. Bulletins of American paleontology. Conglomerate Siltstone/ Sandstone Bedded chert Shale Text-figure 2.—Generalized stratigraphy of Paleozoic Ouachita Front rocks exposed in the Marathon uplift. The pre-orogenic se- quence was deposited along a rifted passive margin, whereas the flysch sequence was deposited syn-orogenically during the Ouachita orogeny. of terrigenous clastic debris, in particular, the source for the Tesnus and lower Raymond, came from the southeast (McBride, 1966; Cotera, 1969). Some of the clastic input during the syn-orogenic stage, however, did come from the north and no
. Bulletins of American paleontology. Conglomerate Siltstone/ Sandstone Bedded chert Shale Text-figure 2.—Generalized stratigraphy of Paleozoic Ouachita Front rocks exposed in the Marathon uplift. The pre-orogenic se- quence was deposited along a rifted passive margin, whereas the flysch sequence was deposited syn-orogenically during the Ouachita orogeny. of terrigenous clastic debris, in particular, the source for the Tesnus and lower Raymond, came from the southeast (McBride, 1966; Cotera, 1969). Some of the clastic input during the syn-orogenic stage, however, did come from the north and northwest. A northern 103 15 EASTERN DOMAIN. 30 00 Text-figure 3. —Locality map showing outcrop pattern of the Ca- ballos Novaculite in gray, modified from King (1937). Heavy gray doited line separates structural domains of Muehlberger (1978). Measured sections: PH = Payne Hills, PH2 = Payne Hills II. SS = Sulphur Springs, MC = Monument Creek, MA = McKnight, EB = East Bourland, WH = Wood Hollow. See Appendix for the precise location of each section. source is proposed for the Dimple Limestone, a cal- carentite sandwiched in between the Tesnus and Ray- mond formations (Thomson and Thomasson, 1969), and olistostromal blocks that occur in the base of the Tesnus Formation in the western basin margin can be traced to North America (McBride, 1978). The size of the Tesnus olistoliths also indicates that the basin had to be in close proximity to continental North America to allow for their transport. The rocks exposed in the Marathon uplift have been folded and thrusted into a series of anticlinoria- syn- clinoria and imbricate stacks of thrust sheets trending NE and showing transport to the NW (King, 1937; Flawn et al., 1961). The structural grain is well illus- trated by the outcrop pattern of the Caballos Novac- ulite (Text-figure 3). Three structural domains are rec- ognized in the uplift based on the deformational style and the rheology of the rocks exposed (Muehlberger. 1978; M
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