The Clitheroe Limestone of Coplow, Salt Hill, and Bellman quarries is redescribed, particularly from the point of view of the origin and structure of the reef knolls and their relation to the surrounding deposits. Coplow knoll is considered to be the exposed part of a lenticular mass of upper C1 reef limestone which originally sloped steeply east. An earth movement within the C2 zone is marked by limestone breccias and a boulder bed, but there seems no evidence of pronounced erosion. A later uplift preceded the deposition of the Worston Shales. Slickensiding in the reef limestone is briefly discussed and possible effects of compaction of the sediments are considered. Three growth stages in reef formation are postulated.

Recent published work on the origin of the South Wales coals has shown that the “original deposition theory” is invalid; the pronounced devolatilization of the coals is due to a cause which operated after the formation of all of the seams and the rate of change of the volatiles is governed by a function which can be expressed as an empirical equation. Nevertheless minor variations in coal seam volatiles arising from differences in original composition of vegetation are recognized, and of several examples one is given from the Northumbrian geo-syncline where the highest volatiles are in the lowest Carboniferous Limestone coals and where the extreme variation throughout a sequence of 7,000 feet of coal-bearing strata is 11%. The minor variations lessen progressively if the coal seams become devolatilized. As illustrated by examples from American and European fields, a most important factor in coal seam devolatilization is orogenic pressure with incidental frictional heat.

The present basis of comparison of essential coal-substances (fixed carbon and volatiles) is shown to be empirical; a mathematical comparison should be based on the original composition of the coal (not peat) substance. it is shown that 50% fixed carbon and 50% volatiles (d.a.f.) constitute good average figures for the original composition of the coal substance of Carboniferous coals. Loss of weight in devolatilized coals is suffered only by the volatiles so that the best basis of mathematical comparison is the 50% fixed carbon (d.a.f.). The volatile percentages of the South Wales seams when calculated on this basis all show a pronounced drop in values, and on the 50% fixed carbon basis it is necessary to find a new controlling function for the rate of change of volatiles in coal seams lying in vertical sequence. It is found that this is best expressed by the following exponential equation:

where v2 and v1 represent the volatiles of the lower and upper seams respectively, y is the vertical distance in feet of v2 below v1; and θ is the angle of dip of the zero plane previously determined in South Wales as 5°.

In a previous number of the Geological Magazine Professor O. T. Jones questioned the existence of the metamorphism of the Trias in the autochthonous Alps. The authors give a reply stating accurately their observations. They also recall similar observations made by other authors.

The assemblage of facts cited enables us to assert that this metamorphism exists. The problem is very complex indeed; but the fact that this metamorphism seems to be in contradiction to the classical theories about alpine orogenesis does not allow one to deny its reality. The authors maintain that the solution of the problem must be looked for in the new ideas on “fronts” of metamorphism.

An abnormal specimen of Dictyonema flabelliforme showing close-set bifurcation of the branches in a portion of the distal mesh is described and figured, and possible interpretations are considered.

Thrusting along a shear plane at the continental margins may result in a temporary up-bulging of the margins above sea-level. During the time of exposure erosion by streams should have incised canyons which now, after isostatic readjustment of the margins, constitute the widely distributed submarine canyons. Known downwarped peneplains below the surface of continental shelves may have been developed on the bulged margins by long continued erosion. The margins may, thus, have served as- sources of some sediments now found on land and believed to have been derived from a seaward direction.

Graptolites found on the east side of Newport Bay, Pembrokeshire, support the original interpretation of the 1857 edition of the one-inch geological map of the area that the rocks there are of Ordovician age and not Silurian as shown in more recent maps.

Present knowledge of the tectonics of the Struan area is summarized. Recumbent-folds and incipient boudinage are recorded in the Struan Flags. The different types of lineation present are described; it is pointed out that all types present are mutually parallel. Simple kinematic analysis of an exposure north-west of Dalnacardoch, demonstrates that the lineations coincide more or less closely, with the axis of rolling; they are therefore b-lineations. The need for further field-work is stressed, and the type of data required is indicated.

An example is described of a dyke feeding a lava flow in the Tertiary basalt plateau of North-East Ireland. The dyke has an erratic course and branches into several veinlets, but otherwise it displays the usual characters of a dyke. Continuity between dyke and flow is seen in five places in the restricted area of outcrop of the flow. The possible relationship of the dykes and volcanic plugs of Antrim to the plateau lavas is briefly discussed.

An abnormal lithological development of the Chalk Rock occurs in the neighbourhood of Winterborne Abbas, South Dorset, where it contains pebbles of Upper Greensand material. Two exposures of this rock have previously been recorded but further information regarding this variant of the Chalk Rock was obtained during the resurvey of the area in 1936. A possible source of origin for the derived material is suggested.

The suggestions made by previous writers are summarized, and Andersson's Solifluction Theory is discussed in detail. Reasons are given why the author believes that solifluction alone could not provide the explanation. Stone runs are shown to be largely an accident of past climate and the structure and lithology of the Upper Quartzite Series rocks. A note on the economic aspect of stone runs is added.

The vertebrate fauna from the Bugti Bone Beds was at first assigned an Upper Nari age by Pilgrim. Later, he assigned them to the Gaj, on the basis of the identification of three species of Ostrea by Vredenburg. Regional field work carried out by members of the geological staff of the Burmah Oil Co., Ltd., showed that the beds really belonged to the Upper Nari after all. Re-examination shows that the identifications of the oysters cannot be upheld, and that there is no palaeontological evidence against the beds being of Upper Nari (Basal Miocene) age. It is therefore necessary to regard the vertebrate fauna as being of Upper Nari (Basal Miocene) age. A list of the species is given for purposes of reference.

It has previously been thought that in Sind the Meting Limestone Laki Limestone succession was equivalent to the Bolan Limestone, and that argillaceous beds, which are occasionally developed above the Laki Limestone and below the overlying Khirthar, represented the Ghazij Shales. Recent evidence indicates that these higher argillaceous beds are the representatives of the Shales with Alabaster of the Western Punjab, that in Sind the Ghazij Shales are cut out at the Laki/Ranikot unconformity, and that the Meting Limestone-Laki Limestone succession represents calcareous horizons higher up in the Laki series than the Bolan Limestone.

Certain small discrepancies in Du Toit's (1937) reconstruction of Gondwanaland are discussed and suggestions made as to its mode of disruption.

Perisphinctes listeri (de Haan). 1825. from the Corallian Beds, and Titanites cingulatus (de Haan), 1825, from the Portland Beds, are valid species that have been overlooked. The original figures on which they were based are reproduced.

To investigate the problem of porosity of wind deposited sands a sample of sand similar to Libyan Desert sand was used for wind tunnel experiments. Average velocity of wind—Average Porosity Curve was obtained for the first time, proving that low wind velocity produces higher porosity than high wind velocity, and that the relationship obtained agrees with the laws governing “vertical” deposition of sands.

The Rhaetic section at Newark is described and compared with sections further south. The Lower Rhaetic is locally sub-zoned by constant bone-bed horizons. In the south-west of the area a much richer fauna occurs and the zone-fossil Pteria contorta appears lower in the succession. The explanation offered is that a lagoon phase existed in the more northerly district.

A section from the extinct waterway of the Little Ouse to the former Red Mere in west Suffolk is described, which shows that the lake mans succeed the clay flanges extending from the roddon silts. Thus the Fenland Meres formed in the course of the Coastal or Upper Silts transgression of the Fenland Basin, during which raised banks of silt were built along the tidal waterways, and these ponded back the fresh water. The Meres are shown to be roughly similar in age and manner of formation to the Norfolk Broads.

A description of the Ingletonian Series is given, with special reference to the sedimentary structures which occur and their use in determining the nature of the folding of the beds; this is shown to be isoclinal. The age of the series is discussed, and it is considered to be in all probability Pre-Cambrian.

Geomorphic evidence is described of very recent upwarping of the shore of Hawke Bay north of Napier, and, as this is of local extent, the suggestion is made that here and in adjoining coastal districts folding is, or recently has been, in progress, with this and another upheaved rib farther to the north-east as anticlinal axes. The coastally drowned areas of Poverty Bay and the north-east and south-west corners of Hawke Bay have escaped the upheaval, and it is suggested that they occupy negative, or synclinal, axes of a fold pattern.

Recorded data are insufficient to show to what extent, if at all, the axes of transverse upheaval recognized in the coastal districts extend westward across the main geanticline of the island. All or most of the axial ranges in this belt have recently been rising, however, for this is indicated by the presence of terraces in the valleys of outflowing rivers and by the fact that the vertical intervals between terraces increase upstream.