In the Zoige basin, located in the Eastern Tibet Plateau, several loess- paleosol sequences have formed in different geomorphological locations. However, the spatio- temporal variation of these eolian deposits and their geographical significance to surface processes remain unclear. This paper aims to address these issues by analyzing material obtained from detailed field investigations and experimental data. The results provide direct evidence for accurately understanding the relationship between paleoclimate evolution, sandstorm activity fluctuations, and changes in weathering intensity since the disappearance of ancient Zoige Lake. Extensive and detailed field surveys were conducted in the Zoige basin in the eastern Tibetan Plateau. The Laoqiaoxi (LQX) site, situated on the first river terrace of the Yellow River in the Maqu reach, was selected as the research focus and systematically sampled. Through a comprehensive study of various proxies, such as soil profile structure, magnetic susceptibility, geochemistry, micromorphology, and optically stimulated luminescence (OSL) dating, the following conclusions were obtained: ① Multi- period soils are commonly found in the Zoige basin, with different loess- paleosol sequences developing in various landform locations. The LQX profile has been continuously developing since 3.0 ka, with a stratigraphic sequence from top to bottom (MS0- MS1- L- MS2- L). The variation in aeolian activity intensity primarily influences the continuous soil development. ② Mineral assemblage data, CIA, Rb/Sr ratio, and magnetic susceptibility indicate that the LQX profile exhibits a stage of low weathering intensity. The weathering intensity slightly increases from the loess layer to the soil layer. ③ The relationship between paleoclimate evolution and soil development in the Maqu valley can be summarized as follows: Around 3.0 ka, the regional climate became dry, and the loess (L) layer formed due to intense aeolian sand activities. Approximately 1.5 ka ago, the climate gradually became warmer, with increased precipitation providing favorable hydrothermal conditions for the growth of meadow plants, leading to the formation of the MS2 soil layer. A relatively short period of dry climate around 0. 6 ka interrupted the soil development, resulting in intensified aeolian dust accumulation and the formation of a 30 cm- thick loess layer. Since 0. 3/0. 4 ka, the climate became less arid, and weakened sandstorm activity allowed for the reestablishment of soil development, forming the MS1 and MS0 layers.