WICHITA AND ANCESTRAL ROCKIES SYSTEMS AND THE TEXAS FORELAND 



241 



Cp Pontotoc for. (Permian) 



Ch Hoxbor group (Missouri •* Virgil) 



Cd Dcese group ( Des Moines) 



Cdh Dornick Hills group (U. Morrows Lamp.) 



CS Springer group ( L. Morrow) 



|>|w Woodford (Mississippion) 



Mc Coney shale (Mississippion) 



Osh Sylvan and hunton' 



Ov Viola limestone JOrdovician 



03 Simpson group 



OCo Arbuckle limestone (Ord i-Comh) 



Cr Reagon sandstone (Cambnon) 



p-G Pre -Cambrian crystallines 



/ w w w \7 w 



Fig. 15.6. Cross sections through the Ardmore basin, Arbuckle Mountains, and Hunton arch, compiled 

 from Dott (1934), Tomlinson (1929), and Moore ei al. (1944). 



a large, complex anticline. In the core of the anticline, two prominent 

 peaks of Precambrian porphyry ( the Timbered Hills) rise 700 feet above 

 the valley of the Washita River and 1400 feet above sea level. Geologically 

 the term Arbuckle Mountians applies also to the hilly area to the north 

 and east in which lower Paleozoic rocks crop out and where structural 

 features of mountain proportions are located. A thick sequence of rocks 

 from Precambrian to Late Pennsylvanian is exposed in the range. See 

 cross sections, Fig. 15.6. 



The regional structure of the Arbuckle Mountains is a series of much- 

 faulted subparallel folds trending northwest and southeast. They are 

 shown on the map of Fig. 14.2, where it will be seen from north to south 



the several divisions are as follows; Lawrence uplift, Franks graben, 

 Hunton anticline, Mill Creek syncline, and Tishomingo anticline. On 

 Fig. 15.4 the Hunton anticline, Franks graben, and Lawrence uplift are 

 combined under the general term, Hunton arch. The Arbuckle anticline 

 is next south of the Tishomingo anticline but offset to the west. The 

 Washita syncline and fault zone separate the Tishomingo anticline from 

 the Arbuckle anticline. The structures are compressional in nature, and 

 especially in the Arbuckle anticline and south-lving Ardmore basin 

 thrust faults and tight folds are pictured by Dott ( 1934 ) and confirmed 

 by Swesnik and Green (1950). The overriding is northward. Study 

 sections in Fig. 15.6. 



