The Taklimakan Desert in Northwest China is the major source of dust storms in China. The northeast edge of this desert is a typical arid area which houses a fragile oasis eco-environment. Frequent dust storms cause harmful effects on the oasis ecosystem and negative impacts on agriculture, transportation, and human health. In this study, the major source region, transport pathway, and the potential contribution of dust storms to particulate air pollution were identified by using both trajectory analysis and monitoring data. To assess the source regions of dust storms, 48 h backward trajectories of air masses arriving at the Bugur (Luntai) County, which is located at the northeast edge of Taklimakan Desert, China on the dusty season (spring) and non-dusty month (August, representing non-dusty season) in the period of 1999–2013, were determined using Hybrid Single Particle Lagrangian Integrated Trajectory model version 4 (HYSPLIT 4). The trajectories were categorized by k-means clustering into 5 clusters (1a–5a) in the dusty season and 2 clusters (1b and 2b) in the non-dusty season, which show distinct features in terms of the trajectory origins and the entry direction to the site. Daily levels of three air pollutants measured at a station located in Bugur County were analyzed by using Potential Source Contribution Function (PSCF) for each air mass cluster in dusty season. The results showed that TSP is the major pollutant, with an average concentration of 612 µg/m3, as compared to SO2 (23 µg/m3) and NO2 (32 µg/m3) in the dusty season. All pollutants were increased with the dust weather intensity, i.e., from suspended dust to dust storms. High levels of SO2 and NO2 were mostly associated with cluster 1a and cluster 5a which had trajectories passing over the anthropogenic source regions, while high TSP was mainly observed in cluster 4a, which has a longer pathway over the shifting sand desert area. Thus, on strong dust storm days, not only higher TSP but also higher SO2 and NO2 levels were observed as compared to normal days. The results of this study could be useful to forecast the potential occurrence of dust storms based on meteorological data. Research focusing on this dust-storm-prone region will help to understand the possible causes for the changes in the dust storm frequency and intensity, which can provide the basis for mitigation of the negative effects on human health and the environment.

In this paper, the sediment grain size, organic matter C/N ratio, and isotope δ 13 C of the ancient Milan River channel, Northwest China are used as indicators, and their responses to paleoclimatic changes since the Holocene were analyzed. The results show that the dominant grain size of the surface sediments of the ancient Milan River channel is silt, and the soil particle size is smaller than that of the floodplain, indicating that the hydrodynamics were weak in the late paleochannel. The surface sediments of the paleochannel contain a wind created layer of sand, indicating that the sedimentary environment was affected by a two-phase function of wind and water. The C/N ratio of the sediments varies from 5 to 19.6 with an average value of 12.3. The δ 13 C values range from -27.383‰ to 21.58‰, indicating that the organic matter in the sediment was dominated by river organic matter but mixed with some terrestrial organic matter. The dates of the Optically Stimulated Luminescence (OSL) and the variation in the measured values of each element in the vertical section indicate that since 5000 aBP, the paleoclimate in the study area has experienced six stages of evolution. In stage I, 5000-4500 aBP, the climate was mainly warm and dry. During this period, the climate environment fluctuated frequently, and the cold and warm periods alternated. During stage II, 4500-3900 aBP, the climate gradually decreased and then rebounded slightly. The overall climate was cold and humid, and the water volume increased significantly during this period. During stage III, 3900-2800 aBP, the climate experienced a large temperature increase and cooling, and a warm front appeared around 3000 aBP, indicating typical warm and dry climate characteristics during this period. In stage IV, 2800-1800 aBP, the temperature continued to decrease, and the climate became cold and humid, which was conducive to the growth of crops. In stage V, the first half of the period from 1800 to 1000 aBP was relatively warm and dry, and the temperature dropped briefly causing a cold period. In stage VI, 1000 aBP to present, the temperature experienced a small fluctuation, the climate became dry and