bluuebunny/crossref_metadata_2025_split huggingface dataset:
On the Structure of the Red Crag
Authors: Wood S. V. 
Published: October 2009

Mr. Prestwich has, I believe, for several years inclined to the opinion that the Red and Fluviomarine Crags are coeval; but, so far as I am aware, he has not expressed that opinion in print. In 1863 my son had arrived at a similar conclusion; and in a paper by him, published in the ‘Ann. & Mag. Nat. Hist.’ for March 1864, he showed that the Chillesford beds overlie alike both the Red and Fluviomarine Crags, and that the Red Crag itself was not all of one age, but divisible into distinct portions, the uppermost of which he regarded as newer than the Fluviomarine, and intermediate in age between it and the Chillesford beds.
In December 1864 another paper by my son was read before this Society (but was afterwards withdrawn, and an epitome of it, together with a map of the Upper Tertiaries of the East of England, printed for private circulation), wherein he contended that the so-called Weybourne Crag, the Cromer Boulder Till, and the Contorted Drift formed a separate series, to which he assigned the term “Lower Drift,” and that this in common with the Red and Fluviomarine Crags was overlain by the great body of sands which intervene between the Crag and the Boulder-clay, and to which he applied the term “Middle Drift,” distinguishing the Boulder-Clay as the “Upper Drift.”
In November 1865 a paper, by the Rev. O. Fisher, was read before this Society (and published in their ‘ Quarterly Journal,’ Feb.1866), wherein he contended
Note on Supposed Remains of the Crag on the North Downs near Folkestone
Authors: Bristow H. W. 
Published: October 2009

On
my return to London, after an excursion made in May 1857, in company with Sir Charles Lyell, Professor Ramsay, and Messrs. Prestwich and Godwin-Austen, to the district of Kent, from which fossils had been got which were thought to be of the age of the Crag, I made a memorandum on the subject, of which the following is a copy:—

“With regard to the sands, &c., seen at Paddlesworth and elsewhere, accompanied by thin bands of iron-grit, I have seen nothing from which it would be at all reasonable to infer that the beds in question were any other than those of the Lower Tertiary (that is, of the Woolwieh and Reading series), occurring in their proper position on the denuded surface of the Chalk.
“Beds like the Paddlesworth ferruginous sands':occur in the Hampshire Basin, where a part of the Woolwich and Reading series is represented by ferruginous clayey sands, with masses of ferruginous grit, &c*. Another strong resemblance is also borne by these last beds to those of Paddlesworth in the red colour of the sands, as may be observed more particularly at Whiteparish, in Wiltshire, where it would seem that when the mottled clays are replaced by sands the colouring matter is often persistent although the mineral character of the rock varies. With regard to the greater development of ferruginous grit at Paddlesworth, that alone is not enough to afford reliable evidence one way or the other, and in either case it might be a mere local
On the Warp (of Mr. Trimmer)—its Age and probable Connexion with the Last Geological Events
Authors: Fisher O. 
Published: October 2009

I am not aware that any geologist since the late Mr. Trimmer has devoted a paper to the elucidation of the subject of what he has called the “warp” or the “warp of the drift”. In his paper “On the Soils of Kent” he lamented the slight attention that had up to that time been paid to “the period which intervened between the desiccation of the bed of the glacial sea and the commencement of the historic era of geology.” Had Mr. Trimmer lived until the present day, he would have seen the earlier part of that period receive at least its due share of attention. The closing portion of it, which saw the formation of that warp or subsoil on which the fertility of our fields chiefly depends, has not, so far as I know, received any particular attention since Mr. Trimmer's valuable labours were pre-maturely terminated.
My attention has for some time past been attracted to this subject, and in my paper on the Brick-pit at Lexden I hinted at its importance as containing records of the latest geological changes.
Mr. Trimmer appears not to have arrived at any satisfactory conclusion as to the causes which have produced the warp. He says, “The majority of soils and subsoils in the British Isles are composed only in part of the débris of the rocks on which they rest, and in part of materials transported from various distances by forces of considerable intensity, differing from ordinary atmospheric action, which were
On the Affinities of
Chondrosteus
, Ag.
Authors: Young John 
Published: October 2009

Abstract

The object of this communication was to show, from the characters of the skeleton, that
Chondrosteus
belongs not to the Chondrostean division of the ganoids as stated by Agassiz, but to the Holostean division, since it possesses a well-ossified basioccipital; and the lateral walls of the cranium are composed of bones answering to the cartilage bones of ordinary Teleosteans.
On Supposed Glacial Markings in the Valley of the Exe, North Devon
Authors: Whitley N. 
Published: October 2009

I
n
a late paper on the grouping of the rocks of North Devon, Professor Jukes mentions some glacial grooves observed by him in the valley of the Exe. The interest attached to this subject in such a country induced me to visit the spot; and in driving down the valley I found the “grooved” rocks about half a mile above Barlynch Abbey, and on the north face of a projecting tongue of hard purple grits. Two separate portions of the rock were deeply indented; and the long straight furrows, like a bold cornice of a room, might, on a hasty view, be set down as large glacial striæ; a nearer inspection, however, soon dispels this opinion.

1. The “grooves” (I use the term for convenience) are not
parallel to the bottom of the valley down which the glacier was
supposed to slide, nor do they on the two pieces of rock run in the
same direction (fig. 1).
2. The “grooves” may be traced into, and under, a portion of the overlying rock;
and it becomes obvious that they were exposed, not by the action of ice grinding down the overlying
rock, but by the tool of the workman removing the rock above in order to form the new road cut as a
bench along the steep hillside.
3. The cross section of the beds, of which I give an enlarged sketch (fig. 2), shows that the
“grooves” are formed by the minor folds of the
On Disturbance of the Level of the Land near Youghal, on the South Coast of Ireland
Authors: Wynne A. B. 
Published: October 2009

T
he
region which has undergone recent disturbance in the neighbourhood of Youghal is a part of that referred to in Prof. Jukes's able paper read before the Geological Society “Upon the Mode of Formation of some of the River-Valleys in the South of Ireland” (see Quart. Journ. Geol. Soc. vol. xviii. p. 378, 1862) with a map, to which I refer more particularly, as upon it Youghal Bay, at the mouth of the river Blackwater, will be found marked.

In this paper (p. 398) is the following:—“The South of Ireland, however, seems to have been exposed as dry land ever since the close of the Palæozoic epoch, with the single exception of the depression which it suffered beneath the sea during the Pleistocene or Glacial period.” To some time during this Glacial period, therefore, evidences of disturbance of level might be referred if they consisted of nothing more than the usual phenomena connected with the Glacial Drift. It will be seen, however, from what follows, that considerable alterations of level have taken place along the coast of Youghal Bay subsequently to the formation of the recent peat which so commonly covers the Glacial Drift of Ireland.
The occurrence of submerged peat beneath Youghal Strand is mentioned at some length by Dr. Charles Smith in his ‘History of Cork,’ 1749, book ii. chap. 1, where it is recorded that “good turf is dug every season, and also great quantities of timber trees, as fir, hazel, &c.,” from beneath the strand, and
On the Geology of the Princes Islands, in the Sea of Marmora, Turkey
Authors: Swan W. R. 
Published: October 2009

1.
Introduction
.—It was during a visit to Prinkipo, the largest of the Princes Islands, in the summer of 1864, that I first had an opportunity of studying the geological features of that island; and the discoveries I then made were of so interesting a character as to induce me to continue the examination of the remaining eight islands.

Before going into a detailed account of each island, I will here relate some of the chief points of interest met with, namely:—

(1.)
The existence of a considerable tract of Devonian strata, partly fossiliferous, in several of these islands, of an age different from that of the beds of the Bosphorus, which latter I have already shown, in a former paper to the Geological Society†, to belong to the lowest of the Devonian series of the Rhine. Also the existence of the remains of “fish” in the above strata, and an ancient “coral reef.”

(2.)
That the rocks which form the remaining portions of these islands are trachytic, and of younger age than the Devonian strata.

(3.)
That the trap rocks of these islands are of younger age than the trachytic.

(4.)
That the quartz rocks, of which some of the islands are largely, and some entirely composed, are altered sandstones of Devonian age, which clearly explains the occurrence of similar quartz rocks on the Bosphorus, which are seen in the mountains of Bulgurlou and Tchemlidja, behind Scutari, and referred to by Mr. Hamilton in his “Observations on the
On the Origin of Smoothed, Rounded, and Hollowed Surfaces of Limestone and Granite
Authors: Mackintosh D. 
Published: October 2009

Abstract

T
he
author, believing that late discussions on denudation have reached a stage which requires that the respective claims of rain-water and sea-waves to mould rock-surfaces should, as far as possible be set at rest, proceeds to state the results of his observations as follows:—

“Unless rain-water be retained for a certain length of time in previously formed hollows, it can exert little or no chemical influence on rock-surfaces; and therefore the principal, if not all, the inequalities found on the sloping or vertical sides of fragments, blocks, or faces of rock must be either the original fractured surfaces, or produced by some kind of mechanical action. Rain-water, uncharged with solid matter, such as sand, can exert little or no mechanical power on hard rocks. The chemical action of rain-water can enlarge previously formed hollows; and where retained for a sufficient time, it can dissolve out fossils, and develope the structural form of rocks. Rain-water, not concentrated into streams of sufficient force, can never, either chemically or mechanically, produce a smooth and regular surface by shaving away hard and soft parts alike, or by cutting equally through crystals of a different nature, but must always leave a surface minutely corresponding to the denudability of the parts (of the crystals) of rocks; it can only roughen, or leave a surface more or less zigzag in profile. In Devonshire and elsewhere, on all granites used in building, atmospheric weathering leaves a surface rough in proportion to the size and varied nature of the crystals, and never a smooth or uniformly curve outline.”
On a Striking Instance of Apparent Oblique Lamination in Granite
Authors: Mackintosh D. 
Published: October 2009

Abstract

I
n
this paper the author draws attention to the resemblance, at first sight, presented by many of the tors and cliffs of granite on Dartmoor, to the forms assumed by the Millstone-grit in yorkshire, and states that, among the former, the apparent lines of lamination and stratification are often as distinctly marked as in the latter. His object, however, is not to defend a theory, or to deny that certain granites may he of directly igneous origin and intrusive, but to bring into notice several phenomena in which the
linear structure
of granite seems to suggest the idea of original aqueous deposition:—(1) a semidetached portion of one of the ranges of cliffs called Hountor Rocks, in which there is the appearance of strata embracing laminæ, the second stratum obliquely denuded, a third thrown down on an inclined plane, and horizontal deposition resumed in the fourth or uppermost stratum; (2) the Kestor Hock, near Chagford, the apparent lamination of which is, in several places, obliquely crossed by fractures of the nature of joints; (3) the Blackenstone Rock, which presents a very regular series of beds; (4) the Hey Tors, especially the western boss of rock, in which two very different kinds of granite are separated by a distinct line parallel to the lines of apparent lamination and stratification below and above.
On the Structure of the Crag-beds of Norfolk and Suffolk, with some observations on their Organic Remains.—Part I. Coralline Crag
Authors: Prestwich Joseph 
Published: October 2009

Abstract

T
he
history of the division of the several crag-deposits into three formations (the Mammaliferous, Red, and Coralline Crags) having been recounted, the author states that for the last thirty years the evidence of their sequence has remained unaltered, the distinction between the Mammaliferous and Red Crags being still purely palæontological, not a single case of superposition having been discovered. Mr. Prestwich then proceeds to the special object of this paper, which is to describe more fully the physical structure of the several crags, and to determine, if possible, the exact relation which the Suffolk Craffs bear to the Crag of Norfolk.

Commencing with the Coralline Crag, the author states that the well-known outlier at Sutton furnishes a base-line and the best clue to its structure and dimensions, showing also the depth to which it has been denuded and replaced by the Red Crag. The Coralline Crag is generally described as consisting of two divisions:—an upper one, formed chiefly of the remains of Bryozoa; and a lower one, of light-coloured sands with a profusion of shells: and the author now gives their exact dimensions and his proposed subdivisions, as follows:
On Volcanoes in the New Hebrides and Banks's Islands
Authors: Atkin Joseph 
Published: October 2009

B
etween
166° and 170° east long., and the parallels of 13° and 21° south lat., is the chain of volcanic islands called the New Hebrides. The Banks's are another small group to the north, and the Torres are five low islands to the north-west. Of the New Hebrides, Tanna, Lopevi and Ambrym are now active volcanoes; of the Banks's Islands, Santa Maria and Great Banks's Island.

At Great Banks's Island there are boiling springs, and a great number of little vents discharging hot sulphureous vapour. At Santa Maria there is only one of these. A great part of the interior of the large island of Ambrym seems perfectly bare of vegetation. The present volcanic action is on the east slope. No crater can be seen, but all the active eruption is in a part two or three miles in extent. It seems to be constant, and violently active. There does not seem to have been any lava-stream recently; but the whole western coast of the island is formed of large irregular masses of lava. There is a fringing reef of coral on the eastern side of Santa Maria, and a short one at the north end of Ambrym.
The Island of Lopevi is not more than two miles and a half long, and is upwards of 5000* feet high; from some points it appears as a perfect cone. It was not known to be active until 1863, when its peak, formerly quite sharp, appeared to have been broken off, and
On the Quaternary Gravels of England
Authors: Tylor Alfred 
Published: October 2009

Abstract

M
r.
Tylor first compares the gravels of the Aire Valley at Bingley, of the Taff Vale between Quaker's Yard Junction and Aberdeen Junction, and of the Valley of the Rhonda near its junction with the Taff. He then describes the cave-section of Bacon Hole, Gower, and the sections exposed at Crayford, Erith, and Salisbury, comparing the angles of deposition of gravel-beds concealing the escarpment of the Chalk in these last three localities with the same conditions at Brighton and Sangatte.

By comparing the gravel-beds at different levels, and upon strata of different age and configuration, he shows in what respect they differ from each other. The bulk and height of the Quaternary deposits have strengthened the conviction which he expressed in his previous paper (on the Amiens Gravel), that there was a long period, reaching nearly to the Historical epoch, in which the rainfall was excessive, and which he termed the “Pluvial period.”
These sections also lead the author to the following conclusions:—(1) That the débris was deposited by land-floods, and that the mode of deposition was quite distinct from that of moraines produced by the melting of ice. (2) That the character of the deposits in the valleys of the Aire, Taff, and Rhonda proves that they were formed under similar conditions. (3) That these gravel-beds point to a Pluvial period of great intensity and duration. (4) That the ice-action of which there is evidence was subordinate to the aqueous action. (5) That the fossiliferous Quaternary deposits have been best preserved where they have been formed in cavities lying between the edge of the bank of a river, estuary, or sea and an escarpment running parallel with it at no great distance. (6) That the immediate source of the gravels was the high land adjoining the rivers, whence they have been washed down by rain, with the assistance of lateral streams, into the lower ground, where they had come into contact with larger quantities of running water, had been mixed with rolled materials, and spread in thick beds over the bottoms and slopes of valleys or the sides of escarpments. (7) That the surface of such a deposit rarely slopes at more than from 2° to 4° while the slope of the beds lower in the series nearer the escarpment averages 12° The escarpment is usually concealed under a coating of gravel or loess.
On the eruption of the Kaimeni of Santorin
Authors: Schmidt J. S. Julius 
Published: October 2009

D
uring
my first journey to Santorin, in February and March 1866, I communicated a general outline of this remarkable eruption, which commenced at the end of January 1866, and has since been visited and described by observers from different parts of Europe. These include the members of the Athens Commission, Messrs. Fouqué and Tauzen, Baron von Seebach, and Messrs. Fritsch, Reiss, and Stübel. From time to time information has been received on the subject, and everything has tended to show the extreme desirability of accurate measurements. Up to the close of 1867 the eruption continued without a day's (perhaps without an hour's) intermission. There has also been no cessation in the growth of the lava-deposit on the south side of the Nea Kaimeni, and there seems every probability that some years may elapse before the volcanic energy of the island will have altogether died out.

On the 4th January 1868 I arrived at Santorin, in the Austrian gunboat “Dalmat,” commanded by Baron Wickede. We anchored at Bancho, a little to the east of Mikra Kaimeni. Here we remained until the evening of the 9th January, and were fortunate enough to complete our observations in very fine weather.
For want of instruments, my own observations were limited to temperature and to taking sketches of the recent formations. Many hours, both of the day and night, were occupied in determining the exact nature of the eruptions of the George volcano, and in approximately making out their periodicity.
The most essential part of
On
Dakosaurus
from the Kimmeridge Clay of Shotover Hill
Authors: Mason J. Wood 
Published: October 2009

Abstract

T
he
Kimmeridge Clay of Shotover Hill has yielded five specimens of the teeth of this reptile, now for the first time represented as a British genus. After noticing the bibliography of the subject, and the presence of specimens in various museums, the author proceeds to describe the characters of the teeth. They are large, conical, incurved, and slightly recurved, having two sharp, prominent, crenulated, longitudinal ridges, which are situated midway between the convex and concave curvatures.

This reptile is regarded by the author as foreshadowing the form of dentition that characterizes the existing group of
Varanidœ
. If the materials were at hand for a complete definition of its comparative osteology,
Dakosaurus
would probably exhibit a combination of Lacertilian and Crocodilian characters, but with the crocodilian elements predominant.
On the Succession of Beds in the “New Red” on the South Coast of Devon, and on the Locality of a New Specimen of
Hyperodapedon
Authors: Whitaker William 
Published: October 2009

T
he
following account of the successive beds that are shown in the “New Red” cliffs of South Devon, is from notes taken during a holiday-walk along that coast last September, and it has been drawn up at the request of Prof. Huxley, in order to mark the stratigraphical place of the
Hyperodapedon
jaw from near Budleigh Salterton.

I believe that the only paper Which treats of the order of these beds is a full report of two lectures by Mr. Pengelly, F.R.S.* To this I refer the reader for a more detailed account of the composition of the various “red rocks.”
Owing to the dip, lower and lower beds rise to the surface southwestward, so that an almost continuous section is given.
The occurrence of the uppermost part of the “New Red” near the eastern boundary of the county, and its passage upwards into the Lias, have been noticed by Sir H. De la Beche †, and more fully by Mr. Pengelly‡; but the cliffs here are so much hidden by fallen masses, that little is to be seen below the “White Lias” until we pass to the west of the great landslip of 1839 at Dowlands. The cliff is then clearer, and shows a set of evenly-bedded greenish clays, with black shales, stone-beds, and layers of hard marl (Rhætic Beds). Here Mr. Pengelly found the well-known bone-bed. Lower down some of the layers of clay have a reddish colour; and there is a passage downwards into “New Red” marl,
Note on the Auriferous Rocks of South-eastern Africa
Authors: Sutherland  
Published: October 2009

I
n
communicating the chief contents of a letter which was addressed to me by Dr. Sutherland, I beg to point out to the Society that the author seems to have arrived at some of the same conclusions as those deduced by Mr. David Forbes from his examination of the gold-bearing rocks of South America, which he described as resulting from the action of two very distinct classes of igneous rocks. (See Geol. Magazine, vol. iii. pp. 385 &c., Sept. 1866).

R
od
. I. M
urchison
.

Natal, South Africa, Sept. 8th, 1868.
A young man of the name of Parsons, who made a journey with me in March last along the southern rivers of this colony, washed some iron-sand, which gave distinct traces of gold. Since his discovery several persons have also succeeded in finding traces by the same means; but in no case has it been found in remunerative quantities; the particles never exceed the tenth or twentieth part of a grain in weight; the form is rounded and pitted, very much the same as the Australian “pepitas,” or nuggets, but visible only with a magnifying power.
Parsons has been temporarily employed by the Government to explore the rivers, with a view to settle the question whether or not the metal exists in such quantities as will pay labouring men fair wages while employed in its extraction.
I have gone carefully over chap. xix. of your fourth edition of ‘Siluria;’ and the conclusion to which I am driven is,—that the noble metal