bluuebunny/crossref_metadata_2025_split huggingface dataset:
Upper Devonian Goniatites from Mount Pierre, Kimberley District, Western Australia
Authors: Delépine Gaston 
Published: October 2009

I. Introduction
In 1890, A. H. Foord described Palæozoic fossils from the Kimberley District, Western Australia. Amongst them were Devonian brachiopods and fragments of indeterminable goniatites.

In 1924, A. Wade collected many goniatites at Mount Pierre. He figured seven specimens in his report (1924, pl. iii). The description of this plate, by Chapman (1925?), records: “Various Cephalopod shells, including ammonitoid forms as
Aganides
and (?)
Gonioclymenia
, and a cyrtoceracone (Nautiloid shell). Devonian or Carboniferous.’ A number of the goniatites collected by Wade are preserved in the British Museum (Natural History), where they are registered under the numbers C.35270 to C.35365; they do not, however, include the figured examples.

Recently, Professor E. de C. Clarke sent some goniatites to me from the same district, with the following note:—

‘The specimens occur in a red limestone at Mount Pierre, on the Margaret River. At the same locality a white limestone occurs which is considered Devonian and contains
Atrypa aspera, desquamata, Wilsonia cuboides
and
Pugnax pugnus
. At present nothing is known of the relationship of the red limestone to the white
Atrypa
-limestone.’

I am indebted to Dr. W. D. Lang and Dr. L. F. Spath for enabling me to study specimens in their charge at the British Museum (Natural History).
Sixteen specimens of this species have been collected by Professor Clarke at Mount Pierre. The Wade collection contains many more specimens, 84 of them being in the British Museum (Natural History). Many of these goniatites, as, for example, the four specimens figured here,
The Westleton Series of East Anglia: its Age, Distribution, and Relations
Authors: Solomon John David 
Published: October 2009

I. Introduction
On the Geological Survey maps of the country to the south-east of the Chalk escarpment, numerous areas, extending almost continuously from Norfolk to Berkshire, are shown coloured in various shades of pink and described somewhat non-committally as “Glacial Sand”. It is clear that several deposits of various origins have been included under this heading, but as yet no intensive attempt has been made to distinguish between them over more than a very limited area. The task is, indeed, in the absence of fossils, a matter of great difficulty. Some workers have drawn criteria from the pebble content of the gravels, but these criteria have sometimes led them astray, and in any case are not applicable to the sandy deposits.
My own method has been to make use of the heavy mineral assemblages, which are obviously of great value in investigating the “directional” deposits formed from ice-borne material, and which are applicable equally to sands and gravels. The results obtained are in partial agreement with those of many previous workers, notably Prestwich, S. V. Wood, H. B. Woodward, A. E. Salter, and R. L. Sherlock. The fresh evidence obtained during the present investigation helps also to resolve many of the mutual contradictions inherent in their conclusions.
II. Historical Summary
It would be useless and tedious to attempt a summary of all the older work on the subject; I have therefore limited myself to the important publications, and especially to those which express the latest views of their authors.
Searles
On a New Section of Fossiliferous Upper Cornbrash of North-Eastern Facies at Enslow Bridge, near Oxford
Authors: Douglas James Archibald , Arkell William Joscelyn 
Published: October 2009

In a recent account of the stratigraphical distribution of the English Cornbrash we pointed out that positive evidence of the existence of Upper Cornbrash was lacking over an extensive area of outcrop north and east of Oxford. All that we were then able to say (1932, p. 123) was: “Over this area the Lower Cornbrash alone forms a surface feature or appears in any of the exposures. The thin representative of the Upper Cornbrash, seen in the Long Handborough and Kidlington quarries and during the construction of the Woodstock railway, if it is present to the north-east of Oxford, has nowhere been encountered nearer than Bedford, 50 miles distant.” We had previously stated, however, in an analysis of the fauna of the South-Western area, including the Oxford district: “The record is still far from complete; new exposures in the area will furnish additional facts.”
Such an exposure has now come into existence, and the Upper Cornbrash thereby revealed, although but a thin formation, has proved so richly fossiliferous, and the light thrown on questions previously doubtful is so illuminating, that we consider a description of the section should be made known without delay.
The quarries at Greenhill, near Enslow Bridge on the River Cherwell, about nine miles north of Oxford, have been famous since the days of Buckland as a hunting ground for Cornbrash fossils; but although they have been visited by many generations of collectors, no fossils indicative of the Upper Cornbrash have hitherto been recorded. When describing the
The Composite Gneiss and Contaminated Granodiorite of Glen Shee, Perthshire
Authors: Williamson William Owen 
Published: October 2009

The area discussed is depicted on Sheet 56 of the 1-inch map of the Geological Survey of Scotland. This sheet was geologically surveyed by James Geikie, H. M. Skae, and G. Barrow, and is not accompanied by a Memoir.
The district shown in Fig. 1 has received the scantiest notice in geological literature. Fundamentally, its rocks are metamorphosed sediments of the Dalradian Series, invaded by intrusions of various characters and ages. Their apparent sequence, as set forth on Sheet 56 and by Bailey (1925, p. 673, and map opposite p. 698), is as follows:—
This table may show the true or the inverted succession (Bailey, 1925, p. 672, footnote). Bailey's terminology is here adopted.
“Basic Older Igneous Rocks” are intercalated with both Ben Lui and Ben Lawers sediments of Glen Shee. Further, the region includes a mass of “Older Granite” which, by invasion of the Ben Lui Schist, produced a complex termed the “Duchray Hill Gneiss”. Sheet 56 shows the gneiss as a band, which is continued on the adjoining Sheets Nos. 55 and 65 (cf. Read, 1928, map on p. 768). In the Memoirs on Sheets 55 and 65 the gneiss is briefly described and reference made to the type area of Duchray Hill (Barrow, 1905, pp. 101–2; 1912, pp. 69–70). Bailey (1925, p. 676) has verified the igneous nature of much of the material exposed on this hill.
Read (1927, pp. 337–8) has compared the composite oligoclase-biotite-gneisses of Cromar, in their respect to their origin, with the Duchray
The Basic Intrusive Rocks Associated with the Cambrian Inlier Near Malvern
Authors: Blyth Francis George Henry 
Published: October 2009

I. Introduction

T
he
rocks to be described occur as minor intrusions in the Cambrian strata which are exposed in a small elongated inlier situated on the western flank of the Malvern Hills, east of Eastnor village, Herefordshire (Ordnance Survey 6-inch sheet, Hereford XLII NW.). Their general petrographic features have been described by T. T. Groom (1899, pl. xiii; 1901, p. 158), whose work is now supplemented by the results of a chemical and petrological re-examination of the rocks. Groom (loc. cit.) showed that the intrusives invade the Cambrian strata but not the Silurian. He recognized three main types: (1) an amphibole-bearing andesitic type (probably camptonitic), forming dykes, sills, and bosses; (2) porphyritic olivine-basalts, forming sills and small laccolites, and (3) olivine-diabases, forming sills with porphyritic margins. These were found at five localities only in the grey Bronsil Shales.

Further descriptive reference to these rocks is confined to one instance, by Groom himself (1910, p. 704).
II. Petrography
With some modification of nomenclature the abovementioned three-fold grouping is retained in the following description of the main rock-types.
The Splitic Andesities (Group A)
These are very fine-grained purplish grey rocks, porphyritic and sometimes trachytic in texture, corresponding in general with Groom's “amphibole-bearing andesitic type”. They are free from vesicles, and occur as (1) dykes in the Hollybush Sandstone north-north-west of Ragged Stone Hill, and (2) bosses or sills in the black shales south-east of Fowlet Farm, and the grey shales south-east of Martins (Fig. 1).
In thin section they show a microcrystalline
Brachiopoda from the Lower Lias, Green Ammonite Beds, of Dorset
Authors: Muir-Wood Helen M. 
Published: October 2009

I. Introduction.
Brachiopods are rare in the Green Ammonite Beds of Dorset and are represented by only three species, two of which belong to the Discinidæ and one to the Rhynchonellidæ. The specimens, with one exception, are of small size and are usually much crushed and distorted.

The most abundant species is
Scalpellirhynchia scalpellum
(Quenstedt), which is found mainly in beds 129 and 130, just below the Middle Lias, while a few scattered specimens occur below in beds 122–126 and 127. This species occurs in the lower part of the Lias δ of Württemberg, but has not been previously recorded from this country, owing probably to the lack of careful collecting in other areas of Liassic deposits.

An investigation of the internal structure of
S. scalpellum
was made by grinding transverse and longitudinal sections of specimens that had been previously heated to redness and embedded in plaster cubes when cool. A full description of this method is given elsewhere (Muir-Wood, 1934).

One pedicle valve of a
Discinisca
of exceptionally large size was obtained from bed 130. One small specimen of
Discinisca holdeni
was obtained from the Upper Limestone, bed 129a, and a second specimen from the Red Band, bed 126a of Stonebarrow Cliff.

All the material was collected by Dr. W. D. Lang and is preserved in the British Museum of Natural History collection.
The specimen [B52300] consists of the conical valve only, of which all but the innermost layer of the shell is missing. The shape is approximately circular
A Further Contribution on the Karroo Rocks of Tanganyika Territory
Authors: Stockley Gordon Murray 
Published: October 2009

The occurrence of Karroo rocks in Tanganyika has been known virtually from the time of Livingstone, who is reported to have discovered coal in the Upper Rovuma. The best known occurrence is that south of Manda, near Lake Nyasa, which is described by Bornhardt. To people within the Territory, however, the Ufipa coalfield in the Kigoma Province is the most familiar. The following list of outcrops of definitely known Karroo rocks is given in order of economic importance.

1.
Ruhuhu coalfields, Njombe and Songea Districts.

2.
Kivira-Songwe coalfields, Tukuyu District.

3.
Ufipa coalfield, Ufipa District.

4.
Kidodi area, South Kilosa District.

5.
Rufiji-Ngerengere area, Morogoro and Rufiji Districts.

6.
Tanga.

7.
Mitomoni on the Portuguese border, on the Rovuma, south of Songea.

Other areas where rocks occur which are now considered to be of Karroo age, though the evidence of fossils is wanting, are

8.
Uha area, in Kigoma District.

9.
Kingongolero Hill, south of Manyoni.

10.
The Rufiji-Luwegu area in the Mahenge and Liwale Districts.

The last-named is an area which may possibly be extended, and may finally link up with the Ruhuhu coalfields in the Songea District in the south; in the north, it passes into the Rufiji-Ngerengere and Tanga districts, and is partly overlain by marine Jurassic rocks north of the Central Railway. It is thus a region which may extend for nearly 500 miles, from Lake Nyasa to Moa, north of Tanga, and in which Karroo rocks are actually exposed for 350 miles. The Karroo formation
Karroo Lamellibranchia from Tanganyika Territory and Madagascar
Authors: Cox Leslie Reginald 
Published: October 2009

This paper deals primarily with a large collection of lamellibranchia obtained by Mr. G. M. Stockley in 1931 from the Karroo beds of the Kidodi district of Tanganyika Territory. These fossils are of considerable interest as affording the first evidence of an Upper Permian marine incursion into an African Karroo basin of deposition, and also include numerous non-marine species new to the Karroo fauna.
It would have been impossible to determine the age of the marine fossils with any degree of certainty had it not been for the fortunate coincidence that, while studying them, I was shown a collection, including two of the same species, obtained from a known horizon in Madagascar by Mlle E. Basse. I must express my very warm thanks to her for relinquishing her original intention of describing her material herself and kindly permitting me to figure some of her specimens in the present paper.

The following details of the succession in the Kidodi district indicate the horizons of the fossils collected by Mr. Stockley:— Ruhembe Beds (3700 foot).— Sanstones and carbonaceous shales, including two molluscan horizons, the upper marine and the lower freshwater, separated by 1200 feet of massive sandstone. The lower horizon is 250 feet from the base of this series. Calcareous Beds (700–800 feet).—Carbonaceous shales, silicified limestones and calcareous sandstones, including an horizon with non-marine mollusca (mainly
Kidodia
, gen. nov.) about 415 feet from the top. Ndeke Beds (2900 feet).—Sandstones and conglomerates with intercalated mudstones, etc. Unfossiliferous. The rocks belonging to the upper
Gravity Collapse Structures and Mountain Ranges, as exemplified in South-Western Iran
Authors: Harrison John Vernon , Falcon Norman Leslie 
Published: October 2009

The object of the present paper is to recapitulate our previous work on gravity-formed anomalous structures, to describe further examples, and to propound arguments based upon structures in the Swiss Alps and upon theoretical considerations.
In south-western Iran, post-Miocene orogenesis produced a series of approximately symmetrical folds, in section nearly sine curves, trending north-west and south-east. Vigorous erosion followed, revealing the following column of strata:—
The limestones now often protrude as strike ridges and dome-like ranges with the marl groups weathered away between and around them. Dissection, measured from the mountain summits to the strike stream beds, reaches as much as 8000 feet; earlier in the cycle it probably reached 12,000 feet.

When erosion left a knife edge upstanding or a dome unsheathed, the beds at first remained unaffected, but when the pile exceeded about 2000 feet in height they tended to bend and break, and to produce such secondary structures as
roof-and-wall, cascade, flap
, or
slip-sheet
. In every case, an unmoved control bed can be seen within the original fold; the form which these secondary structures took depended upon the attitude of the rock under the progressive denudation of its cover and support.

A
roof-and-wall
structure is produced from a sine-curve fold when the crest is notched by erosion, and the two sheets so produced slip down and outwards, bending at first into a knee-fold. This knee then breaks; the lower limb remains nearly vertical whilst the upper rests upon it with a sudden change in dip, and separated
The Differentiated Dyke of Newmains, Dumfriesshire, and its Contact and Contamination Phenomena
Authors: Kennedy William Quarrier , Read Herbert Harold 
Published: October 2009

I. Introduction
Within the Southern Uplands of Scotland, the highly folded Ordovician and Silurian sediments are intruded by a suite of calc-alkaline igneous rocks of Lower Old Red Sandstone age which includes a well-developed dyke swarm. The dykes trend in a north-east and south-west direction and, although individually thin, collectively they represent a considerable body of magma.
The only literature dealing with the subject, however, is Teall's generalized account in the Southern Upland Memoir (1899, pp. 625–31), a paper by Read (1926) on the micalamprophyres of Wigtownshire, and a short section in the description by Gardiner and Reynolds of the Loch Doon granite (1932, pp. 19–26).
The Newmains dyke, which forms the subject of the present paper, is a member of the Southern Upland swarm and crops out on the hillside immediately north and north-east of Newmains farm, some 4½ miles west of Dumfries and within Sheet 9 of the 1-inch Geological Survey Map (Fig. 1). The dyke is about 15 feet wide and runs for a little more than a mile in a general north-east and south-west direction, in conformity with the strike of the Silurian (Llandovery-Tarannon) greywackes into which it is intruded. It is a typically heterogeneous, differentiated intrusion and consists of three main rock types associated in an intimate manner. The main rock is a granophyric spessartite or markfieldite, which passes on the one hand into a basic, hornblende-rich type and on the other into a leucocratic variety poor in ferromagnesian constituents. These three rock types are
The Ammonite Zones of the Upper Oxfordian of Oxford, and the Horizons of the Sowerbys' and Buckman's Types
Authors: Arkell William Joscelyn 
Published: October 2009

It is more than a century since J. and J. de C. Sowerby figured in
The Mineral Conchology
, from the Corallian of the neighbourhood of Oxford, the type specimens of
Ammonites plicatilis, Am. cordatus, Am. excavatus, Am. vertebralis
and
Am. catena
, and since Brongniart made the district the type and standard of the Oxfordian stage, a term adopted by Marcou and, after emendation by d'Orbigny, eventually disseminated in the stratigraphical literature of the whole world.

Nevertheless, in spite of the time that has elapsed and of the labours of S. S. Buckman in the district, the precise stratigraphical horizons and ranges of the Sowerbyan types remain obscure, as does also the whole succession of ammonite faunas. This obscurity is reflected in the variety of interpretations that have been put upon the term “Oxfordian stage” (see Arkell, 1927, pp. 154–5). I accept here the scope of the stage as stabilized by d'Orbigny (1852, p. 522: “l'Oxford Clay, le Calcareous Grit, le Coralline Oolite de M. Phillips” [the last the Oxford Oolite of Buckland and Fitton]) in which form (including, of course, the coral rags) it has also been accepted by Dr. Spath in his latest comprehensive table of Jurassic stages (1933, p. 872). The Upper Oxfordian as there represented, and as now commonly understood, corresponds with the Corallian beds in England and the Argovian and Rauracian substages on the Continent.
In this paper I attempt to show the content of the Upper Oxfordian, with special referrence to ammonite horizons, in the
The Age of the Sarn Granite
Authors: Matley Charles Alfred , Smith Bernard 
Published: October 2009

The age of the granitic and gneissose rocks near Sarn, Rhôs Hirwaen, and Meillionydd in south-western Lleyn has long been a subject of difference of geological opinion. The granite and its gneissic associates were originally mapped together by the Geological Survey as “syenite”, and were generally known as the “Rhôs Hirwaen syenite”; this was considered by Ramsay to be of Palæozoic age. Later, Hicks visited Lleyn, and among the numerous rocks in that district which, in 1878, he claimed to be of Pre-Cambrian age was the Rhôs Hirwaen “syenite”, which he called a metamorphic Dimetian granitoidite. Tawney soon afterwards examined the geological relationships of the rocks mentioned by Hicks and came to the conclusion that “of all the areas of rock in the Lleyn promontory which Dr. Hicks claims as Pre-Cambrian, this patch of metamorphic rocks near Sarn [that is, the Rhôs Hirwaen “syenite”] seems to be the only one with any claim. It is, however, unfortunate that we have not been able to find any fragments of it inclosed in Cambrian beds” (1883, p. 68).
Tawney's opinion was based on the examination of the junction of the granite and Ordovician sediments in a quarry near a fine cromlech at the north-eastern margin of the granite mass, which he calls “the quarry by Amwlch Lodge”. As the cottage is now shown on the six-inch map as “Mountain Cottage” the exposure will be referred to in future as “Mountain Cottage Quarry” (Fig. 1). Tawney's account shows that he had considerable difficulty
Observations on the Distribution of Land and Freshwater Mollusca in the Southern Libyan Desert
Authors: Sandford Kenneth Stuart 
Published: October 2009

In the course of a reconnaissance of the southern Libyan Desert and north-western frontiers of the Anglo-Egyptian Sudan, led by Major R. A. Bagnold (1933), I searched carefully for shells in oases and other localities. Of species now living in other parts of Africa, some were found only in the geological deposits of some oases, while a few appear to be living in this region in certain circumstances. Thus, shells of a land-snail common in tropical Africa were found in regions now totally arid, and the molluscs had evidently lived and multiplied there recently. Moreover, the freshwater species found in widely separated localities can breed only near or in water, and their dispersal or survival is an interesting problem.
Evidence will be given to show that small and purely temporary changes of precipitation—a matter of good or bad rain years—have disproportionate results in arid lands. Rapid re-colonization by molluscs follows exceptional rains, and in some instances a few individuals have survived long droughts. An explanation is offered in this paper of the alternations of barren and highly fossiliferous continental deposits found in this and other arid regions. Deductions as to climatic changes, made from the evidence of such alternations of superficial deposits in lands now or previously arid, are unsafe, and may give rise to confusion or doubtful correlations.
This paper, written in 1934, was intended to be a study of the past and present conditions of the southern part of the Libyan Desert, and to demonstrate some of the
The Conchostraca of the Cambrian Area of Comley, Shropshire, with a note on a New Variety of
Atops reticulatus
Walcott
Authors: Cobbold Edgar Sterling 
Published: October 2009

The principal object of this paper is to record species of Conchostraca that have been left over from my previous communications for more detailed study. Opportunity is also taken to record a specimen of
Atops reticulata
(Walcott) var., and thus to complete my account of the Cambrian faunas of Comley.

The index letters for the horizons used in this paper are those set out in my paper of 1921 (table facing p. 326). An index to the exposure numbers will be found in my 1927 paper (p. 553).
In the study of these fossils I am much indebted for guidance to the work of Drs. Ulrich and Bassler (1931), and I have followed their classification and, to a great extent, their nomenclature and method of description. It is most important, in dealing with these small fossils, to give a clear statement of their form. In the following pages the method generally adopted is : first, a note on the hinge-line; then, in consecutive order, the antero-dorsal angle, the anterior curves, the ventral curves, the posterior curves to the post-dorsal angle and hinge-line. The term “length” indicates the greatest extension parallel with the hinge-line; the “greatest length” (when necessary) is a measurement diagonally across the valve; “depth” is the extension at right angles to the hinge-line; “thickness,” the measure of the test may be smooth, punctate (like sharp needle punctures), pitted (relatively large punctæ), granular, tubercular, or scabrous. This last term is used when the test appears to have been broken