Comprehensive research on the structure attributions, the primary basin features, the combination of lithology and lithofacies, provenance analysis, and the distinction of thickness distribution of the Ordos Basin in the Mesozoic, suggests that the depocenters of the basin transferred contraclockwise from southeast to north, then to southwest from middle Late Triassic to Early Cretaceous. There was no a unified or lagerscale accumulation center present at the west of the basin before Early Cretaceous, but only small, isolated accumulated centers occurred. The reason why thicker strata appear to the west of the basin in multistages is that these areas were much close to the west boundary of the primary basin, where abundant water source offered huge power. Therefore it stands for the local accumulation centers. Till Early Cretaceous, the depocenters, the accumulation and subsidence centers were superposed as an entity in the southwest of the basin. It was not until the Middle Jurassic that the extant residual basin in the west of the Yellow River took a paleogeographic structural pattern of high in the west and low in the east. The depocenters of the Ordos Basin remained and were superposed consistently from middle Late Triassic to middle Jurassic. The higher thermal maturation of Mesozoic and Paleozoic strata in the depocenters and its neighborhood indicate an active effect at depth in these areas. Comprehensive research suggests that superposition of depocenters in several periods and its consistence with higher thermal maturation centers, reflect that the basin is controlled generally by subsidence centers. Therefore, the depocenters may represent the centers of subsidence. Most of the subsidence or depocenter centers within the largescale Ordos craton during Mesozoic were distributed in the south of the Ordos Basin, and are closely associated with flexing and subsiding of the foreland, resulted from strong converged orogenic activity, which took place at the same time as the Qinling Orogenic belt.