Mr. J. Hays Hammond in his paper, “Gold-mining in the Transvaal, South Africa,” read at the Richmond meeting of the American Institute of Mining Engineers in February, 1901, referring to this Old Granite, states: “There are at places intrusions from this enveloping granitic mass into the younger formations.”

The British form recognized under this designation appears to have been first recorded and figured from this country by J. de C. Sowerby (16, pl. lvii, fig. 30), who named it Asaphus or Trinucleus (?). He remarks “that no trace of the position of the eyes remains on the cast, which is also the case with the genus Trinucleus, Murchison”. This form was afterwards allocated by Salter to Phacops (Trimerocephalus) lœvis (Münst.) (13, p. 16, pl. i, figs. 5–7; 14, p. 1, pl. ix, figs. 1–5). Phillips had previously named the same species Calymene lœvis, Münst. (8, p. 129, pl. lv, fig. 250), a determination which both Salter (13, p. 16) and M'Coy (6, p. 404) showed to be at fault. This was complicated by the fact that Münster (7, pl. x, fig. 6; 7a, pl. v, fig. 4) had described two different forms under the same specific name, Trinucleus ? lœvis and Calymene lœvis, the latter of which Salter (13, p. 18) correctly adjudged to be a synonym of Phacops granulatus (Münst.) (Calymene auct.) (7a, pl. v, fig. 3). M'Coy had previously noted the identity of C. lœvis, Münst., with Calymene granulata of the same author, but assigned it to his genus Portlockia (6, p. 404).

Although the general path of the ice-sheet of the central valley of Scotland has been traced, no advantage has, up till now, been taken of the glacial distribution of boulders from a peculiar intrusive rock, which occurs in the Campsie Fells near Lennoxtown.

In a denehole at Abbey Wood, near Plumstead, there is shown in the Chalk a fault of unknown extent (but probably having a throw of only a few inches), the plane of the fault roughly coinciding with one of the chamber walls. This wall has a strongly slickensided surface for some superficial yards, and extends to the roof of the chamber where the deposit of allophane is contained between the two fault faces. In some instances this mineral may be seen adhering to the fault face, and the roof of the denehole is composed of it for a length of about 7 feet by 2 feet wide; other patches are to be observed where the roof has been broken away, so that it seems evident the allophane extends horizontally some distance between the Chalk and the Thanet Sand; this latter is about 32 feet thick here. The deposit appears to be a roughly wedge-shaped mass, the greatest width being at the top of the Chalk, and from there diminishing downwards into tongues of the mineral extending between the two boundaries of the fault. Mr. J. L. Foucar, B.Sc., F.C.S., who kindly submitted a specimen to analysis for me, says: “I find the following to represent its composition:—

The occurrence of a pre-Glacial marine terrace and raised beach along the coast of the south of Ireland was described by Messrs. Wright & Muff in 1904, and its development in the eastern part of co. Waterford was the subject of two short papers by the author in 1907 in this Magazine. Messrs. Wright & Muff (op. cit.) observed the same raised beach only in the south-eastern portion of co. Wexford, so that its recognition this summer by the author further north along the east coast of Ireland deserves recording, for it has been traced for several miles to the north and south of Courtown Harbour, and its height, characters, and relations to the overlying deposits show that it is a continuation of the same feature. The first locality to be mentioned is about 3 miles to the south of the village of Courtown, where relics of it are preserved between Roney Point and Salt Rock; it is still more distinct as a rock-terrace a little further north at Pollshone Head and Breanoge Head, but in the bays between these points the conditions are not favourable for its exposure, as there are no rocky cliffs, only extensive sand-dunes stretching along the shore. From Courtown Harbour northwards for about 2 miles to Duffcarrig Rocks sand-dunes are similarly developed, forming a nearly continuous line of ridges rising to heights of over 50 feet. Thick drift deposits occur behind them, but no pre-Glacial cliff or platform is exposed. At Duffcarrig Rocks solid rock again appears forming the headland, and we can recognize remnants of the rock-cut shelf in a much eroded and fissured condition.

Ware, about a mile west of Lyme Regis, is situated on the lower part of the Foxmould Sands of the Upper Greensand, and some distance above the ‘West Cliffs’, which are formed of Lower Lias clay and limestone.

Having had occasion to work at the Chalk Rock in this quarry, we took advantage of the opportunity to examine the whole of the Chalk exposed above that bed, which, owing to the inaccessibility of the upper half of the quarry, had not been examined in detail. The floor of the quarry coincides in part with the top of the Chalk Rock, and as there is a vertical face of nearly 50 feet of Chalk above it, the junction of the zones of Holaster planus and Micraster cortestudinarium was to be expected in the upper portion of the section, and it was with the object of defining the junction of these two zones that we paid attention to the higher beds.

During the summer of 1908 I examined in the field the contact metamorphosed limestones of the county Donegal, my attention being mainly confined to those masses of limestone occurring as xenoliths in the granite. These strongly metamorphosed limestones frequently contain the interesting rock named by Dr. B. H. Scott ‘Sphene-rock’, which (“Granitic Rocks of Donegal”: Journal of the Geological Society of Dublin, 1861, vol. ix, p. 288) he describes as “occurring in actual contact with garnet limestones wherever we find these rocks”. This Sphene-rock consists of allotriomorphic and hypidiomorphic felspars, with quartz, idiomorphic diopside and sphene, and in some localities zoisite, scapolite, etc.

In his interesting and excellent Voyage of the Discovery Captain R. F. Scott speculates on the former ice conditions of the Ross Sea and the adjacent ice formations. He regards the views he expresses on this subject as only speculations, so I trust that I shall not be considered ungenerous if I attempt to express what I understand to be his views, and then subject them to criticism. It may be that I have misunderstood Captain Scott. If this should be the case the method of treatment proposed will prevent confusion.

The Lower Severn Valley has been classic ground to students of river-development ever since Professor W. M. Davis visited and applied those principles of river-development which he had found so illuminating in his own country. Recorded in print, and developed by Mr. S. S. Buckman and others, these views have met with much support, and certainly have the advantage of explaining many otherwise unintelligible phenomena.