DIFFERENT PROVINCES OF NORTH AMERICA IN LATE PALEOZOIC TIME 57 



Following the red shales and sandstones which initiated the Joggins series 

 is a considerable thickness of gray shales and an increase in the number of 

 coal seams — 



"A monotonous sequence is quite noticeable of zones of regularly, evenly 

 bedded shales, thin sandstones, underclays, and coal, in alternation with massive, 

 uneven beds of cross-bedded sandstone that characteristically channel into the 

 underlying shale zones. . . . Commonly in association with the coals are thin, 

 shell-limestones which carry abundant Anthracomyas, Spirorbis, and leperditian 

 ostracods, a fact which may be advanced as an argument in favor of temporary 

 estuarine invasions, as the fauna is neither a distinctively marine nor a fresh- 

 water one." 1 



It is possible that this same series was deposited south of the Cobequids, 

 as at Parsboro on the Minas Basin, but the evidence is not conclusive. 



The Shulie formation is composed largely of coarse grits and conglomer- 

 ates, the material of which can be traced to the Cobequid region, with an 

 increase of the size of the pebbles in that direction. Also there is an ap- 

 preciable amount of material from the Joggins formation. The beds are 

 markedly uneven; showing ripples, or crests and hollows, some of consider- 

 able size. Drift logs and other vegetation are not uncommon. 



The characters cited above show that the Shulie formation, regarded by 

 Ells as Permo-Carboniferous but placed by Bell in upper Pennsylvanian time, 

 is almost entirely a subaerial deposit. Bell regards this as due to an elevation 

 of the Cobequid region at the close of the deposition of the Joggins formation. 

 It is probably in part the equivalent of the New Glasgow conglomerate. 



The whole of the Cumberland Basin was the site of accumulation from 

 the north, south, and west. In Boss Point time this was probably largely 

 from the Caledonian upland of New Brunswick, with possibly some contribu- 

 tion from the Cobequids; in Joggins time it was largely from the Cobequids 

 as at Styles Brook, 15 miles inland from the Joggins exposure, there are 

 1,000 feet of coarse conglomerate formed of pebbles directly traceable to the 

 Cobequids. In Shulie time the amount of material from the south is 

 increased in quantity. In conclusion it is stated — 



" (i) That a large proportion of the frner material of the 13,600 feet (Logan's 

 measurement) of Pennsylvanian beds of the Joggins section was probably derived 

 from the pre-Carboniferous highlands to the southwest, west, and northwest; 

 (2) that the excessive sedimentation in the Cumberland Basin was due to the 

 establishment of a geosyncline in early Pennsylvanian time and to proximity to 

 a Cobequid highland to the south; (3) that this Cobequid area was subject to 

 periodic rejuvenations resulting in renewed activities of erosion; (4) that the 

 derivation of these terrestrial sediments from the south, west, and northwest 

 has resulted in an interfingering of synchronous lens-like deposits. 



"Furthermore, the establishment of these successive Pennsylvanian periods 

 of uplift, with their consequent effects on the sedimentation, explains what had 



1 Bell, loc. cit., 1912, p. 368, 1914. 



