bluuebunny/crossref_metadata_2025_split huggingface dataset:
On the Lower Cretaceous Beds of the Bas-Boulonnais, with notes on their English Equivalents
Authors: Topley William 
Published: October 2009

T
he
following notes are the result of an excursion made, with my colleague Mr. Whitaker, in the summer of 1866, supplemented by two hasty visits by myself later in the same year.

To Mr. Whitaker and to M. E. Rigaux, of Boulogne, I am indebted for much assistance.

I. G
eneral
D
escription of the
D
istrict
.

The Bas-Boulonnais forms the easterly continuation of the English Wealden area, both being bounded alike by a well-defined escarpment of Chalk. The lowest beds exposed in the Weald have been doubtfully referred to the Purbeek formation; but none of undoubted precretaceous age occur therein on the English side of the Channel.
In the Bas Boulonnais the major part of the surface is occupied by Lower Secondary and Palæozoic beds, the Lower Cretaceous rocks occupying only a narrow border at the foot of the Chalk escarpment, and capping the hills in the interior. The Chalk falls away from the escarpment with a gentle slope. The Gault generally occupies a slight depression at the base of the Chalk hills; but, from its diminished thickness, the valley thus formed is far less striking than in Kent. The Lower Greensand is too thin to make a constant feature in the district; towards the south and south-east, however, it, togather with the underlying ferruginous sands, forms the range of hills which runs more or less parallel with the Chalk, but without making a well defined escarpment. The hills of the central district, which are capped by ferruginous sands (Wealden), are mostly
On worked Flint Flakes from Carrickfergus and Larne
Authors: Du Noyer G. V. 
Published: October 2009

Abstract

T
hese
flakes have been found by the author in two very distinct positions, namely:—the older in the marine drift (sand and gravel) skirting the shores of the county Antrim and county Down, the maximum elevation being about 20 feet above the sea; and the more recent in the subsoil-clay at all elevations up to 600 feet, near Belfast, Carrickfergus, Larne Lough, and Island Magee. The former are of the rudest forms, highly oxidized or white on their entire surface, but, though imbedded in marine drift, having the chippings around the sides and angles generally sharp. The latter have a comparatively fresh look, though still possessing the characteristic porcellanous glaze; they are regarded by Mr. Du Noyer as possibly the rough materials out of which the historic races in Ireland manufactured the spear- and arrowheads which are found with their sepulchral and other remains.
On the Diminution of the Volume of the Sea during past Geological Epochs
Authors: Murray Andrew 
Published: October 2009

Abstract

T
he
author regards Mr. Darwin's theory of Coral islands as imperfect, from not recognizing the fact of a gradual diminution of the amount of water on the face of the earth. He objects to Mr. Darwin's explanation of the mode in which the islets appear above the water, namely, the dash of the waves breaking the reef, and their wash piling up the débris until it forms dry land; and he quotes the objections of M. de Rochas to the same theory. The opinion of the latter author was that the islands had been raised by a movement of upheaval; but Mr. Murray considers this still more improbable, as we are dealing with a large number of islands scattered over an immense space, and all at one uniform level, only a little above the surface of the sea; while the amount of all known elevations is irregular, and increases towards some axis of elevation.

Mr. Murray believes the true explanation to be that the sea is gradually diminishing in volume; and he regards the Coral islets as a proof that it is so, at any rate, he remarks that if we apply this condition of things to an area of coral reefs, all as near the surface of the sea as the polyps can make them, we should have a result exactly in accordance with the state of things now existing in Polynesia.
The author then states that the fossils of the older formations being wholly marine, and the thickness of those formations largely exceeding those of later periods, afford evidence in support of the view that the globe was then enveloped in water. In opposition to Sir Charles Lyell's view, that the proportion of dry land to sea was always the same, and the volume of the land above the sea a constant quantity, he maintain that the latter is constantly increasing, and that both the mean and the extreme depth of the sea are constantly diminishing; and he believes the cause of this constant diminution to be the extreme affinity which water has for the constituent elements of minerals.
Mr. Marray is careful to state his admission that whether there be more or less free water now than at the beginning, there can be neither more nor less of the elementary constituents out of which it is composed. He then refers to volcanic action as showing that the process of the cooling of the earth's crust and the attendant abstraction of water the surface are still going on; and he remarks that although not a particle of water can be present in the molten mineral core of the earth, yet every particle of that core will, when cool, be largely composed of water—and that therefore the amount of water on the surface of the earth must continue to diminish until the earth is cool or the water wholly absorbed. In conclusion, he quotes the case of the Moon as one in which this process of absorption of not only its water, but of its atmosphere also, has been brought to a conclusion.
On the Occurrence of Celestine in the Nummulitic Limestone of Egypt
Authors: Bauerman H. , Foster C. Le Neve 
Published: October 2009

T
he
fact of the occurrence of sulphate of strontia in the Eocene rocks forming the great escarpment of Mokattam to the east of Cairo has already been noticed by geologists, the latest and most complete account being that contained in Dr. Fraas's description of the Tertiary strata of Egypt*. The object of the present communication is to furnish some additional particulars in connexion with the position and mode of occurrence of the mineral.

The Mokattam escarpment forms a long connected line of cliff, for the most part nearly inaccessible in front, but which can be easily ascended from some of the numerous lateral ravines. The highest point even commands the old citadel, and has therefore been fortified. The height is probably about 800 feet above the Nile; that of the citadel being 567 feet, by a single barometrical observation. The beds are almost fiat, having but a slight dip towards the desert. In a northerly direction the hill diminishes rapidly in height until it is covered by the red quartzose millstone-rock of Jebel Achmar.
Apart from palæontological considerations, the Nummulitic escarpment, owing to a well-marked physical division, may be divided into two parts, the white and the brown beds, the latter being the higher member of the group. The lower, or white beds, are said by Dr. Figari Bey†, to rest upon tufaceous and slightly argillaceous limestone, representing the upper part of the Cretaceous formation.
The following is the observed section in ascending order, commencing in a quarry at the
On some Fossils from the “Menevian Group”.
Authors: Salter J. W. , Hicks Henry 
Published: October 2009

D
escription
of some of the principal fossils of the Menevian formation, including the large
Paradoxides
(
P. Davidis
), appeared in the Quarterly Journal of the Society for August 1864, and others in the number for November 1865; but as many new forms have been obtained since then, a large number yet remain to be described. The continued research, carried on by one of the authors, in the typical locality, St. David's, has been the means of discovering the whole of these new forms, many of which, however, have been subsequently found in various other places. Around the Merionethshire anticlinal ridge of Lower Cambrian rocks large collections have been made:—on the north side, near Maentwrog, and at Tafarn Helig, near Trawsfynydd, by Messrs. D. Homfray and R. A. Eskrigge; and on the south side near Dolgelly by Messrs. T. Belt, E. Williamson, J. Plant, and J. C. Barlow,—all of whom have also done something towards defining the boundaries of the group in North Wales. Much also has been done by us, in like manner, in South Wales, and many new localities have been found to be occupied by this interesting group.

The range of some of these fossils has been more clearly ascertained, and greatly extended. They are not in any way limited to the black Lower Lingula-shales, but occur also in the hard grey rocks which form the upper bands of the Harlech grits.
One of the authors has recently found both Trilobites and Shells in a series of red and
A Description of the “Broads” of East Norfolk, showing their Origin, Position, and Formation in the Valleys of the Rivers Bure, Yare, and Waveney
Authors: Grantham Richard B. 
Published: October 2009

T
he
author described the “Broads” of East Norfolk as large lakes of fresh water situated in the valleys of certain rivers, such as the Bure, Yare, and Waveney, although never directly in their course, the distance of the Broads from the above-mentioned rivers being from one quarter of a mile to three miles. They are, however, connected with the rivers by watercourses. The Broads in the valleys of the rivers Bure, Yare, and Waveney are thirty in number, twenty-three of which are in the valley of the first-named river. The author gives the following list of them with their areas in acres:-

The aggregate area amounts to 2816 acres.
Many of the Broads are being reduced in size by the deposition of decaying vegetable matter, and the accumulation of detritus brought into them by the small streams which feed them. The bottoms of Martham, Hickling, Whitesley, and Horsey Broads are about on the level of low water at Yarmouth; the bottom of the united Ormesby, Rollesby, and Filby Broads is from 12 to 14 feet below that level. The surface of the water in the last-named Broad is about 2 or 3 feet above that of high water.
The author maintains that the “Broads,” although freshwater lakes, are relics of a time when the whole of these valleys were submerged, and in fact formed great estuaries. He instances the saltwater lake called Breydon Water, which lies on the west of Yarmouth, and to which the tide still has access; this
On the Geology and Mineralogy of the County of Hastings, Canada West
Authors: Wallbridge T. C. 
Published: October 2009

I. I
ntroduction

W
ithin
the last two or three years, considerable excitement has been aroused by the discovery of gold in several localities in the North Riding of the County of Hastings. Long previously, attention had been directed to the occurrence of valuable deposits of iron-ore distributed through the northern townships of the county; but although attempts have been made from time to time to explore a few of these deposits, no systematic or extensive workings have yet been undertaken, and at the present time these iron-ores remain almost entirely undeveloped, Looking, however, to the extensive mineral resources of North Hastings, and to its favourable geographical position, it can hardly be doubted that mauy of the townships are destined to become important mining-districts; and the object of the present communication is to lay before the Society an account of the chief mineral deposits, so far at least as they admit of description in their present undeveloped state.

Before describing these minerals, however, it seems desirable, for the better understanding of their mode of occurrence, to give a general sketch of the geological features of the country. Much information on this subject may be found scattered through the pages of the admirable Reports issued by the Geological Survey of Canada; but the following description is mainly the result of personal observation and local knowledge derived from a long residence in that part of Canada.
The County of Hastings is situated on the north shore of the Bay of Quinté in Upper Canada.
On the Distribution of Flint Implements in the Drift, with reference to some recent Discoveries in Norfolk and Suffolk
Authors: Flower J. W. 
Published: October 2009

Abstract

T
he
author noticed some recently discovered localities in the valley of the Little Ouse which have yielded Flint Implements, viz. at Broomhill, about 350 feet from, and 5 or 6 feet above the level of the river; at Gravel Hill, about 1 mile from, and 60 feet above the river; at Shrub Hill, about 1 mile from, and only a foot or two above the river; and at Lakenheath, nearly 3 miles from the river, and 60 feet above it. In the first three of these localities the worked flints are in coarse gravel, resting immediately on the Cretaceous beds (chalk in the first and second, gatflt in the third), and overlain by regular deposits of gravel and sand. The implements resemble those of St. Acheul, Thetford, and Salisbury, but present some peculiarities, from which the author inferred that each place might have had its own workmen, and that the different forms were intended to answer different purposes. At Brandon some implements formed of quartzite had been found in a bed consisting of rounded quartzite pebbles mixed with about one-fourth of flints. Flint implements occurred beneath this bed.

The author described the geographical characters of the district and the peculiarities in the distribution of the flint implements, which he regarded as in accordance with the phenomena presented by the valley of the Somme; and he argued, from the presence of rocks of foreign origin and other considerations, that the implement-bearing gravels were not transported to their present situation by the agency of the rivers in whose valleys they occur, but that the implements were made upon the spot, exposed upon the surface with the gravels in which they are found, and from which they were made, and finally covered up by the gravels and sandy beds which now overlie them.
On the Geology of the Diamond-Fields of South Africa
Authors: Shaw John 
Published: October 2009

We have presented in the various parts worked for diamonds up to the present date two apparently different classes of soil in which diamonds are found imbedded. The one class exists along the Vaal River and its tributaries, the Reit and Hart Rivers; and the other occurs in the Orange-River Republic, in isolated spots, generally circumscribed, and in many cases in what are called “Pans,” which are basin-like hollows, in wet seasons more or less filled with water of a saline character, in dry seasons presenting a whitish surface saturated with salts.
I shall endeavour to show that there is really no distinction in the geological origin of the two classes. It will be convenient, however, in the first place to treat them separately, for the sake of clearness.

The prevailing rocks of the Vaal region and the isolated diamond-farms are
trappean
—greenstone and basalt. There is every indication that the upheaval of these has been continued throughout a vast length of time, and has extended until recently, geologically speaking. The summits of the hills consist of trap, which has been protruded through vast layers of sedimentary strata—generally calcareous sandstones, clay-slate, and such like rocks, all remarkably barren of fossils, Very little disturbance is shown in the lie of these sedimentary rocks. Hence the prevailing character of the ranges is tabular, though dome-like, conical, and even pointed peaks are seen. They are dispersed more or less circularly around dreary flats, which are in many instances of considerable extent. The trap, intruded
Further Remarks on the Relationship of the
Xiphosura
to the Eurypterida and to the Trilobita and Arachnida
Authors: Woodward Henry 
Published: October 2009

I had, on a former occasion (November 21, 1866), the honour to communicate a paper to this Society “On some points in the structure of the Xiphosura having reference to their relationship with the Eurypterida”, in which were discussed the grounds for the union of these two suborders (afterwards dealt with in greater detail in the monograph of the Merostomata in the Palæontographical Society's publications for 1866). I therefore venture to think it may not be considered inappropriate if I bring the subject again under your consideration after an interval of five years, during which time some considerable additions have been made to our knowledge of this group.

The papers to which I shall have occasion especially to refer are the following:—

1.

“On a New Limuloid Crustacean (
Neolimulus falcatus
) from the Upper Silurian of Lesmahagow, Lanarkshire.” By H. Woodward. (Geol. Mag. 1868, vol. v. pl. i. fig. 1, p. 1.)

2.

“On some new Species of Crustacea from the Upper Silurian Rocks of Lanarkshire, and further Observations on the Structure of
Pterygotus
.” By H. Woodward. (Quart. Journ. Geol. Soc. 1868, vol. xxiv. pis. ix. & x., p. 289.)

3.
“Notes on some Specimens of Lower Silurian Trilobites.” By E. Billings, F.G.S. (Quart. Journ. Geol. Soc. 1870, vol. xxvi. pls. xxi. & xxii., p. 479.)

4.

“Note on the palpus and other Appendages of
Asaphus
from the Trenton Limestone, in the British Museum.” By Henry Woodward. (Quart. Journ. Soc. 1870, vol. xxvi. p. 486.)
On the River-courses of England and Wales
Authors: Ramsay Andrew C. 
Published: October 2009

In the following paper I propose to show the origin of many of the principal rivers of England and Wales—that is to say, what are the special geological causes the operation of which led them to flow in the general directions they now take. I am not aware that any attempt has heretofore been made to do this on a large scale, though I have already done something on the subject with regard to the rivers of the Weald, in which line of argument I was afterwards followed by Mr. Foster and Mr. Topley.
I shall begin the subject by a rapid summary of certain physical changes that affected the English Secondary and Eocene strata, long before the Severn (leaving the mountains of Wales) took its present southern and south-western course along the eastern side of the palæozoic rocks that border that old land.
About the close of the Oolitic epoch the strata of these formations were raised above the sea, and remained a long time out of water; and during that period those atmospheric influences that produced the sediments of the great Purbeck and Wealden delta were slowly wearing away and lowering the land, and reducing it to the state of a broad undulating plain. At this time the Oolitic strata (till abutted on the mountain country now forming Wales and parts of the adjacent counties. They also completely covered the Mendip Hills, and passed westwards as far as the hilly ground of Devonshire, running out between Wales and
On Modern Glacial Action in Canada
Authors: Bleasdell William 
Published: October 2009

Second Article
.

Further inquiry into the action of ice in Canada furnishes new facts illustrating the powerful effects of this agent in changing or modifying the Boulder-drift surfaces of the country lying over the Silurian strata, even during the period of human observation; and if so, how much more of change must have been effected in this way during that comparatively long period which, as far as Canada is concerned, may be designated prehistoric, when it lacked observers to note, and a written language to record, those changes which must have occurred in the bygone centuries of its existence in its present form, and subject to the same powerful glacial agencies and climate? In addition to the facts furnished to the Geological Society, and kindly received by it, in my previous paper†, I am now in a position to lay before the Society further evidence of this nature.
At the head of that arm of Lake Ontario named the Bay of Quinte, the Canadian river Trent discharges its waters at the village of Trenton; and a mile above the latter the lower or Frankford Rapids terminate. These rapids extend for about nine miles up the river, from this point to a mile above the village of Frankford, where there is again deep and navigable water. Between these two points the river runs over a limestone bed of the upper Trenton series of the Lower Silurian rocks, and the rapids are thus formed. At intervals small islands exist in what are
Note on the Relations of the Supposed Carboniferous Plants of Bear Island with the Palæozoic Flora of North America
Authors: Dawson J. W. 
Published: October 2009

I have only recently received the May number of the ‘Geological Journal’, containing the interesting paper of Dr. Heer on the plants above mentioned, and beg to request permission to address to the Society a few remarks on their supposed equivalency with the American Devonian Flora.
The plants catalogued by Dr. Heer, and characterizing what he calls the “Ursa Stage,” are in part representatives of those of the American flora which I have described as the “Lower Carboniferous Coal-measures” (Subcarboniferous of Dana), and whose characteristic species, as developed in Nova Scotia, I noticed in the Journal of the Geological Society in 1858 (vol. xv.). Dr. Heer's list, however, includes some Upper Devonian forms; and I would suggest that either the plants of two distinct beds, one Lower Carboniferous and the other Upper Devonian, have been near to or in contact with each other and have been intermixed, or else that in this high northern latitude, in which (for reasons stated in my Report on the Devonian Flora) I believe the Devonian plants to have originated, there was an actual intermixture of the two floras. In America, at the base of the Carboniferous of Ohio, a transition of this kind seems to occur; but elsewhere in North-Eastern America the Lower Carboniferous beds are usually unmixed with the Devonian.
Dr. Heer, however, proceeds to identify these plants with those of the American Chemung, and even with those of the Middle Devonian of New Brunswick, as described by me—a conclusion from which I
Further Notes on the Punfield Section
Authors: Meyer C. J. A. 
Published: October 2009

In a paper read before the Society in March 1872, I stated my conviction that the so-called “Punfield Formation” of the Isle of Purbeck was superior in position to the “Lobster-clay” of Atherfield—or (to state the matter more clearly) that the Punfield beds, from the “marine band” upwards, were Lower Greensand instead of Wealden, representing, however, only so much of the Lower Greensand of the Isle of Wight as would be included between the “Lobster-clay” and the Gault.
The assertion was a bold one, and should, I am well aware, have been supported at the time by fuller evidence. It was not, however, put forward thoughtlessly; and I have now to offer such further evidence as may tend towards a settlement of the points in question.

To test the truth or error of my impressions with respect to the relation of the Isle-of-Wight
Wealden
and
Neocomian
strata to those of Punfield, I revisited the coast-sections at Redcliff and Atherfield, and spent several days in studying the corresponding strata in Compton Bay. I sought carefully in either formation for such change in its passage westward as might indicate the relation of either to the marine, or semi-marine, Punfield beds of the Isle of Purbeck.

The Wealden beds showed no such change. But for slight variations in thickness and disposition, these Upper Wealden shales of the Isle of Wight are almost perfectly alike at Compton Bay, at Sundown, and at Atherfield. The section of the Wealden strata of Compton Bay, at Sandown