93 The feldspar varies greatly in habit, occurring in some rocks as interstitial, stringy masses, and in others as rounded grains with sutured borders, or as small subhedral erystalloblasts. Two distinct kinds of feld- spar are represented; albite-oligoclase, and potash feldspar—both ortho- clase and microcline. In the less metamorphosed quartzites, which usually contain less than 30 per cent total feldspar, nearly all the feldspar recog- nized was found to be plagioclase, much of which shows polysynthetic albite twinning. Many of the plagioclase crystals are zoned, and are commonly clouded by fine dust-like inclusions. In more highly feldspathic rocks, which seem to be also coarser and better crystallized, grains of orthoclase appear, and in some sections comprise an estimated 10 per cent of the rock. At higher metamorphic grades, where the rock passes into a quartz-mica-feldspar gneiss, a few crystalloblasts of microcline were observed, but microcline and orthoclase were not both noted in the same thin section of any of the rocks classed as quartzites. The foliation of the quartzites is due primarily to the flakes of biotite, which in some sections appear to have a nearly perfect planar arrange- ment. In general, there is no sign of linear structure, and thin sections parallel with the foliation plane show a haphazard pattern of grains. The muscovite shows much less tendency toward a common planar orientation than the biotite, and some relatively large grains have grown with their long axes across the foliation. In many specimens the quartz and feldspar grains are elongated and share in the general foliation. Needles of sillimanite, commonly grouped in radiating clusters, were observed in about half the thin sections examined, the largest noted about a millimetre long. Most of them are in the biotite flakes; although a few crystals of what appears to be the same mineral occur in quartz. Quartz-mica-feldspar Schist The quartz-mica-feldspar schists of the Wolverine complex differ in no essential respect, except in the proportion of quartz, from the feldspathic quartzites with which they are interbedded, and which themselves are either schistose or gneissic. Rocks in which quartz is not a dominant mineral are quite minor, and in the main are restricted to beds, usually less than 3 feet thick, that are correspondingly richer in biotite. Although most of them probably represent beds that were originally among the most fine-grained beds in the assemblage, many are now slightly coarser in texture than the quartzites with which they are interbedded, indicating that they recrystallize with greater ease than the quartz-rich rocks. Garnetiferous Schist and Quartzite Garnet-bearing rocks are of relatively restricted occurrence in the Wolverine complex. The abundant quartz-mica-garnet schists of the Tenakihi group apparently suffer a complete breakdown of garnet during alteration to quartz-mica-feldspar schists and gneisses. The Ingenika group rocks exposed in the syncline passing through Tomias Lake Valley have been metamorphosed to quartz-muscovite- garnet schists and quartzites, and garnet-bearing quartzitic conglomerates,