that sometimes follow the bedding planes and sometimes the planes of movement.” The boundaries of the intrusive peridotites, etc. are sharply marked faults separating them from the schists of the Humboldt and Olivine Ranges to the east, and from the semi-schist of the Bryneira Ranges to the west, a point first noted by McKay (1881) and emphasised by the more detailed examinations of Park (1887). Further north, Turner (1930) has shown that the peridotites, etc., occupy a fault-zone between the schists of the Olivine Range and the much more strongly metamorphosed schists of the Hope-Blue River Range to the west. In the south, though he did not investigate in detail the character of the formations bounding the serpentine on either side beyond commenting that they comprised chiefly the greywackes of the Te Anau series and their slightly metamorphosed equivalents, Hutton (1937) recognised that “the actual contacts on both sides are marked by zones of intense shearing along which fault-breccias have been developed.” It is, however, noteworthy that throughout its extent the peridotites, etc., of this long belt like those of the Great Serpentine Belt of New South Wales (Benson, 1926, p. 39, fig. 11) have been injected into an almost vertical fault-zone, so that active horizontal thrusting had ceased at the time of their intrusion, which in our present case is believed to have been at the close of the Late-Jurassic—Early-Cretaceous (?) orogeny. A detailed interpretation of the structures and textures of the above described metamorphic rocks must await petrofabric investigation of oriented specimens. That they have suffered intense lateral compression, shearing and “external rotation” seems apparent, and the general west-south-westerly convexity of the boundaries of the several metamorphic sub-zones accords with the evidence derived from Manapouri (Turner, 1937-8), and Eastern Otago (Turner, 1938), that the compressive stresses acted across N.N.W.-N. axes and may have been connected with the westerly to south-westerly superficial thrusting near Preservation Inlet. Further, it seems, from the distribution of the various grades of metamorphism, that a late phase of the crust-movements was a flexure on a broad scale resulting in an uplift in the regions north and east of the Lake Wakatipu regions and a southward pitching syncline to the west where the rocks of the Chl. 1 sub-zone are bounded to east and west by those of Chl. 2 and 3 [Hutton and Turner, 1936, confirming McKay's' (1881) earlier studies]. The northern limit of this major syncline is recognisable in the southern margin of our present area. It is possible that this broad flexuring occurred in connection with the intrusion of the peridotites, etc. Certainly it was completed and had been followed by prolonged erosion before deposition of the Cainozoic marine sediments, for the latter rest directly on almost unmetamorphosed or slightly altered Te Anau rocks west of the Livingstone Range (Hutton, 1937), and near the head of the Hollyford River (Hutton and Turner, 1936), but on rocks of the Chl. 4 sub-zone in the inverted sequence at Bob's Cove, Lake Wakatipu (Park, 1909).