bluuebunny/crossref_metadata_2025_split huggingface dataset:
On the Packing of the Ice in the River St. Lawrence; the occurrence of Landslips in the Modern Deposits of its Valley; and the existence of Marine Shells in them and on the Mountain of Montreal.
Authors: Logan W. E. 
Published: October 2009

The island of Montreal stands at the confluence of the rivers Ottawa and St. Lawrence, and is the largest of several islands splitting up these mighty streams, which cannot be said to be thoroughly mingled until they have descended some miles below the whole cluster. The rivers first come in contact in a considerable sheet of water called Lake St. Louis, which separates the upper part of the island of Montreal from the southern main. But though the streams here touch, they do not mingle. The waters of the St. Lawrence, which are beautifully clear and transparent, keep along the southern shore, while those of the Ottawa, of a darker aspect, though by no means turbid, wash the banks of the island; and the contrast of colour they present strongly marks their line of contact for many miles.
Lake St. Louis is at the widest part about six miles broad, with a length of twelve miles. It gradually narrows towards the lower end, and the river as it issues from it becoming compressed into the space of half a mile, rushes with great violence down the Rapids of Lachine, and, although the stream is known to be upwards of eight feet deep, it is thrown into huge surges of nearly as many feet high as it passes over its rocky bottom, which at this spot is composed of layers of trap extending into floors that lie in successive steps.
At the termination of this cascade the river expands to a
On the Geology of the Calf of Man
Authors: Cumming J. G. 
Published: October 2009

The Calf of Man is an islet of about 800 acres in superficial extent, situated at the south-western extremity of the Isle of Man, and separated from it by a narrow channel, in breadth not more than 500 yards, called “the Race” or “Sound” of the Calf. Nearly in the centre of this channel, but rather towards its northern side, lies the small rocky islet of Kitterland, between which and the Isle of Man the channel is fordable at low water, and between it and the Calf islet the passage is rendered dangerous by several sunken rocks, the tide rushing through the channel at certain periods of ebb and flow at the rate of nine miles per hour.
Geologically, the islet of the Calf must be considered simply as a prolongation of the Mull hills, separated from them by a chasm at right angles to the general axis of elevation, and which corresponds, in fact, with the larger chasms, which, when the sea was at a higher relative level, formed channels at Port Erin, Fleshwick and Peel. It rises gradually from the south-western extremity, the northern and south-eastern side presenting to the sea precipices to the height of 470 feet, the highest point being at the pile near the ruins of Bushel's house. Off the western point is the dangerous reef of the Hen and Chickens, the two revolving lights on the Calf, when brought in line, bearing upon them.
The Stack is a singular pile of rocks near the
On the Neighbourhood of Bombay, and certain beds containing Fossil Frogs
Authors: Clark G. T. 
Published: October 2009

The island of Bombay is composed of five or six bands of trap rock, chiefly greenstone and amygdaloid, conformable, and dipping west at about 10° or 15°, and separated by beds that have every appearance of being of sedimentary origin, though there is no actual proof of the fact. The highest and most western of these beds have been laid open in some engineering operations, and in these the fossils sent to the Society have been found.
The batrachian beds are a mass of blue rock, weathering into a shale not unlike ordinary coal shale, and containing what I have no doubt will turn out to be vegetable impressions. The upper beds are interstratified with thin seams of sandstone and argillaceous rock, and over the whole is a mantle of basalt which cannot have been less than 70 feet thick. This basalt has in parts caused imperfect fusion of the fossil beds, obliterating their stratification and superimposing something of its own columnar, or at least prismatic structure.
These fossil were discovered, a few days ago, by Dr. Leith of the Bombay Service, and as he is an acute and diligent observer and well-acquainted with his subject, I think, before very long, these beds will be thoroughly investigated.
I am preparing an account of the geology of the island, but it is so closely connected with that of the main land, that I am loath to say much upon the one until I am better acquainted with the details of the
Extract from Mr. Conybeare's Report on the Country between the Summit of the Malsej Ghaut and the Gungathuree, dated Bombay, Oct. 1846
Authors: Hamilton W. J. 
Published: October 2009

Numerous spurs everywhere extend from the Sahadry range to the eastward, and the distance to which they extend is proportionate to the importance of the streams which run between them. The ranges which separate the smaller class of tributaries soon cease; those which intervene between the rivers which result from the junction of such tributaries have a greater extent, and the ranges which form the watersheds dividing the great river systems, sometimes extend 200 or 300 miles into the interior.
To the latter class belongs the range forming the northern boundary of the valley at the head of the Malsej Ghaut; that valley is the most northern of the river system of the Kristna, and the waters of the Kristnawuttee, which rise in it near the crest of the Ghaut, reach the main trunk by flowing successively along the Kokree, the Goor and the Beema; the precipitous range which bounds and hedges in this valley on the north is the southernmost member of a hilly tract thirty miles in depth, which separates the Kristnawuttee from the level plains of the Gunga or Godavery, and in which rise the most southern affluents of the latter river.
No eligible opportunity occurs for traversing this range and thereby entering the Bramanwarree hills, until the Alleh Khind is reached about twenty-two miles E. of the Malsej. A few miles beyond this point the southernmost range becomes almost impracticable, expanding into broken table-land, and barring all further progress to the east, by pushing out towards
On recent Depression in the Land
Authors: Smith James 
Published: October 2009

The human period may be subdivided into the present, or that in which geological events are subjected to our own observation; the historieal, or that in which they have been observed and recorded; stud the antiquarian, in which, although we cannot assign a date to them, we can prove from human remains or works of art that they must have taken place since the earth was inhabited by man.
Having recently observed proofs of movements of depression in each of these periods, I proceed to notice them in their retrograde order.
When I visited Pozzuoli in 1819, the floor of the temple of Serapis was dry, but I remarked that the channels cut across it for the purpose of draining the waters of the thermal spring which rises within i t s predncts were nearly filled with sea-water, with a sensible current flowing inwards, or from the sea ; when I returned in 1845, I found that the high-water mark stood at 28 inches above the pavement, exhibiting a rise of about an inch yearly.
As there is a rise and fall of tide of nearly 10 inches within the building, and as I have no means of knowing the state of the tide at my first visit, I cannot speak with certainty as to the exact change of level which had taken place during the interval between my observations ; I am however satisfied that it could not be much more or less than one inch yearly.
Professor Forbes
Notes on the Palæozoic Formations of New South Wales and Van Diemen's Land
Authors: Jukes J. Beete 
Published: October 2009

The county of Cumberland, in which the city of Sydney is situated, and parts of the adjacent counties, are composed almost entirely of a palæozoic formation of great thickness and extent. The principal materials of this formation are certain shales and sandstones, with a few associated beds of coal. In the close of the year 1845 I made a short excursion across a portion of this district, in company with the Rev. W. B. Clarke. We carried with us a mountain barometer, and by taking the means of the two sets of observations made in going and returning, got such an approximate estimate of the heights of the ground and the thickness of the rocks, as to enable us to construct a section with a sufficient approach to accuracy to be relied on for my present purpose. This section runs from Liverpool (a town just at the head of the tidal waters of George's River, which falls into Botany Bay) by a slightly winding line, first S.S.W. for about twenty miles, through Campbelltown to Appin, and then about S.S.E. for about eighteen miles to Wollongong in the Illawarra district. Wollongong is on the coast about forty-five miles to the northward of Sydney.
From Paramatta by Liverpool to Campbelltown the country is low, gently undulating, and composed (P1. VII.) almost entirely of (No. 1) black and brown shales, with a few thin interstratified beds of sandstone in their lower portion. From Campbelltown to Appin the country rises into bolder undulations, and
Introduction to a Second Memoir of Capt. Vicary on the Geology of parts of Sinde
Authors: Murchison R. I. 
Published: October 2009

Geologists are indebted to the enterprising and lamented Burnes for the first general sketch of the structure of the region watered by the Indus. In subsequent years we were furnished with more detailed information by Capt. Grant, who, collecting fossils in the Run of Cutch, gave us the means of ascertaining that in addition to the nummulitic and conglomerate rocks partially described by Burnes, other portions of that tract were of Jurassic or Oolitic age (Oxford clay, &c.).
When the brilliant victories gained by Sir Charles Napier added Sinde to the British possessions, that officer resolved to ascertain more precisely the geological structure and real mineral condition of the new province. Having driven back the Belooches into their mountains, he directed Capt. Vicary, whom he selected for the purpose, to prepare a report on the geological relations of these tracts, which, with the exception of the partial and rapid journeys of Pottinger, Grant and Christie, were unknown to Europeans. The report of Capt. Vicary on the previously unexplored Muree country, from Shakpoor to the Degra valley*, was accompanied by a case of fossils collected under circumstances of unusual difficulty.
Having had the honour of being entrusted by the Earl of Ellen-borough and Sir Charles Napier with that report of Capt. Vicary and with his fossils, I laid them before this Society, and an account of them is printed in the second volume of our Quarterly Journal, p. 260.
I have recently been favoured with another letter from Sir Charles Napier
On the Elevation and Denudation of the District of the Lakes of Cumberland and Westmoreland
Authors: Hopkins W. 
Published: October 2009

The general structure of the district of the lakes of Cumberland and Westmoreland is well known to geologists, more particularly by the labours of Professor Sedgwick. My own task, in the general examination which I have recently made of the district, has been one of inspection and not of discovery ; and the object of the present communication is not the description of phmnomena, but the theoretical discussion of the causes to which they are to be referred. I shall enter into descriptive details only so far as may be necessary for this purpose. In the first part of the memoir I shall consider the structure and elevation of the district, and in the second part the ph~enomena of its denudation.
1. Boundary of the District.--In descriptive geology we may apply the term district to a portion of country comprised within any arbitrary boundary to which our researches may have extended; but in considering the theory of its elevation, a district must include the whole of that space throughout which we recognize a character of continuity in the external configuration and the observed phmnomena. Thus in the case before us, we must not limit ourselves to the group of mountains immediately associated with the lakes, but must extend the district eastward to the great Penine fault, which will thus form its eastern boundary. On the north, from Kirkby Stephen by Hesket round to Egremont and thence to Morcambe Bay, its boundary will be sufficiently marked by that of the New Red
Notes on the Geology of the Coasts of Australia
Authors: Jukes J. Beete 
Published: October 2009

In this memoir Mr. Jukes gave a short abstract of all the information collected by various travellers regarding the Australian continent, including his own observations.
The eastern coast is occupied by a great range of high land, appearing like a continuous chain of mountains when seen from the sea, and rising in several places to 5000 feet or more above the sea-level. This chain has an axis of granite, with occasional large masses of greenstone, basalt and other igneous rocks. It is flanked on both sides by thick beds of palæozoic formations, chiefly sandstone, but also containing limestone and coal. In the northern portion of the chain Dr. Leichardt found similar formations, and especially trap and granite near the Burdekin river. In the Port Philip district there are similar igneous rocks, and on the coast tertiary formations, which Mr. Jukes found resting on the edges of upturned palæozoic beds. In West Australia the Darling range consists of granite below, covered by metamorphic rocks; and between it and the sea is a plain composed of tertiary beds. In the colony of North Australia there is a great sandstone plateau, rising about 1800 feet above the sea, and probably of palæozoic age; whilst on the immediate shore and round the Gulf of Carpentaria are beds supposed to belong to the tertiary period. Similar formations constitute the substratum of the central desert, in which Capt. Sturt was compelled to turn, when half-way to the Gulf of Carpentaria, from the southern coast.
On the presence of Phosphoric Acid in the subordinate members of the Chalk Formation
Authors: Nesbit J. C. 
Published: October 2009

It is well known, that upon certain strata of the upper and lower greensand, the use of bones and other substances containing phosphoric acid has not proved of the slightest benefit for agricultural purposes. I have for some time been engaged in collecting soils and rocks from these formations, for the purpose of chemical investigation into the origin of their fertility. Among others, I obtained from Farnham specimens of a fertile marl which is found on the estate of J. M. Paine, Esq. A cursory examination gave evidence of the existence of an unusual amount of phosphoric acid in the marl, and in November 1847 I communicated to Mr. Paine the discovery I had made.
From the marl was subsequently obtained by washing, substances, evidently coprolitic, containing twenty-eight per cent. of phosphoric acid; the general mass of the marl contained from two to three per cent. of phosphoric acid.
Outline of the principal Geological Features of the Salt-Field of Cheshire and the adjoining districts
Authors: Ormerod G. Wareing 
Published: October 2009

In the following pages it is proposed to give only a general geological description of the district connected with the Cheshire salt-field. In so doing, such dislocations only as affect the general geological features will be noticed, and it is purposed to avoid as much as possible touching upon any theoretical points, confining this paper to mere description.
The word “fault” will be used as meaning a dislocation causing a general change in the direction of dip : the word “throw” when the direction is not altered.
Sketch of the Structure of the country extending from Cader Idris to Moel Siabod, North Wales
Authors: Jukes J. Beete , Sewlyn Alfred R. 
Published: October 2009

The rocks are arranged into the following groups, of which the names are only provisional, and the thicknesses assigned from rough estimation. In the ascending order:—

A.
The Barmouth and Harlech sandstones, 3000 feet. A mass of quartzose sandstone and conglomerate, with some beds of blue and purple slates, and occasionally trap rocks. No organic remains discovered in this group.

B.

The Trappæan group, 15,000 feet: subdivided into—

B 1.
Blue and grey schistose slates and flagstones, interstratified with many beds of a grey calcareo-feldspathic “ash” often crystalline, together with feldspathic trap and greenstone; the slaty rocks predominating.

B 2.
Great masses of feldspar-porphyry and some greenstone, with feldspathic trappsean “ash” arranged in beds a few inches or many feet in thickness. Interstratified with these, and passing into them (especially into the ash) by almost imperceptible gradations, are many beds of black slate, forming often irregular and apparently lenticular-shaped masses. In some parts of B 1, Lingulæ are found in great abundance, and a few other fossils. In B 2 Lingulæ and Graptolites also occur, but not very abundantly.

C.

The Bala group, 9000 feet: subdivided into—

C 1.
Black slates of variable thickness, very fine-grained, brittle, and frequently having their true lamination or stratification entirely obscured by cleavage and numerous joints.

C 2.

Grey, fine-grained, arenaceous
slate-rock
, often passing into a hard, compact, splintery gritstone; in its lower portion are one or two beds of trappæan ash, sometimes crystalline, sometimes flaky and sometimes brecciated, often highly calcareous. About its centre is one thin bed of impure limestone (Bala limestone), and sometimes, but very rarely, another little band in its upper portion (Hirnant limestone). Organic remains are very rare in C 1; but in C 2, as is well known, are very abundant and in great variety.
Observations on the Silurian Strata of the South-East of Scotland
Authors: Nicol James 
Published: October 2009

D
uring
a visit to the south of Scotland last autumn I collected some fossils from the older rocks of that district, which appear interesting as adding another link to the chain of evidence by which the true age of these deposits may he ascertained. Taken in connection with the fossils formerly noticed* and with those procured by Mr. Moore in Wigtonshire†, they may be regarded as rendering the Lower Silurian age of one part of these beds almost certain, so that the connection of the rocks and mountain-chains of this portion of Britain with those of other countries may now be so far traced out.

The fossils which Mr. Salter last year kindly determined were chiefly procured from the only bed of limestone known in the Silurian rocks of the south-east of Scotland. My hopes of obtaining better or more characteristic specimens from that locality were disappointed, and not even a single new form was discovered after a careful search. Indeed, the highly crystalline texture of the limestone, probably occasioned by a mass of trap with which it is always associated, renders it very improbable that this bed will ever add much to our knowledge of the beings existing in the seas in which it was deposited.
My researches in the slate rocks were more successful, especially in the Grieston quarry near Traquair. In this place the rocks consist of clay-slate, sometimes passing into a fine greywacke, and are wrought for a coarse kind of roofing-slate. The strata are thin
On the Occurrence of Productive Iron Ore in the Eocene Formations of Hampshire
Authors: Tylor Alfred 
Published: October 2009

T
he
presence of large ferruginous Septaria, containing carbonized wood, principally in small fragments, was noticed in the lower part of the Barton clays, between Barton Cliff and Muddiford, by Mr. Prestwich and myself about two years ago. At that time we did not proceed west of Christchurch, and I was unable to accompany Mr. Prestwich in his more recent visit to the cliffs between Christchurch and Poole, when Mr. Prestwich also noticed the very ferruginous condition of these large tabular Septaria†.

Having lately had an opportunity of paying a visit to Hengistbury Head, I was much interested in finding that these blocks have been found to contain so large a per-centage of iron as to be available for economic purposes. As productive iron ores have not previously been known to occur in the English tertiaries, I have thought the fact of sufficient interest to be laid before the Geological Society.
Mr. Holloway, of Christchurch, who has undertaken these works, informs me that the occurrence of large masses containing iron in these cliffs appears to have been discovered in the reign of Charles II., during a survey of the adjoining harbour of Christchurch. The king was recommended to establish iron-works here for the purpose of founding cannon; the ore was to be obtained from the shore, and the charcoal from the neighbouring New Forest; this scheme, however, was not carried out. Within the last three years Mr. Holloway sent specimens to South Wales for examination. The first impression of the ironmasters
On certain Beds in the Inferior Oolite, near Cheltenham
Authors: Brodie P. B. 
Published: October 2009

T
he
inferior oolite in the immediate neighbourhood of Cheltenham, has been already well described in the “Geology of Cheltenham,” by Sir R. Murchison, Mr. Buckman, and Mr. H. E. Strickland; but as there is a very interesting bed called “the roestone” by local geologists, which, however, for obvious reasons it will be better to name “
shelly freestone
,” containing several new and peculiar fossils, many of which have not been previously noticed, it may be desirable to lay a brief account of it before the Society.

The outer escarpments of the Cotswold Hills are composed of the inferior oolite and lias, and form an important feature in the geology of the county, presenting bold headlands along the vales of Gloucester and Berkeley, in some instances rising to the height of more than 1000 feet above the level of the sea, and extending in a tortuous line for several miles from north-east to south-west. They constitute the eastern boundary of the Severn; the towns of Cheltenham and Gloucester lying in bays at the foot of this range of hills, the base of which consists of lias, surmounted by a variable thickness of oolite.
The following divisions (see Section, p. 242) of the oolitic strata at Leckhampton Hill, near Cheltenham, where the shelly freestone may be most advantageously studied, have been principally proposed and adopted by the authors of the work above referred to; although later investigations by Mr. Strickland prove, that their relative thickness is greater than has been generally supposed, and