34 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 75 



below Glenogle. but their stratigraphic relations to the Glenogle 

 shales have not been determined. The evidence of the graptolitic 

 faunu'.es, hovvever, is that the Glenogle shales are superjacent to the 

 Sinclair shales. 



Sinclair Formation : 



This is described in detail in the Wonah Ridge section on Sinclair 

 Mountain (p. 14). It should include an extension of the Glenogle 

 graptolitic shales, and the upper part may be equivalent to the 

 latter, but at present we do not know of an unbroken section where 

 the faunas of the two formations occur. It will presumably be found 

 in Kicking Horse Canyon or vicinity, as the Glenogle shale occurs 

 near Glenogle station, and 3.5 miles (5.6 km.) west of there, on both 

 sides of Kicking Horse Canyon. A little below tunnel No. 31-08 on 

 the Canadian Pacific Railway, a thin band of black argillaceous shale 

 is crowded with graptolites on some of its surfaces. In a small col- 

 lection Mrs Walcott and I made there, Dr. Ruedemann identified the 

 following (locality 21k) : 



Clonograptus sp. nov. cf. icncUiis (Linnar-son) 

 Loganograptus logani Hall 

 Tetragraptus similis (bigsbyi) Hall 

 Tetragraptiis sp. nov. aff. fruticosits Hall 

 Tetragraptus (Etagr.) cf. Icntns Ruedemann 

 Phyllograptus cf. typus Hall (gigantic form) 

 Didymograptus cf. extensus Hall 

 Didyniograptus bifidus Hall 

 Didymograptus sp. nov. aff. gracilis Tornquist 



He wrote as follows : 



This fauna is decidedly older than the one Lapworth published from the 

 Kicking Horse Pass (^Glenogle). It is a distinct Deep Kill fauna, belonging 

 to the Didymograptus bifidus horizon, but containing also some older elements, 

 as the Clonograptus, Tetragraptus aff. fruticosus and Didymograptus cf. 

 extensus. which suggest a mixture with the preceding horizon. 



There is a considerable thickness of brownish gray arenaceous 

 shales above and below the black graptolite shales that are twisted and 

 folded and thrust over westward onto liinestones of the Ozarkian 

 Mons formation. The locality is about 3.5 miles (5.6 km.) w^est of 

 the typical locality of the formation just west of Glenogle. A further 

 study of this section and that of the norh end of the Beaverfoot Range 

 may disclose the relations of the Glenogle shales to the Sinclair shales 

 beneath and the superjacent ^^'onah quartzite, which appears to be 

 present in the section, or if it is not. to the limestones of the Beaver- 

 foot formation. 



