ASPEN SPECIAL MAP. 57 
with the doming-up, and probably both have originated in a single cause; 
so that in a general way the amount of uplift as measured is correct. 
The uplifting of the beds along the strike seems to have reached its 
maximum in the north half of the area shown on the Tourtelotte Park 
special map, but its effects are seen to less extent farther south. All the 
rocks between the Roaring Fork and the southern end of the district show 
this remarkable uplifting, accompanied by minor folding and by intense 
faulting; so that the district is entirely different from that adjoiming it along 
the strike to the north. On account of its peculiar deformation this region 
becomes isolated and conspicuous, and its difference from the adjoining 
areas becomes even more important when it is considered that the center 
of greatest uplift and disturbance has also been the chief center of ore 
deposition. 
Parallel with the main axis of this domelike uplift, which is also par- 
allel with the general strike of the beds and with the Castle Creek fault, 
are the axes of minor folds which corrugate the dome. The chief of these 
minor folds is a syncline lying on the eastern side of the uplifted area. 
This syneline, which has been much broken by later faults, many of which 
are important, is most strongly developed just south of Aspen, where it 
occurs in the depression between West Aspen and Kast Aspen mountains. 
It has a general pitch to the north, so that the beds im its center strike east 
and west, while those on its western side have a northwest strike, and on 
its eastern side there is a southwest strike, which approaches and merges 
into the normal strike of the beds throughout the whole district. This 
syncline is continuous up into Tourtelotte Park, but grows constantly 
shallower toward the south, and finally dies out; so that in the southern 
half of the area shown on the Tourtelotte Park special map it can not be 
distinguished. North of Aspen Mountain it also becomes greatly dimin- 
ished in importance, but it can be traced along the eastern side of the 
Castle Creek fault for a considerable distance. In the beds on Red Moun- 
tain, a short distance northeast of Red Butte, there is an easterly dip which 
proves the synclinal structure. This structure, as well as that of the over- 
turned beds to the west of the Castle Creek fault, is shown on Section C of 
the Aspen district map (P!. VII). 
East of this deep, broken syncline on Aspen Mountain the dip of the 
beds flattens, so that on the ridge of Kast Aspen Mountain an approaching 
