342 Transactions. 



basal layer of tlio conglomerate as a bed 2 in. tliiok of conglomerate 

 formed of small rounded pebbles of greywacke. " Next follows 2 ft. 6 in. 

 of bedded sandstone, covered ))y 1 ft. of mudstone, and that again is 

 followed by many feet of fairly coarse conglomerate interbedded with 

 sandstone ajul mudstone bands 1 ft. to 3 ft. in thickness, and with bands 

 of very coarse conglomerate."' Tlie l>oulders in the conglomerate ])ands 

 are of varied sizes, about one-third being over 6 in. in diameter, and blocks 

 of to 2 ft. in diameter being common. Still larger blocks occur, but are 

 rare. Small pebbles of greywacke are very abundant tlironghout, and are 

 smooth and well-rounded. '' There is in addition a large proi)ortion of 

 fine, sandy material filling the interstices, and the conglomerate is cemented 

 into a very hard rock." The rocks represented are — pre-Notocene grey- 

 wacke and jasperoid pebbles, forming the bulk of the finer material ; sand- 

 stone blocks of all sizes, probably mostly Clarentian ; small boulders of 

 basalts resembling those of the Clarentian of Herring River and ilouat's 

 Lookout in the Awatere Valley ; Amuri limestone, not very abundant, 

 in bhx'ks n]i to 6 in. in diameter, but rarely larger ; water-worn blocks of 

 fine Tertiarv sandstone, crow^ded with shells, and resembling in appearance 

 and fossil-content the supposedly derived boulders in tlie underlying '"grey 

 marls." 



Dee Gorge (Plate XXIX, fig. 2). — The lower part of the conglomerate is 

 very well bedded by thin sandstone bands. The material is genei'ally similar 

 to that in the Mead, and the presence of Clarentian rocks is proved b}' 

 the presence of blocks of sandstone containing fragments of Inoceramus. 

 A verv large block of flint-beds was observed near the base on the north 

 side, but in general the size of the boulders, as xn the Mead, is smaller 

 than in the exposures of the Kekerangu area. For further details Cotton's 

 description should be consulted. 



Upper Swale aiul Ure Rivet-^.- There are several se})arated outcrops 

 of the conglomerate in the uj^per Swale Valley, presumably owing to its 

 repetition of folds or faults, but their relations are unknown except in 

 the case of the most easterly, which McKay examined and found resting 

 on the " grey marls.*' Mr. A. Tomlinson, of Awapiri, Awatere Valley, 

 informs me that these conglomerates are reddish in colour and form three 

 sharp ridges known as the Razorbacks. In the upper Ure, as seen from 

 the summit of the Challc Tlange, there is a main outcrop of conglomerate 

 running from behind the Whaleback across the river and terminating 

 opposite Whitewash Creek. This outcrop evidently occupies the core of 

 the overturned syncline. Two smaller outcrops are seen on tlie w^atershed 

 between the Ure and the Swale, dipping towards Limestone Hill Avhich 

 is formed bv the Amuri limestone of the upper limb of the syncline. 



Dail River. — McKa\' describes the conglomerate as resting on the '' grey 

 marls." The series is 500 ft. thick, and dips .r^O'' to 60°"^ to the ncrrtli- 

 west. The lower beds are coarser tJian the middle and upper parts. In 

 the middle beds there are gritty sandstones \vilh broken shells and black 

 shales with abundant plant-remains forming coaly streaks. The upper 

 part, which is well stratified near the top, is mainly formed of modei-ate- 

 sized pebbles, with beds of ])lark sliale. 



Muzzle River. — McKay describes the beds as of about the same thick- 

 ness as in the Dart and the Dee. In the west branch they are standing 

 vertical and rest against the fault. In the eastern branch they form a 

 syncline resting on the '' grey marls," and the junction along the fault 

 is obscured. Fossiliferous blocks of Tertiary rocks and concretions and 

 fossiliferous blocks from the Clarentian are abundant in both sections. 



