In the American Journal of Science in 1877, the writer described a remarkable extinct reptile from Colorado, under the name Stegosaurus armatus, and later a much more perfect specimen of another species, Stegosaurus ungulatus, from essentially the same horizon, in the Jurassic of Wyoming. The latter specimen was in fine preservation, and the more important parts of the skull and skeleton, and especially of the remarkable dermal armour, were secured. Subsequently, more than twenty other specimens of these and other species were obtained, so that nearly every part of the osseous structure thus became known, and only portions of the dermal armour were in doubt. A fortunate discovery cleared away most of the doubt in regard to one species, Stegosaurus stenops, as the type specimen had the skull, skeleton, and dermal armour together when entombed, and almost in the position they were when the animal died.

It is now fifty years since Charpentier told us that the heaps of Northern boulders which stretch across the plains of Prussia and Saxony mark the ancient limits of the great glacier of Scandinavia, and that the smaller debris met with farther south represents the stuff carried on by the torrents that escaped from the margin of the ice. All this he explained to his incredulous contemporaries, and now after half a century of debate, in which every other conceivable mode of accounting for the phenomena has been tried, it seems to he agreed on all hands that he was right—right in every particular—but, strange to say, it appears to be now generally forgotten that he was the man to whom we owe the first sketch of this explanation.

Among the many valleys of Daghestan that are interesting to the geologist there are none more remarkable than the channel by which the river Sulak passes through the chain of Cretaceous and Jurassic mountains which borders Inner Daghestan. Just above the entrance of this defile the four rivers Koissu unite in one stream, which in a series of cataracts tears through a stupendous chasm some fifteen miles in length, cutting the huge ridge almost at right angles to its axis.

On the Italian side of the Alps a similar set of lignite beds occurs as on the Swiss side. But these Italian lignites, although occurring beneath, are not underlaid by glacial deposits.

The Geological Survey of India Records, vol. xxiv. part 1, 1890, only came to hand to-day, enabling me to see Mr. Middlemiss's late paper on the Salt Range.

[From a collection of stones obtained from the refuse-heaps of the Kimberley Mines by Mr. Louis Atkinson, a selection was made by Prof. T. Rupert Jones and, by kind permission of Prof. Bonney, was submitted to him for examination, in packets marked I.—VIII. and X. Specimen No. IX. was sent many years ago, as a traprock with garnets from the Vaal River, by Mr. Robert Crofts Jones.—T. R. J.]

Glen Fruin is a quiet secluded glen, about six miles in length, extending in a north-westerly direction between Lochlomond and the Gareloch, and opening off the neck of land which divides those lochs at between 200 and 300 feet above the sea. To the south-east, it slopes towards Lochlomond, of which the Fruin water is one of the principal affluents. On the west it is divided from the Gareloch by a range of hills 1000 or 1200 feet in height, which at its upper extremity subside into a col or pass of 600 or 700 feet. This upper part of the glen is composed of the mica and clay slates common to the Western Highlands. The lower part is formed of beds of the Calciferous Sandstone series, which have here been faulted down against the older formations.