TOURTELOTTE PARK SPECIAL MAP. 8&5 
whole extent of the Tourtelotte Park special area, becomes in its turn a 
gentle monocline, dipping into the Castle Creek fault, and in the southern- 
most part of the area the remnant of this anticline is united with the 
easternmost syncline to form a single simple monoclinal structure. 
Within this district, bounded on the west by the Castle Creek fault 
and on the east by the granite, there is an excessively complicated system 
of faulting. The faults may be separated imto various distinct systems, 
but all have apparently an interdependence. A very conspicuous system 
runs nearly parallel to the Castle Creek fault and to the contact of granite 
and sedimentaries, and therefore nearly parallel to the longest axis of the 
wedge-shaped area included between these two boundaries. Another, 
weaker, but not less conspicuous, system runs at right angles to the first, 
parallel to the shortest axis of the area. Wherever these faults intersect 
the Castle Creek fault, as is often the case with the east-west system, they 
usually seem to disappear. Occasionally, however, an east-west fault 
seems to displace the Castle Creek fault, thus showing its later age; but 
even in this case the cross-cutting fault probably disappears a_ short 
distance away from the Castle Creek fault to the west. 
On the western side of the main Castle Creek break there is no 
evidence of any such complicated system of intersecting faults as is found 
on the east. There is, however, a system of faults which are nearly par- 
allel with the main Castle Creek break and which are evidently dependent 
upon it; but these faults are quite distinct in nature from the Tourtelotte Park 
types. In the great mass of Maroon and Triassic sandstones immediately 
west of the Castle Creek fault, and also in the Weber shales and limestones 
which occur on the west side of the fault im the southern part of the Tour- 
telotte Park special area, it is hard to distinguish slight faulting, owing to 
the similarity in lithological composition of the beds through great thick- 
nesses; but from all the data that can be obtained it seems that the 
Tourtelotte Park type of faults is either absent in these beds or has become 
so unimportant as not to be easily recognized. 
On the eastern side of the Tourtelotte Park special area the contact 
of the granite with the overlying beds constitutes an effectual barrier to 
further investigation of structure. It is probable that many of the faults 
are continuous into the granite for indefinite distances, for the faulting 
D 
along the contact of granite and Cambrian quartzite is often very strong 
