EELATIONS OF THE AJIBIK QUARTZITE. 295 



iron-bearing- formation. In the eastern part of tlie di>strict the ({uartzite 

 grades above into a slate, and bek)Av it rests npon another slate. 



In the area west of Goose Lake the Wewe slate, as has been said, 

 appears to grade up into the Ajibik quartzite, in many places the boundary 

 line between the two being somewhat arbitrai-ily placed. 



In the quartzite range in sec. 29, T. 47 N., R. 2(J W. (Atbis Sheet 

 XXXII), the quartzite rests immediately upon tlie Archcan, the Wewe slate 

 not appearing between the two, as is the case to the eastward. This is 

 explained by the fact that the transgression of the sea was from the east, 

 but it is not impossible that the lower part of the quartzite is really the 

 equivalent of the upper part of the Wewe slate, sand being deposited near 

 shore at the same time that mud Avas being deposited offshore. 



East of Teal Lake, supposing the slate belt in tlie middle of the 

 quartzite to belong with the Wewe slate, there is a transition from the slate 

 u])ward into the quartzite. West of Teal Lake it has been seen that the 

 inferior formations of the Lower Marquette series were not deposited, and 

 therefore that the quartzites rest directly upon the Archean. In the petro- 

 graphical description it has been indicated that here basal conglomerates 

 occur. North of the west end of Teal Lake, and at various places for a 

 few miles west, the actual contacts between the quartzite aud the green 

 schists, greenstone-conglomerates, and amygdaloids of the Archean are 

 found. (_)ne of the best localities at which to observe this contact is just 

 north of the west end of Teal Lake (Atlas Sheet XXVII). Here the green 

 schist strikes approximately ea^st and west, and its schistose structure dips at 

 a high angle — 75° to 80° — to the south. However, the contact of the quartz- 

 ite and schist dips but 55° to the south, so that the iibers of the schist abut 

 against the contact plane at an acute angle (fig. 14). Above the contact 

 plane is a genuine basal conglomerate, the pebbles of which are mainly 

 derived from the schist, but with which are also large pebbles of quartz, 

 some of them 8 or 9 inches in greatest diameter. Besides the green schist 

 and quartzite pebbles, there are also present abundant pebbles of a more 

 acid schist which is like the acidic schists occumng in the Northern Com- 

 plex north of the stone quarry at Carp River. There can be no doubt 

 that here the green schist had become foliated and was deeply truncated 

 before the deposition of the overlying conglomerate. 



