found a strip of marine Tertiary sediments thrown down nearly five thousand feet below the adjacent general level of the Fiordland matureland surface (cf. Benson, 1935b). The form of these valleys can be gathered from the above-mentioned illustrations. Beneath the higher shoulders are more or less marked traces of a shoulder about 2500–2000 feet above the present valley floors, perhaps indicating vaguely the base-level attained at the time of formation of the coastal plateau. The northward decrease in height of this shoulder along the Pyke Valley suggested by Plate 2, fig. (a), may have resulted from spur-truncation by the branch of the Hollyford Glacier which moved up the lower Pyke Valley to discharge into the Big Bay depression, and on its retreat left moraines (e.g. at the Knoll), which deflect the northern tributaries of the Pyke from their former direct seaward course, so that they now discharge through Lake Alabaster (Park, 1887, Marshall, 1906). The major tributaries entering this valley from the east, High Falls Creek, Hidden Falls Creek, the Olivine River, and Barrier River, though entering at present at grade, drop over noteworthy falls or high cascades a short distance back from their mouths, possibly the result of headward erosion of streams rejuvenated by uplift during an inter-glacial period followed by step-making during the last glaciation, in which, perhaps, the oversteepening of the lowest (500–300 feet) portion of the valley-sides was effected. No data are available for discussing the relation (if any) of such an uplift with the raised beaches and terraces, 100–300 feet high, that fringe the shore (Hector, 1863, Park, 1887), or the occurrence of uncemented conglomerate noted along the eastern side of the Lake Alabaster and the Pyke Valley (Christie, priv. com.). The branch of the Hollyford Glacier which was deflected by the Skippers Range into Lake McKerrow failed to remove all of the spur over and around which it passed, and has left a strongly glaciated spur-residual. Post-glacial dissection of this and other remnants of spurs have etched out a series of shatter-zones running parallel to the general direction of the valley. (Plate 2, fig. (b).) During the last glaciation the rock-floor of the main valley may have been eroded to a depth below the present sea-level, but has since been partially covered by fluvioglacial deposits forming the present broad and swampy valley-bottom. The Bryneira Range east of this consists chiefly of semi-schistose or phyllitic breccia and tuffs, quartzites and limestones, with almost vertical dip and perhaps a general anticlinal arrangement. It was described by Park (1887) as being “remarkable for the uniformity of its outline and the equality of height exhibited by its higher peaks* Probably this is all that was intended by his later (1921) reference to the “flat-topped” character of the Bryneira Range. many of which are over 6000 feet high. The effect of glaciation seems to be remarkably vivid. It consists on its western side of a number of square-shouldered spurs separated by narrow ravines. The spurs terminate abruptly, presenting steep faces to the Pyke Valley. They are mostly devoid of vegetation, and consist of great