C. CALLAWAI Olf THE QUAKTZITES OF SHllOPSHIEE. 759 



being of quartz, with a matrix of quartz, green earth, and felspar. 

 The beds e are the ordinary green sandstone. The thin band d 

 deserves more attention. It is less than 1 foot in thickness, and is 

 a dark-coloured compact limestone. Associated with it is a little 

 red shale, and near the surface of the bed the limestone assumes the 

 same colour. This band is very fossiliferous, the most abundant 

 form being apparently trilobitic ; but it occurs in such a fragmentary 

 condition, and is of such an unusual type, that I cannot express any 

 opinion on its generic affinities. Brachiopoda are not uncommon: 

 two or three species are undeterminable, save that they belong to 

 the Tretenterata. One form, a minute roundish Lingulid, is appa- 

 rently new. What is of more importance for our purpose is that 

 the bed contains two well-known Malvern species, Kutorgina cingu- 

 lata, Bill., and Serjpulites fistula, Holl, both of which are found in 

 the same formation on the flanks of the Wrekin. The Holiybush 

 Sandstone is thus shown to overlie the quartz -rock, as in the Wrekin 

 district. It is about 300 or 400 feet in thickness, and extends to 

 the south-west for some distance ; but I have not traced it quite so 

 far as the quartzite. Indeed the exact limits of both formations 

 are not ascertained, the exposures towards the south-west being 

 very few and slight. 



I have had the good fortune to discover the presence of the 

 Shineton Shales in their true place above the Holiybush Sandstone 

 of this subarea. They are seen in the road leading up from the gap 

 towards Shoots Rough. The width exposed represents a thickness 

 of about 30 feet, and the dip is east or east-south-east apparently at 

 35°. They are succeeded by the Hoar-Edge grits (Lower Caradoc), 

 which plunge towards them at an angle of 60° or 70°. In the 

 Shineton district the shales are apparently conformable to the over- 

 lying Caradoc, and the chief evidence for the greater antiquity of 

 the former is derived from fossils. Here, however, the two forma- 

 tions are separated by a fault, which must be of considerable throw, 

 since, as I have reason to believe, neither the upper part of the 

 shales nor the lower part of the sandstone is represented. Following 

 the shales on the line of strike to the north-east into the ravine 

 between the Lawley and the sandstone escarpment of Hoar Edge, 

 where the escarpment approaches to within a quarter of a mile of 

 the hill, we find them well exposed on the stream, dipping to the 

 east at an angle of 50°, which probably represents the true dip more 

 accurately than the shallow road-section. I have detected in them 

 Lingulella Nicholsoni and Shineton Graptolites. From their general 

 appearance, and from the presence of Graptolites, I infer that these 

 beds belong to the middle part of the series. There are slight 

 indications, in the shape of the ground and in the soil, that the shales 

 run parallel to the Holiybush towards the south-west, where both 

 are cut off by the Hoar-Edge grits (Caradoc). 



The quartzite, Holiybush Sandstone, and Shineton Shales thus 

 appear to succeed each other in conformable succession ; but, from 

 the relations of the three groups at the Wrekin, from the number of 

 parallel faults which traverse the area, and from other considerations, 



