.
Introduction
.—The basaltic rocks of the north of England occur in two forms—as
sheets
lying amongst the sedimentary strata, and as
dykes
cutting through them. The intrusive character of the latter is, of course, undisputed; but there is much uncertainty in the minds of many geologists as to the character of the former.

In this paper we purpose to show, from the detailed work of the Geological Survey, that in Northumberland there can be no doubt whatever as to the intrusive nature of the bed or beds of basalt known as the Whin Sill. This conclusion can be established both by the evidence of individual sections and by the line of outcrop of the trap.
The question of the nature of the Whin Sill is of importance in three ways:—1st, as a point of theoretical geology, bearing upon the history of volcanic action in Britain; 2nd, in reference to the classification of the Carboniferous System; 3rd, in its bearing upon practical mining.
The Whin Sill is best known in Teesdale, especially in the two fine waterfalls of High Force and Cauldron Snout. It also appears along the face of the Penine escarpment, and is beautifully exposed in the “Nicks” which furrow the face of that range. Although this district is known to us, we will not stay to describe it, because it has already much engaged the attention of geologists, especially Professors Sedgwick and Phillips. It is generally supposed that there is but little evidence of intrusion there; but this
On the Strata and their Fossil Contents between the Borrowdale Series of the North of England and the Coniston Flags
Authors: Harkness Robert , Nicholson H. Alleyne 
Published: October 2009

In the following communication we propose shortly to consider the various groups of strata which intervene between the great volcanic series (Borrowdale Rocks) of the Lake-district and the well-marked band of sedimentary rocks to which Prof. Sedgwick applied the name of the “Coniston Flags.” In so doing we shall have occasion to note, in a general way, the physical characters and relations of the successive deposits in question; but we shall have to draw attention more especially to the organic remains which they contain and to some indications thus afforded as to their precise age and position in the geological scale.
The base of the great Silurian series of the north of England is constituted, as is well known, by the “Skiddaw Slates,” a thick mass of sediments, originally in the condition of black mud, clearly proved by their fossil contents to be of the age of the “Arenig group” of Wales. Succeeding the Skiddaw Slates there occurs a great series of volcanic products, termed by Prof. Sedgwick the “green slates and porphyries,” to which we have elsewhere given the name of “the Borrowdale series.” These consist of ashes and breccias, alternating with ancient lavas, a portion of the series being subaerial, whilst part is of submarine formation.
Throughout the greater part of this extent, for a thickness of some thousand feet, the Borrowdale series has hitherto proved unfossiliferous; fossils, however, make their appearance in a thin band of calcareous ashes near the summit of the group (Harkness and Nicholson
Supplementary Notes on the Fauna of the Cambridge Greensand
Authors: Jukes-Browne A. J. 
Published: October 2009

In a paper read before the Society in January 1875, I discussed the relations of the Gault and Chalk Marl in Bedfordshire and South Cambridgeshire, and endeavoured to show that the fossil contents of the so-called Cambridge Greensand are for the most part remaniés and have been derived from the upper beds of the Gault.
The conclusions arrived at were briefly these:—that the Upper Greensand does not extend further in a north-westerly direction than West-end Hill near Cheddington in Bucks; that stratigraphically the Cambridge Greensand is of no importance, being a mere nodule-bed at the base of the Chalk Marl; that it rests unconformably upon denuded Gault; that a greater portion of the fauna belonged originally to the Upper Gault; that the remainder, really belonging to the bed itself, are species proper to the Chalk Marl rather than to the Upper Greensand.
A full list of the species then known as existing in the formation was appended; and the derived forms were therein separated from those presumed to be indigenous to the Greensand itself. This list was mainly prepared from an examination of the large collection of fossils in the Woodwardian Museum; and my investigations resulted in the determination of many species that were previously unnamed in that collection, and in the identification of others which had been wrongly named. All these species were separately noticed, with remarks upon their determination and synonymy.
These observations, however, were by no means intended as an exhaustive study of the fauna of the
Note on some Recent Discoveries of Copper-ore in Nova Scotia
Authors: Gilpin Edwin 
Published: October 2009

A
lthough
for many years the presence of various ores of copper was known in this province, it is but recently that discoveries have been made of economic value.

In the early French expeditions to Canada and Acadie (now Nova Scotia) were men similar to those styled by Sir Humphrey Gilbert “rare refiners of miners;” and their reports on the supposed mineral wealth of Nova Scotia and Cape Breton excited much interest in Paris, and formed one of the reasons that France struggled so strongly to retain her supremacy in British America.
Lescharbot, writing in 1609, speaks of the native copper of the Bay of Fundy as being “very pure in the stone,” and adds, “many goldsmiths have seen it in France, which do say that under the copper-mine there might be a golden mine, which is very probable.”
The stone he alludes to is the trap associated with the Triassic sandstones of the Bay of Fundy; copper is found scattered through it in small grains and lumps, but has not yet been found in workable quantity. Although this trap resembles that from the famous Lake-Superior copper-district, the zeolites and other minerals characteristic of the Nova-Scotia trap are wanting in the Lake-Superior trap; and on no ground, so far I am aware, can any equivalence of age be established.
Passing over without notice the numerous unsuccessful attempts that have been made to open productive copper-mines in Upper and Lower Carboniferous strata, we find that the eastern part of the province gives
The Steppes of Southern Russia
Authors: Belt Thomas 
Published: October 2009

I
first
saw the steppes of Southern Russia in the spring of 1873, and under circumstances calculated to impress some of their peculiar features on my mind. I had, in company with a friend, crossed the Caucasus from Tints to Vladikafkas. We had travelled by the great military road through the pass of Dariel, and down the stupendously precipitous valley of the Terek. At Vladikafkas we came out on a vast plain, sensibly level as far as the horizon, and running in between and around the spurs of the mountains, like the sea around the headlands of a precipitous coast. I have since then travelled for thousands of miles over similar plains in Asiatic and European Russia; but the vividness of my first impressions of the steppe of Vladikafkas has not been dimmed, although my interest in the great plains has been increased by the personal experience I have since gained of their almost continental extent.

At Vladikafkas I saw no sections to a greater depth than 15 feet. These showed the upper surface of the plain to be composed of about 4 feet of black soil, resting on a fine grey loess-like clay, the base of which was not seen. I was only able to make a short search, and found no organic remains.
In 1875, and again in 1876, I travelled much in Southern Russia; and I propose to lay before the Society the information I have obtained respecting the extent, the constitution, the geological age, and the
On Terminal Curvature in the South-western Counties
Authors: Ussher W. A. E. 
Published: October 2009

M
ore
than two years ago my attention was drawn to this subject by the perusal of a paper by Mr. Mackintosh in vol. xxiii. of the ‘Quarterly Journal.’ Having in the interim neglected no opportunity of studying the phenomena in question over a large area, I arrived at conclusions adverse to those advocated by Mr. Mackintosh; so that the object of this paper is twofold :—first, to controvert Mr. Mackintosh's opinions; secondly, to put forward more tenable explanations. To carry out this object thoroughly is impossible without considering the Pleistocene history of Devon, &c., in some at least of its aspects; but as the wider subject is reserved for a future communication, I shall here only touch on it as briefly as possible.

P
art
I.

Mr. Mackintosh suggests four explanations of the instances of terminal curvature described in his paper*. They are as follows :—
1st. “Land-ice filling up the basin of the Bristol Channel” and travelling southward.
2nd. Floating ice, in bergs or in “any other form.”
3rd. “A swift oceanic current exerting a pressure on the underlying slates by means of a forcible drifting forward of detritus.”
4th. “A still more violent rush of waters caused by a sudden upheaval or depression of the land.”
The first of these alternative solutions finds most favour with their author. I do not deny its applicability to some instances of terminal curvature within three or four feet of the surface in glaciated districts; but in the South-western Counties, where evidence of
On Points of Similarity between Zeolitic and Siliceous Incrustations of recent Formation by Thermal Springs, and those observed in Amygdaloids and other altered Volcanic Rocks
Authors: Daubrée A. 
Published: October 2009

The production of zeolitic minerals by the agency of thermal waters is not, as might at first sight have been supposed, a merely accidental circumstance confined to a particular locality, but appears to be tolerably general in many places—and is therefore of particular interest, not merely as illustrating the changes that have gone on at the springs themselves, but as furnishing a clue to the origin of many of the components of erupted rocks, and more especially of altered volcanic rocks.

I.
Zeolites and allied minerals produced by Thermal Springs
.

The locality where these minerals were first observed as deposits from hot springs is Plombières* (Vosges); and subsequently I have discovered them under similar conditions in Roman masonry at Luxeuil† (Haute-Saône), at Bourbonne (Haute-Marne), and in the neighbourhood of 0ran in Algeria. At all these places the mouths of the thermal springs, when first utilized for baths during the Roman occupation, were surrounded by works in concrete formed of fragments of brick and stone, both sandstone and limestone, united by lime mortar. When, in the progress of recent works, it became necessary to cut into these masses of ancient masonry, it has been found that certain portions of them have, under the action of the mineral-water, undergone changes of a very remarkable kind, both in a chemical and mineralogical point of view, and of the following character‡.
In the vesicular cavities of the bricks new minerals are prominently developed, being principally zeolites, among the most abundant of which is chabasite