The igneous rocks of the Stanner-Hanter district are included within the Geological Survey I-inch map, sheet 56 S.E., (Old Series), and form three hog-backed hills, Stanner Rocks, Worsell Wood, and Hanter Hill, which are prominent features in the country between New Radnor and Kington, close to the Welsh border. This line of hills trends from south-west to north-east, though the separate ridges are arranged en échelon. Stanner Rocks (I,08I feet), is separated from Worsell Wrood (about 940 feet), by the alluvial plain of the Gilwern Brook, while there is a low col between Worsell Wood and Hanter Hill (I,36I feet).

A Small series of fossils, recently collected by Mr. James L. Begg mainly from the Ordovician beds of Girvan and sent to me for examination, include some interesting specimens amongst which is a species of trilobite which must be put in a new genus. My thanks are due to Mr. Andrew Ferguson, of the Geological Department of Glasgow University, for making the photographs of the specimens.

The occurrence of massive reddish sandstones and quartzites lying between the Coal Measures and Carboniferous Limestone in the Bristol District has long been known. From their position and distinctive lithology, these beds have been referred to as the Millstone Grit by many early writers, amongst whom Austin (1865) may be mentioned. However, it has been shown that in part these beds are of Lower Carboniferous age. This was recognized by Vaughan (1905) notably in the Avon Section and at Long Ashton, where red grits and sandstones, previously regarded as Millstone Grit, were shown to represent horizon ∈, and later found by him to be of D3 age. Dr. Stanley Smith (1930) has shown at Wick, on the eastern border of the Bristol Coalfield, that the lower part of the red and gritty beds of that area are likewise of Avonian D3 age. Dr. Smith suggested a non-sequence between Lower and Upper Carboniferous to occur some 30 feet above a thin gritty limestone, the “Mollusca Band” of D3 age. Between this horizon and that from which Yorkian plants were recorded (Crookall in Smith, 1930, p. 342), some 350 to 400 feet of grits and micaceous shales occurred. These beds were of uncertain age, and Dr. Smith held the opinion that part and probably most of these beds belong to the Upper Carboniferous.

This paper is chiefly concerned with the micro-crinoid Allagecrinus biplex, recent discoveries of which have added considerably to our knowledge of the species. Others like A. auslinii, Callimorphocrinus scoticus, and C. elongatus are only briefly noticed. Their adequate study and illustration must be deferred to more settled times.

The younger rocks of Iceland (Pliocene to Present Day) occupy the broad median zone shown in Text-fig. I; the boundaries are only approximate in places, and information is lacking with regard to the eastern one particularly. Outside this zone early Tertiary basalts predominate but (I) the uppermost basalts are regarded by some authors as Quaternary, (2) Quaternary and Recent volcanic rocks occur in the Snaefells Peninsula and in Skagi. The thickness of the early Tertiary series has been estimated at 3,000 m.; it may well be more, and it is reasonable to suppose that originally these basalts extended over the site of the median zone. Hitherto all workers in Icelandic geology have considered the zone to be a graben where the older rocks have been faulted or tilted downwards, but recently R. A. Sonder (1, 2) has put forward the startling idea that it is a horst, a view which is discussed, and not unfavourably, by H. G. Backlund (3). Before considering this new conception attention will be drawn to evidence in the neighbourhood of the north-western boundary of the zone, evidence which is not mentioned by Sonder and which, although it has been known for over 70 years, is often ignored or forgotten by writers on Icelandic tectonics.

The Cretaceous System of England, according to A. J. Jukes-Browne1 is “naturally divisible into two distinct and different series of strata”, namely a lower series consisting chiefly of sands and clays, and an upper series, consisting mainly of chalk. The succession on the whole is easy to unravel, and was correctly described (even before the name Cretaceous had been thought of) by Webster in his Letters, written in 1811 and published in 1816 in Sir Henry Englefield's Isle of Wight; it is almost exactly the same as we recognize it to-day. Two slight changes have been made, but they have been considered by some to be changes for the worse. Firstly, the beds to which the name“Greensand” had originally been applied by Smith and Webster2 are now called “Upper” Greensand, a term that has given rise to much confusion3; and, secondly, the “Ferruginous Sands” are now known as “Lower” Greensand, a name that was strongly condemned by workers like Fitton, Godwin-Austen, and Judd. It is on record4 that even Jukes-Browne admitted that he had long been endeavouring to do away with the awkward and misleading terms “Upper” and “Lower” Greensand ; but these names, though better not used without locality, have now become too familiar and are too useful for mapping to be abandoned entirely in favour of the more precise stage names Cenomanian, Albian, and Aptian.