An Overview

(550- m (4) pre-Gilmer salt diapirs (Oakwood and, Saline); and (5) post-Gilmer salt diapirs in the basin center. This inward increase in shape maturity results from increasing salt thickness and distribution of post-Louarm sedimentary fades. The Louann Salt (Middle Jurassic) was deposited in a broad continental basin on a post-rift unconformity surface. Domain 1 suggests that a critical salt thickness (~500 m) was necessary to initiate flow. In the Late Jurassic, an aggrading carbonate wedge uniformly loaded the underlying salt and formed the salt pillows of domain 2. Salt flow in the basin center had not begun by Gilmer time, probably due to a thiimer overburden of basinal car bonate fades there. The Uppa Jurassic-Lower Cretaceous Schuler-Hosston regressive terrigenous elastics prograded rapidly across the carbonate platform as coalesdng fan deltas, filling the central basin. Salt anticlines of domain 3 grew by serial amplifica tion of pre-Gilmer pillows to form ridges normal to dip direction fronting depocenters. Salt diapirs subsequently evolved from the distal anticlines. Salt anticlines 80% of petrolexmi from the west-center of the pre-Gilmer source rocks, ly initiation of folding, the large size of the anticlines have contributed to petroleum accumulation.