I9i 



KOomltres hallana Walcott ; Stropheodonta demissa (Con- 

 rad), Schizophoria striatula (Schlotheim), 

 Chenungensis var. arctostriatus (Hall), Phillips- 

 astraea verrilli Meek, Syringopora cf. perelegans 

 Billings, and other Devonian species. 



A few yards beyond the west end of the 

 siding, the railway cuts through a down- 

 faulted block of dark brown Fernie shales 

 containing ammonites, which indicate that they 

 are Jurassic in age. 

 96-2 m. The upper part of Johnson creek separates 



153-9 km. Sawback range from Castle Mountain range. 

 It follows in a fault valley. Four miles from 

 its mouth the stream has been diverted to the 

 south by the down-faulted block of Jurassic 

 shales referred to above. From this point 

 there is an excellent view of Castle mountain 

 with its perpendicular cliffs and broad amphi- 

 theatre behind. 



99 m. Castle — Alt. 4,660 ft. (1, 420 m.), is situated 



158-4 km. at the base of Castle mountain. West of the 

 station the railway follows along the base of 

 this mountain for over 10 miles (16-1 km.). 

 The eastern end of the mountain is terminated 

 by a large pinnacle which, from the railway, 

 resembles the ruins of a massive castle; hence 

 the name. The accompanying illustration 

 shows the character of the rock in Castle 

 mountain. The upper slopes are Cambrian. 

 It is capped by the thin-bedded red-weathering 

 limestones and shales of the Bosworth formation 

 (Upper Cambrian). The perpendicular cliffs 

 at the top represent the Eldon formation. 

 This is the type locality and this formation 

 has a measured thickness of 2,728 feet (832 m.). 

 The Stephen formation is about 600 feet (183 m.) 

 thick, and forms a very flat talus-covered 

 slope, while the Cathedral formation below is 

 about 1,500 feet (458 m.) thick and forms 

 a precipitous slope. These three formations 

 are Middle Cambrian in age. The Lower 

 Cambrian beds are largely quartzitic and 

 form brush-covered, irregular slopes. 



