elle 105 margins of the bodies have been chilled, and there is a puzzling lack of dykes of granodiorite into the surrounding rocks, or of inclusions of these rocks within the granodiorite. The general pattern of occurrence of migmatite and leucogranite, and, especially, the distribution of the pegmatite and aplite dykes, would seem to indicate strongly that much of the alleged granitizing solutions and the pegmatite-forming fluid was distributed from the space now occupied by the grey granodiorite. It would seem to follow that the granitizing solu- tions, the material that formed the pegmatite and aplite bodies, and the ‘magma’ that consolidated into grey granodiorite are genetically con- nected, and are all products of a common syntectic (or igneous) activity that developed in a relatively narrow zone trending northeast through the Tenakihi and Ingenika group rocks. This activity has taken place at relatively higher levels at each end of the zone, so that erosion has revealed more highly granitized rocks near Blackpine Lake and in the Butler Range. A tentative sequence of events resulting in the production of the Wolverine complex rocks might be summarized as follows: (1) The first stage of the processes unique to the Wolverine complex involved the emplacement and consolidation of the grey granodiorite. The material forming the stocks was apparently actively intrusive into the Ingenika and Tenakihi group sediments, which were probably already regionally metamorphosed. The intrusion probably caused severe local deformation of the rocks, resulting in the confused structures found within the Wolverine complex rocks, but no pronounced regional stresses were active during the time of intrusion and consolidation, and the granodiorite solidified with an internal structure controlled mainly by its external form and method of intrusion. The contact action of this intrusion on the surrounding rock is not known, but there was apparently very limited mutual reaction or gradational assimilation between the granodiorite and the intruded rocks. (2) After, or perhaps partly contemporaneous with the later stages of, consolidation of at least the upper part of the granodiorite stocks, fractures within the granodiorite and along its contact admitted solutions of great chemical activity, which travelled distances of several thousand feet, and perhaps miles, into the adjacent older formations. The solutions selectively attacked the regionally metamorphosed sediments and made them over toward granitic material. Only near the granodiorite bodies, in and around which were located the feeding channels, were the solutions abund- ant enough or potent enough to complete the process of granitization; there they formed leucogranites, some of which consolidated in situ, others of which were mobilized and travelled along foliation planes and fractures in the partly granitized sediments to form sills and dykes. At greater distances from the feeding channels, the intermediate rock types represented by the migmatites, quartz-mica-feldspar gneisses, feld- spathic quartzites, and schists formed from the clastic sediments, and amphibolites, skarns, and silicated marbles, formed from the limestones, were produced. The solutions carrying magnesia, iron, alkalis, and lime travelled farthest; they were followed by less mobile, or perhaps less plentiful, solutions that introduced alumina, more alkalis, and redistributed silica. There is no evidence of appreciable deformation due to local or