bluuebunny/crossref_metadata_2025_split huggingface dataset:
Notes on the Geology of the Valleys of the Upper Part of the River Teign and its Feeders
Authors: Ormerod G. Wareing 
Published: October 2009

A
memoir
on “The Bovey deposit,” by J. H. Key, Esq., was read before the Geological Society of London, on November 20th, 1861†; and a memoir “On the Lignite and Clays of Bovey Tracey, Devonshire,” by W. Pengelly, Esq., was read before the Royal Society November 21st, 1861‡. The district noticed in the following pages consists of the portions of the valleys of the River Teign and its feeders, that lie north of that described in these papers.

The Teign is formed for the most part by the North and South Teigns, the Walla Brook, Easter Brook, and Bovey River.
The South Teign rises near Fernworthy, about 1400 feet above the sea level§, and joins the North Teign at Leigh Bridge.
The North Teign rises on Dartmoor, about 1600 feet above the sea-level, near the upper end of a valley that is crossed at its western extremity by the East Dart; and near the Tolmen, 1192 feet above the sea, it receives the Walla Brook, which brings the drainage of an extensive granitic district to the north. Both these streams, near and at their junction, run in artificial courses, walled at the side with blocks of granite, and cut through a rising bank, the diversion having probably been made by tin-streamers to drain the broad level that occupies a hollow of the hills at this point. From this place the North Teign runs in a narrow gorge to a level in an opening of the hills at Gidley Park, where
On a Plant-and Insect-bed on the Rocky River, New South Wales
Authors: Moore Charles 
Published: October 2009

Abstract

T
he
organic remains noticed by the author were found by him in a small block of chocolate-coloured micaceous laminated marl, obtained from a bed about ten feet thick, at a depth of 100-110 feet, in the auriferous drifts of Sydney flats, on the banks of the Rocky River. The author found the leaves of two forms of Dicotyledonous plants, fragments of a flat narrow leaf which he refers to the Coniferæ, a seed-vessel, and the impressions of several seeds. The insect-remains consist principally of the elytra of Beetles, among which Buprestidæ appear to predominate. The vegetable-remains seem to indicate that the deposit is of Tertiary age.
On the Fall of an Aerolite in Fezzan
Authors: Coumbary M. 
Published: October 2009

Abstract

T
he
object of this communication was to describe the fall of an aërolite or bolide, which took place on the 25th December, 1869, at Mourzouk, in Fezzan (lat. 26° N., long. 12° E. of Paris), in the presence of a group of Arabs. The bolide is described as a globe of fire nearly a metre in diameter, which, on falling, exploded with a sound resembling pistol-shots and a strong odour.

It is further stated that the whole or portions of the bolide will be forwarded—and that, according to information given, the poignards, sabres, and lances of the principal people of Waddai are constructed of meteoric iron, much of which has fallen in that district.
Note on the Palpus and other Appendages of Asaphus, from the Trenton Limestone, in the British Museum
Authors: Woodward Henry 
Published: October 2009

H
aving
been requested by Sir William Logan to examine the Trilobite sent over by Mr. Billings from Montreal, I was led to compare it with certain specimens in the British-Museum collection, presented by Dr. J. J. Bigsby, F.R.S., some years since.

I was at once attracted by a specimen of Asaphus, from the Black Trenton Limestone (Lower Silurian), which has been much eroded on its upper surface, leaving the hypostoma, and what appear to be the appendages belonging to the first, second, and third somites, exposed to view, united along the median line by a longitudinal ridge. The pseudo-appendages, however, have no evidence of any articulations. But what appears to me to be of the highest importance, as a piece of additional information afforded by the Museum specimen, is the discovery of what I believe to be the jointed
palpus
of one of the maxillæ (Fig. 1), which has left its impression upon the side of the hypostoma—just, in fact, in that position which it must have occupied in life, judging by other Crustaceans which are furnished with an hypostoma, as
Apus
,
Scrolls
, &e.

The palpus is 9 lines in length; the basal joint measures 3 lines, and is 2 lines broad, and somewhat triangular in form.
There appear to be about seven articulations in the palpus itself, above the basal joint, marked by swellings upon its tubular stem, which is 1 line in diameter.
There can be no reason to doubt that the Trilobita possessed antennules, antennæ, mandibles, maxillæ
On the Superficial Deposits of the South of Hampshire and the Isle of Wight
Authors: Codrington Thomas 
Published: October 2009

Summary
The chief points to which attention has been called in the foregoing paper are as follows:—

1.
That the gravel plains of the New Forest and the neighbourhood are portions of a tableland rising slightly to the northward and attaining an elevation of 420 feet: and that the remains of similar tablelands exist on the cast side of Southampton Water, and, in a more fragmentary state, in the Isle of Wight, having a slope greater and in other directions.

2.
That while the gravel covering these tablelands at the highest levels is of a far greater age than the valley-gravels of the rivers, the gravel near Bournemouth, on Beaulieu Heath, Titchfield Common, and at similar levels appears to be equivalent in position and age to the high-level valley-gravels, and also to the beach-deposits of Avisford and Waterbeach containing marine shells; and that a lower tract of gravel bordering on the northern shore of the Solent and Spithead appears to correspond on the one hand with the low-level valley-gravels of the rivers, and on the other with the marine gravel covering the low land of Selsea.

3.
That the spreading out of the gravel, and the levelling of the tablelands, probably was effected in an inlet of the sea shut in on the south side by land which connected the Isle of Wight with the mainland, and opening to the eastward.

4.
That a gradual upheaval appears to have gone on from the time of the oldest and highest gravels down to the date of the low-level valley-gravels, by which the inlet was narrowed into an estuary which received the waters of all the rivers from Poole Harbour eastward, the Isle of Wight being still connected with the mainland.

5.
That of this upheaval in its latter stages there is evidence remaining in the marine gravel of Sussex, in the raised shingle of the Foreland, and in the beach-deposits of Waterbeach and Avisford.

6.
That the flint implements of Bournemouth and Southampton Common are from gravel covering tablelands at elevations corresponding to the high-level valley-gravels, and that the implements from the coast between Southampton and Gosport are from gravel corresponding to the low-level valley-gravels.

7.
That the position of the flint implement found above the raised shingle of the Foreland appears to prove that an upheaval to the extent of 70 or 80 feet has taken place since its deposition in the brick-earth; and that if the origin of the gravel covering the plains be as above supposed, the flint implements of Bournemouth show that the upheaval has been as much as 120 feet, and the implements in the gravel on Southampton Common as much as 150 feet, since the appearance of man.
On a new Labyrinthodont Amphibian from the Magnesian Limestone of Midderidge, Durham
Authors: Hancock Albany , Howse Richard 
Published: October 2009

Among the important additions to the fauna of the Permian rocks of Durham made by Joseph Duff, Esq., last autumn, not the least interesting, perhaps, maybe reckoned the remains of a Labyrinthodont having numerous finely striated, rhombiform scutes or scales, resembling in shape those of some Ganoid fishes, though very superior in size. These remains were found at the Midderidge quarry (a portion of which has recently been removed for the purpose of widening the Darlington and Wear-valley Railway), in a bed of yellow marly limestone 7 or 8 feet above the marl-slate properly so called.
The section at this quarry is thus described by Prof. Sedgwick, Geol. Trans. ser. ii. vol. iii. p. 76:—

“1.
Bed of light-coloured siliceous sandstone, worked as a coarse flagstone and also as a building-stone. The upper beds alternate with blue-coloured calcareous shale. At East Thickley they are about 3O feet thick.

“2.
Yellow-coloured calcareous shale and shale-slate, in thickness about 9 feet. Some of these beds are incoherent and sandy ; the marl-slate forms a series of indurated bands, which divide the more incoherent shale.

3.
A series of thin beds with marly partings ; the whole about 20 feet thick. The average thickness of the several beds is not more than a few inches; their surfaces are often covered with yellow marl ; at their natural partings they are generally covered with dendritical impressions,” etc.

In the above section, No. 1 represents the uppermost member of the Coal-measures, which in this part of Durham have
Notes on the Geology of the Lofoten Islands
Authors: Bonney T. G. 
Published: October 2009

Abstract

T
he
author described the general appearance of the Lofoten Islands, which have commonly been described as composed of granite, but which, he stated, really consist of gneissic rocks. The scenery of some of the islands on which he did not land resembled that of the Cambrian and Cambro-Silurian districts of Wales and Cumberland; and the interior of Hassel showed dark rounded fells, resembling in outline some of the softer Welsh slates. At Stokmarknæs and at Melbo there is a granitoid rock of pinkish-grey colour, consisting of felspar and platy hornblende, with some mica and quartz. The Svolvaer Fjeld in Ost Vaagö shows a distinctly bedded structure in the cliffs near Svolvaer, the débris at the foot of which consists of a rock resembling syenite, and a quartzite containing a little hornblende and felspar. Bedding was also observed towards the Oxnæs Fjord. The islets near this coast consisted chiefly of a granitoid rock resembling a syenite, showing traces of bedding to the west of Svolvaer. Veins of quartz and seams of hornblende &c. occurred in some of the islets; and the latter were too regular to be explained by deposition in fissures. Near the Svolvaer post-office there was gneiss coarsely foliated, containing hornblende and mica, with pink orthoclase felspar. The author concluded, from his observations, that, with few exceptions, the so-called granites of the Lofoten Islands are stratified, highly metamorphosed rocks—quartzites and gneiss, generally with much fel-spar in the latter, and with more or less hornblende in both—and that they are inferior in position to the gneiss and schists of the mainland, and to the more slaty rocks of the southern and western parts of the same islands. He compares them with some gneiss from Dalbeg on the west coast of the island of Lewis, and thinks it highly probable that they also are of Hebridean age. The remainder of the paper described some raised beaches and moraines. The latter are frequent in the Raftsund at the mouth of tributary glens, and just above the sea-level.
Observations on Modern Glacial Action in Canada
Authors: Bleasdell W. 
Published: October 2009

Sir Charles Lyell, in his ‘Principles of Geology,’ has drawn attention to the effects of glacial action in Canada in the transportation of large stones and boulders on the shores of the river St. Lawrence to new positions by the powerful agency there exercised, more or less, every winter. As this subject possesses much geological importance, I write down a few observations of this kind that may be of interest.
There can be no doubt that in every portion of the province where large rivers, streams, and lakes abound, the effects of ice may be seen in the removal of gravel, stones, and shingle from sites where they have remained since the Boulder-drift period.
On that arm of Lake Ontario which commences at the outlet of the river Trent, at Trenton, and runs in a zig-zag direction for nearly 90 miles until it meets the main lake near Kingston, named the Bay of Quinte, the waters are frozen over every winter to a thickness of from 1½ to 2½ feet. Near the head of the bay (with which, from a residence of nearly twenty years, I am more especially conversant), and at some period during the season, a crack occurs right across from shore to shore. If this strikes a gravelly shore at either end (as it frequently does), the ice forming the crack being lifted up on each side, gravel, shingle, or stones may be seen imbedded in the ice which has thus been lifted up. These have been
On the Evidence afforded by the Detrital Beds without and within the North-eastern part of the Valley of the Weald as to the Mode and Date of the Denudation of that Valley
Authors: Wood S. V. 
Published: October 2009

T
he
denudation of the Weald valley has long been a subject of interest and of contention among geologists. The theory of a rise of a dome of strata from beneath the sea and the offthrow of the waters on all sides from that dome, their escape through lateral fractures in the upheaved chalk, together with a slow wearing back of the fractured and denuded edges of the chalk in the form of cliffs, long held its ground in our text-books, and it is only of late years that this theory has met with partial dissent.

Sir Roderick Murchison was the first, I believe, to bring prominently into notice the fact that a large part of the débris contained within the denuded area consisted of angular chalk flints brought from the exterior into the inner part of this area, and so far therefore was at variance with the received hypothesis of a flow of the denuding waters outwards from the exposed subcretaceous strata, over the surface of which these flints were scattered. His view, after an elaborate description of the detrital beds of, more especially, the western part of the great valley, was that the denudation had been accomplished by a powerful aqueous agent directed eastwards from the apex or western extremity of the Weald valley, by which these flints have been thus scattered over the Neocomian strata of that part of the valley.
Another elaborate memoir treating of the detrital beds within the Wealden escarpment, and their bearing upon the
On the probable Cause, Date, and Duration of the Glacial Epoch of Geology
Authors: Drayson  
Published: October 2009

A
fter
referring to the evidence of the occurrence of a Glacial Epoch, and to the various hypotheses which have been proposed to account for it, the author brought forward the following considerations:—

Of the three principal movements of the earth, namely its daily rotation on its axis, its revolution round the sun, and the slow conical movement of its axis of rotation round the poles of the ecliptic, the third is, in the author’s opinion, the cause of glacial epochs. The angular distance of the pole of the ecliptic and the pole of the heavens is at all times the exact measure of the obliquity of the ecliptic, or the extent of the Arctic circle upon the earth. There is evidence that during the last 2000 years these two poles have gradually decreased their angular distance, so that, while the pole of the heavens moves round some curve at the rate of about 1° in seventy-two years, it approaches the pole of the ecliptic at a variable rate, at present about 46″ in a century. The author had calculated from the recorded positions of the pole of the heavens during the last 2000 years, the curve traced by this pole with relation to the pole of the ecliptic. He found it to be a circle, the centre of which is 6° from the pole of the ecliptic, and 29° 25′ 4.7″ from that of the heavens.
Taking this curve as a guide, the author finds that 2000 years ago the
On the Principal Features of the Stratigraphical Distribution of the British Fossil Lamellibranchiata
Authors: Lobley J. Logan 
Published: October 2009

H
aving
been engaged for some years past in investigating the organic contents of British strata, and in the enumeration of the species which have been recorded as occurring in each geological formation, I am enabled to bring before this Society a summary of the stratigraphical distribution of the remains of one of the classes of the Mollusca, the Lamellibranchiata, as far as it is at present known.

The results here presented are submitted with confidence in their reliability as being approximately correct to the present time, since well authenticated species only have been retained in my lists, and extreme care has been taken to exclude those numerous synonyms which are so frequently productive of incorrect conclusions.
The class Lamellibranchiata of De Blainville, or Conchifera of Lamarck, is represented in British strata so abundantly that the genera alone number nearly two hundred. I will not here attempt to give the details of the range and distribution of these very numerous genera, but confine myself at the present time to the consideration of the principal groups of the class.
The classification of the Lamellibranchiata that will be followed is founded on that of Lamarck, and differs little from the one given in the excellent and much used Woodward's ‘Manual of the Mollusca.’

In the accompanying Tables the usual geological scale has been adopted. The term
Siluran
is intended to embrace all the rocks included by Murchison in this “System,” namely, from the Liugula Flags to the Passage Beds.
Triassic
includes the Rhætic
Geological Observations on British Guiana
Authors: Sawkins James G. 
Published: October 2009

A
detailed
geological survey of British Guiana, in the present state of the colony, would be a very difficult and prolonged undertaking, as the only lands not covered by dense forests are the coast alluvium, and the savannas or prairies of the interior; few roads extend beyond the sugar plantations on the former, and few Indian tracks over the latter; therefore it must be understood that my observations were chiefly confined to the rivers.

Along the coast the land is low, at many places (as at Georgetown) below the sea-level, composed entirely of sands, clays, and marine débris brought down by the larger rivers, which have been frequently silted up into lakes by the contra-action of the waves of the Atlantic ocean. The extent of this alluvium varies from ten to forty miles inland, where it terminates in low sand-hills of 10–70 feet elevation above the sea-level. These sand-hills extend inland until they are seen resting on granite. They are somewhat rounded by the action of the water of insignificant streams and rain.
The amount of rain, according to observations by Mr. Sandeman during ten years, shows an annual average of 102·826 in., the minimum being 68·680, and maximum 133·219; these facts will convey an idea of what the denuding influences in this colony are.
My first excursion was limited to what is called the Pomeroon district, comprising the Wainii, Barama, Barima, and Pomeroon rivers. The first granite was observed on the Wainii and Canyaballi, just below the mouth of
On the Structure of the Crag-beds of Suffolk and Norfolk, with some Observations on their Organic Remains
Authors: Prestwich Joseph 
Published: October 2009

Conclusion
Nothing can be clearer than the relation of the Red to the Coralline Crag; but the Norwich Crag occupying a different area, and each area presenting a crag-series of its own type, without superposition or passage, their relation to one another must necessarily be established on other grounds. We have to see what other beds there may be common to the two districts, whether in each they bear a like relation to those Crag beds which are the object of inquiry, and whether the differences known to exist in the latter may not be owing to geographical distribution.
In this case we have the one common bed in the Chillesford Clay, which forms a zone limiting in ascending order the position both of the Red and of the Norwich Crags, both of which it overlies and with both of which it shows a close relation. But although we can follow the Chillesford Clay (retaining its usual characters and fossils) into the southern part of the Norwich-Crag area at Southwold, north of that district it is not fossiliferous and we can only identify it by position and mineral characters. Nevertheless we can follow this argillaceous zone, although a charaoter of uncertain value, with sufficient clearness to Bacton and Weybourne, and also inland to Norwich and Coltishall. In Norfolk, however, as the sands and shingle overlying the Chillesford Clay become interstratified with beds of laminated clay very similar in appearance to the Chillesford Clay, it might be a question whether the
New Facts bearing on the Inquiry concerning Forms intermediate between Birds and Reptiles
Authors: Woodward Henry 
Published: October 2009

There is perhaps no single point along the whole line of defences raised by the opponents of the theory of Evolution which has been more warmly contested than the question of the significance attaching to the relationship of birds to reptiles. Professor Huxley truly remarks that “to superficial observation no two groups of beings can appear to be more entirely dissimilar than reptiles and birds. Placed side by side, a humming-bird and a tortoise, an ostrich and a crocodile, offer the strongest contrast, and a stork seems to have little but animality in common with the snake it swallows”.
“In perfect strictness,” writes the same authority, “no doubt, it is true that birds are no more modified reptiles than reptiles are modified birds, the reptilian and ornithic types being both, in reality, somewhat different superstructures raised upon one and the same ground-plan; but it is also true that some reptiles deviate so very much less from that ground-plan than any bird does, that they might be taken to represent that which is common to both classes without any serious error.”

“A
lizard
is not very far from being the centre of the circle, the periphery of which is occupied by
Chelonia, Ichthyosauria, Plesiosauria, Pterosauria
, and
Aves
”.
Notes on the Structure sometimes developed in Chalk
Authors: Fordham H. George 
Published: October 2009

A paper on this subject (the peculiar parallel striæ found in Chalk), read before the Society last May, brought up a discussion in which such a great variety of opinion as to the origin of this structure was shown, that I thought the following few facts might perhaps be of interest.
In a pit one mile east of Ashwell, on the borders of Hertfordshire and Cambridgeshire, a small section of the “Chalk without flints” of the Geological Survey, about 40 or 50 feet above its base, is exposed. The chalk here is hard, and may be divided into layers, which differ considerably in structure. There are at least three varieties:—(1) layers of hard chalk, divided into slabs about an inch thick; (2) beds much thicker and more massive than the last; and (3) a bed of a concretionary nature. These beds are from six inches to several feet in thickness.
The concretions are marked nearly all over by the lines of this structure. I find that the lines are only found on the concretions (which are easily removed from the parent rock) and in their very immediate neighbourhood. The other beds are entirely free from any trace of the structure.