484 DEPARTMENT OF THE INTERIOR 



2 GEORGE V., A. 1912 



labradorite) and 5 per cent to biotite, titanite, epidote, and limonite. All but 

 tbe epidote and limonite are of detrital origin. The feldspars are greatly kaolin- 

 ized and were doubtless nearly as much altered before the fragments found their 

 places in the bed. The biotite occurs in thin, ragged and crinkled flakes, quite 

 like those which may be seen in micaceous sands of the present day. The specific 

 gravity of the specimen is 2-625. 



The mineralogical composition of the sandstone is like that of the secularly 

 weathered shell of the Remmel granodiorite below the agglomerate, member A. 

 In both cases hornblende fails to appear, as if it had been leached out completely 

 during the ancient weathering. Otherwise the important constituents of the 

 Rem m el batholith are all represented in the sandstone. There can remain no 

 doubt that the sandstone has resulted from the destruction of the* batholith. It 

 is probable that the various sandstones overlying member B have had a like 

 origin, but, from the lack of microscopic analysis, the proof of this has not yet 

 been completed. 



Member G is exposed in but a small area, occurring at the northern limit 

 of the Boundary belt on the eastern slope of the Chuchuwanten valley. Farther 

 south it is faulted out of sight by the Chuchuwanten fault. This member is the 

 most highly variegated portion of the Pasayten series. It consists of a group of 

 rapidly alternating red argillaceous sandstones and grits ; gray, feldspathic, often 

 pebbly sandstone and grit; with red, gray and green conglomerate. The beds 

 range from an inch or less to twenty feet in thickness. The pebbles of the con- 

 glomerates are composed of hard, gray quartzite, chert, and hard, red and gray 

 slate. Some of the larger, always well rounded boulders are as much as two 

 feet in diameter. 



These beds of G have variable attitudes; the rapid changes are probably 

 connected with the adjacent fault. A mile or more east of Chuchuwanten creek 

 the member dips rather steadily about 20 degrees to the north and visibly over- 

 lies member B. It is itself there overlain by 400 feet of member D, which on 

 the north gradually approaches a horizontal position and is terminated above by 

 an erosion-surface. The measurement of the thickness of member G, 600 feet, 

 was made at this locality. 



Member D is lithologically like the great basal sandstone but tends to assume 

 a dominant green colour. 



Member E is well exposed near the Boundary slash in a cliff overlooking 

 Chuchuwanten creek on its west side. The conglomerate is of medium coarse- 

 ness and seems to contain few pebbles not composed of gray quartzite or vein 

 quartz. It is overlain by member F, some 1,500 feet of green and gray felds- 

 pathic sandstone of rather dark tints but essentially like the sandstone below the 

 conglomerate E. 



Member G is a 200-foot bed of conglomerate recalling E in its general 

 character but abundantly charged with pebbles of an andesitic nature — the only 

 known occurrence of such material in the conglomerates of the series. 



Member H is not well exposed; so far as seen, it is a homogeneous, green, 

 feldspathic sandstone. The estimate of the thickness, 3,500 feet, though so 



