In the Chambéry region, Jura folds with a north-north-west trend meet the boundary of the Subalpine zone, which strikes north-north-east. The two fold trends were probably not formed at exactly the same time. Minor folding, thrusting on steep planes, wrench-faulting, formation of sub-horizontal stylolites, and opening of filled joints all took place during a succession of tectonic events with maximum compression at about east-west, after the aforementioned fold-trends had been formed. The evidence considered in this study seems incompatible with hypotheses of deformation by gravitational gliding.

Minor folds in slates and sandstones are upright in the south and northerly overturned towards the north, and plunge approximately E.N.E. and W.S.W. towards three major N.W.–S.E. dextral faults. The folds are monoclinal and angular; regardless of attitude, the short limbs lie on the northerly sides of anticlines. Both slaty and fracture cleavages tend to parallel axial planes and local directions of extension. Similarly, the vertical axial planes may closely parallel those of major folds.

Boudins and W.N.W.–E.S.E. dextral oblique faults indicate extension along fold hinges, N.W.–S.E. dextral cross faults a change to N.–S. compression. Folded basic dykes parallel to faults and joints suggest early initiation of the fractures.

Evidence is presented which suggests that there is a strong angular unconformity between the Mesozoic sediments and the Tertiary lavas in certain parts of the Island of Mull. The conclusion is drawn that folding movements peripheral to the volcanic centre occurred both before and after the eruption of the main lava succession.

The magnetic susceptibility anisotropy of specimens of a glacial till is described and used to define a magnetic fabric. This is compared with the fabric established by small particle and stone orientation. The maximum susceptibility direction is shown to be similar to the preferred direction of the long axes of particles and stones.

Five thousand feet of Upper Arenig turbidites are described with reference to their provenance and mechanism of emplacement. The turbidites were emplaced in a gently curving E.–W. trough whose width was approximately 20 miles and minimum length 50 miles. Axial and lateral derivation are recognized and it is suggested that entirely different mechanisms were responsible for the emplacement of each type.

Pitchstones and obsidians from Arran, Eigg, and Iceland, are shown to have small but distinct differences in their major-and trace-element composition, and it is concluded that acid magma in the British Tertiary as represented by the pitchstones from Arran and Eigg maybe more variable in composition than that of the Icelandic subprovince. Fourteen new analyses are represented.

Mineral and chemical evidence suggest that an unusual rock from the Upper Manganese Shales of Diphwys is of spilitic origin, despite certain geochemical anomalies. Some similarities of the rock to the shales themselves are only superficial, and a metasomatic origin is precluded; the rock is also very distinct from the “greenstone” sills of the region.

Chalk Rock lithology suggests shallow-water conditions, but the fauna has been said (Woods, 1897; Jukes-Brown, 1904) to imply a depth between about 100–500 fm. A study of the sponges which are numerous in the Oxfordshire–Hertfordshire area shows that these form a fauna of the sort which is typical of the Chalk as a whole, with Hexactinellida predominant as was pointed out by Woods; this is a fauna of deep-water type by both modern and Cretaceous standards. The depth which these sponges imply need, however, not be much more than 100 fm., and their presence need have no direct bearing on the depth at which erosional features were formed.