104 tions are represented, from recognizable sedimentary strata that have suffered low- to medium-grade regional metamorphism, to high-grade gneisses, migmatites, and rocks of granitic aspect. It is also apparent that the intensity of the “additional” metamorphism and replacement increases progressively toward a centre now represented by the grey granodiorite bodies northeast of Blackpine Lake, and toward a less well-defined, less intensely altered centre in the Butler Range at the east border of the map- area. Thus the processes that produced the Wolverine complex bear no direct relation to the regional metamorphism of the surrounding rocks. The changes involved in the development of the Wolverine complex are essentially those by which quartzites, schists (originally subgreywackes and greywackes), and limestones are converted into a rock that is identical, mineralogically and texturally, with a normal igneous granitic rock; the process is one of granitization (Read, 1943). The granitization has been accomplished by high-temperature solutions, which circulated mainly along foliation planes, from which they have intimately pervaded the pores of the rock itself, have selectively added or subtracted various chemical constituents, and have facilitated recrystallization and reconstitution of the material already in the rock. The nature of these solutions, their ultimate origin, and method of reaction, are fundamental questions in the entire problem of granitization and the origin of granites, and have given rise to much controversy and a voluminous literature (Gilluly, 1948, and numerous references therein). Reynolds (1946) has discussed the sequence of chemical changes that take place during such a process of granitization; the changes producing the “Wolverine complex” rocks appear to follow this sequence quite closely. According to this sequence, the quartzites are progressively feldspathized, with a marked increase in the alkali content of the rock, and a somewhat less pronounced enrichment in lime, magnesia, and iron oxides. The schists are first desilicated, with concomitant increase of alkali and lime, magnesia, and iron content; at a later stage, when feldspathization is more advanced, silica is added, and lime, magnesia, and iron oxides are removed. The limestones are likewise altered in two stages: first, toward a rock of ultrabasic composition (i.e., amphibolite), by addition of iron oxide, magnesia, alkalis, and alumina, together with a subtraction of lime and carbon dioxide; and then the ultrabasic rock is granitized by addition of silica and alkalis. All of these changes can be observed in the rocks northeast of Blackpine Lake. It is difficult to escape the conclusion that the leucogranite is an end product of the granitization of the Ingenika group sediments, and that, farther northeast, Tenakihi group rocks are trending toward the same end product. The grey granodiorite appears to be of a different immediate origin. Its contact with the sediments, and with the leucogranite supposedly derived from the sediments, is invariably sharp; and it shows no difference in character against rocks of different chemical composition. The outward form of the bodies, and the internal structure as revealed by planes of foliation, are apparently independent of the structure of the surrounding rocks. The stocks of grey granodiorite thus appear to have the charac- teristics of actively intrusive bodies, but there is no evidence that the