Peripheral foreland basins, an elongated trough between linear contractional orogenic belts and stable cratons, are developed due to downward flexural subsidence of the cratonic lithosphere driven by thrustsheet loading of the overriding mountain range (DeCelles, 2012;DeCelles & Giles, 1996;Lyon-Caen & Molnar, 1985). The difference in thrust loading across the fold-thrust belt results in the spatial and temporal variation of sedimentation within the foreland basins (DeCelles & Giles, 1996;Flemings & Jordan, 1989;Kumar et al., 2003a;Waschbusch & Royden, 2007). During the initial underfilled stage, sediments from marine and deltaic settings are commonly deposited in the foreland basins. Eventually, in the overfilled stage, the marine deposits are replaced by the fluvial-dominating environments with sediments sourced