﻿Vol. 66. ] SCHISTS OF THE SCOTTISH HIGHLANDS. 615 



three, the middle fold (d) is certainly an anticline, as can be seen 

 on the hill-slopes above the termination of the Leven Schist outcrop 

 (d) north-east of the Lairigmor Valley. Therefore, it is clear that 

 the whole complex mass of quartzite, lying between the Leven 

 Schist outcrops (c) and (g), rests upon a folded substratum of Leven 

 Schist connecting these two outcrops (c) and (g) underground. 

 This important fact is confirmed, since : 



(1) the Leven Schist fold (e), shown in PI. XLIII, Sections B & 0, is anticlinal, 



as can be seen at both ends of its outcrop, especially on the western 

 slopes of the Binncin Mor ; 



(2) the small isolated exposure of Leven Schists, mapped to the south-west 



of the termination of the outcrop (e), and almost on the same line of 

 strike as the latter, also occupies the core of a clearly exposed anticline. 



(3) The fold of Leven Schists (./") which develops into prominence south of 



Kinlochleven (Section D), furnishes in the hill-face above the village 

 yet another example of an obvious anticline bringing the Leven Schists 

 up from beneath their covering of quartzite. In addition to this, the 

 hill-top definitely exposes the synclinal structure of the quartzite tongue 

 intervening between the two anticlines (/) and (d)— the anticline (e) has 

 dwindled out of recognition before reaching this side of the Leven 

 Valley. Further, the synclinal structure of the quartzite extending 

 down between / and g, although more complicated, can also be 

 recognized on piecing together certain important artificial exposures at 

 Kinlochleven with others afforded by the streams and hill-face south 

 of the village. 



Thus it may be claimed that the essential features of the sections 

 drawn in PI. XLIII have been established as far east as the out- 

 crop of the Leven Schist fold (g). Such minor twists and turns as 

 are indicated (Sections A & B) in the quartzite east of the out- 

 crop of the Aonach Beag Core do not require individual discussion, 

 as they are copied more or less directly from the mountain-slopes 

 bordering Glen Nevis (see map, PI. XLII). The thinning of the 

 quartzite at one point in Section B is, it may be mentioned in 

 passing, probably illusory, and due to the fact that the lower lobe 

 of quartzite shown in this section is fed from the north rather than 

 directly from above. 



Let us now return to the Leven Schist fold (g) : see map, PI. XLII. 

 Passing south-eastwards from this Leven Schist outcrop, we cross 

 a broad band of Glen Coe Quartzite, and then reach the Eilde Flags. 

 In so doing we have been ascending in the structural sequence, 

 since, as already pointed out, the faulted continuation of the Eilde 

 Flags at Allt Coire an Easain, within the cauldron subsidence of 

 Glen Coe, is merely separated by a band of Glen Coe Quartzite 

 from the Ballachulish Slide above. 



Under these circumstances it is clear that 



(1) the Leven Schist fold (g, Section D in PL XLIII) must close in an 



upward direction as indicated, and 



(2) the fold of quartzite underlying the Ballachulish Core, which we have 



already seen close before our eyes in Tom Meadhoin (fig. 4, p. 606), has 

 now, in its south-easterly extension, gaped widely enough to include a 

 core of the Eilde Flags (c/. Sects. A-D, PI. XLIII, & Sect. E, PL XLIV). 



