575 



from the lower slopes of the mount, easterly, to the public 

 road, a distance of about a mile, and having a fall of about 

 100 feet. A number of springs, in lineal order, follow the 

 base of the mount, and probably indicate the junction 

 between the quartzite and the sunken purple-slates of the 

 plain. 



The fault which defines the south-eastern side of the 

 mount divides the mount proper from the foot hills, and at 

 its southern end is cut by the transverse fault that truncates 

 the south end of the mount. The great scarp of the Cathe- 

 dral Rock, 300 feet in height (made in two sections), as well 

 as other prominent scarp faces of quartzite, probably repre- 

 sents the line of fracture. The Cathedral-rock Creek also 

 marks the line of a transverse fault, which is evident from the 

 discontinuity of the beds on either side of it. 



The two principal faults just described, together with 

 the plains on the eastern side of the mount, mark off a 

 triangular area of foot hills that include features of great 

 geological interest. The stratigraphical succession of the beds 

 within this area has already been described. They are identi- 

 cal with those met with on the western and northern side of 

 the mount, but the tectonic phenomena seen in this segment 

 are unique. The main limestone is but little disturbed, and 

 follows a definite strike (although interrupted at the 

 Mount Creek) till cut off by the transverse fault, but 

 all the beds between it and the quartzite of the mount 

 (belonging to the siliceous limestones and ribbon-slate series) 

 have been subjected, not simply to distortion, but disruption 

 to an extreme degree. 



The belt of rocks adjacent to the base of the mount, and 

 in places far up the side, is composed of crushed and 

 triturated rock that has become recemented in irregular 

 masses that are now quite destitute of bedding planes. An 

 outcrop of this kind, consisting of mashed material in large 

 dark-coloured rock masses, at a height of 600 feet from the 

 base, can be easily recognized from the township of Melrose, 

 and is known locally as the "Cat Rocks." (See pi. liv., fig. 2.) 



The zone of crush-rock includes the two inner ridges of 

 the foot hills (opposite Melrose), while set in the mass of 

 mashed material are larger dissociated fragments of the 

 original rocks outcropping at various angles, but still retain- 

 ing to some extent their natural bedding planes. These are 

 no doubt fragments that have been torn from the parent mass 

 by the earth-creep, and are now mixed up indiscriminately 

 with the more brecciated portions, which accounts for the 

 incongruities that occur in their respective strike and dip. 



