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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