WEBEE CANOIS^. 387 



like the purer limestones below, wliich neither here nor in Ogclen Cailon 

 have suffered any interior contortions. 



The very uppermost members of the series are reddened by oxide of 

 iron. Overlying them, and for a short distance intercalated with them, are 

 coarse red sandstones, quite conformable, and dipping about 40^ to the east- 

 ward. These represent the lower beds of the Weber Quartzite group. 

 Among them are more or less conglomerates, of which the pebbles are quite 

 small, and of white quartz. Their general texture is gritty, with a tendency 

 to quartzite. Passing upward, the red zone, which is about 250 feet in 

 thickness, is succeeded by a rather finely-laminated gray and white quartz- 

 ite, above which the dip rapidly declines, varying from 20° to 16°, and 

 showing slight undulations in the strata. The curve from the steeper to the 

 lower dip is very gentle, and occurs without dislocation or cracking of the 

 strata. This low dip of 15° to 20° is held for about two miles up the 

 caiion, the strata becoming thicker and more heavily bedded, while the text- 

 ure of the quartzites grows more and more dense, and the occurrence of 

 conglomerates less frequent, until a mile and a half from the base of the 

 series there are no conglomerates at all, and the rock is a pure, compact 

 quartzite, varying in color from white and greenish- white to brown and 

 gray, and on its weathered surfaces being of a dark earthy brown. At 

 the lower railroad-tunnel, a sharp double curve is described by the strata. 

 They pass from the easterly dip of 16°, under a shallow synclinal, rising a 

 hundred feet on a dip of about 20° westward; then, passing over a sharp 

 anticlinal, dip again to the east at a steep angle of about 50° to 56°. In- 

 cluded in the strata of the quartzite, as displayed in the lower tunnel, there 

 is a small development of what seems to be an interstratified limestone, quite 

 black in color, and so siliceous as to scratch glass, yet effervescing freely 

 under acids. It contains about 83 per cent, of leilica and 5 per cent, of or- 

 ganic matter, the remainder being mostly carbonate of lime and magnesia. 

 Above the upper tunnel are about 1,500 feet of massive quartzites, white and 

 greenish-white, all having the easterly dip, and striking a little east of north. 

 The strike of the beds seems to deviate a little more and more to the east 

 of north as one ascends the canon. In these solid white quartzites are 

 peculiar cavities, like thsoe often left by decomposed fossils. They may 



