## 8 Selectivity of the Aeolian Process  
Similar to hydric erosion, gaseous emissions are also affected at different stages of wind erosion (Table 2). Lighter fractions (SOC, clay, and fine silt) are also selectivity removed in wind-blown dust. Towards an attempt to understand the magnitude and mechanism of SOC-ER in dust, using Big Spring Number Eight (BSNE) wind-vane samplers across five land types in rangelands of Western Queensland, Australia, [PERSON] et al. [57] observed that sandy soils and finer particulate quartz-rich soils are more efficient at SOC emission and have larger SOC-ER in dust than that in clay-rich aggregated soils. The SOC-ER of dust originating from sand-rich soil ranged from 2-41. [PERSON] et al. [57] observed that two dust samples from regional transport events contained 15-20% SOC. In addition to texture, wind speed also affects SOC-ER. Using a wind tunnel on a manured sandy soil, [PERSON] et al. [58] observed that wind erosion caused a preferred release of manure particles at wind speeds close to the threshold of 7 m/s, with the greatest sorting effects in size, shape, and density the of particles. [PERSON] and colleagues concluded that wind erosion immediately leads to the loss of added organic material. At higher wind speeds, [PERSON] et al. observed that the sediment composition corresponds to the entire soil or soil-manure mixture. Depending on the wind speed and the magnitude of erosion, the loss of manure ranged from 1.7-14% of the fertilization rate. Wind velocity interacts closely with the local topography, as a factor affecting sediment transport by wind erosion. Based on studies involving simulation or dust transport from a mine tailing using a computational fluid dynamics model, [PERSON] et al. [59] observed that local topography and wind velocity profiles are the major factors that influence deposition. In a study involving sandy dunes in Southeastern Niger, [PERSON] et al. [60] observed that saltation flux on the bare mobile dune was 2-40 times higher than that observed from cultivated fields and rangelands. [PERSON] and colleagues measured the annual fluxes on the dune to be from 2000 to 6000 kg/m\({}^{2}\), due to the variability of the wind from year to year. Soil temperature is also among the major factors controlling desert soil CO\({}_{2}\) flux [61]. In the Horqin Sandy Land, northeastern China, [PERSON] et al. [63] observed that soil temperature at a depth of 20 cm was significantly correlated with soil respiration. The autotrophic respiration (R\({}_{2}\)) was more sensitive to soil temperature than the heterotrophic respiration \begin{table}
\begin{tabular}{l l l l} \hline \multicolumn{1}{c}{**Stage**} & \multicolumn{1}{c}{**Processes**} & \multicolumn{1}{c}{**References**} \\ \hline I. Detachment & Sandy and particulate quartz-rich soil, local & \(\bullet\) & [PERSON] et al. [57] \\  & topography, wind velocity. & \(\bullet\) & [PERSON] et al. [58] \\  & & \(\bullet\) & [PERSON] et al. [59] \\  & & \(\bullet\) & [PERSON] et al. [60] [PERSON] et al. [56] \\ \hline II. Saltation & Mobile sand dunes, vegetation cover, soil temperature. & \(\bullet\) & [PERSON] et al. [61] \\ \hline III–V. Deposition, Deep Burial, and Re-Aggregation & Buried SOC; climate change, anthropogenic & \(\bullet\) & [PERSON] et al. [62] \\  & perturbations, fallow phase of the rotation cycle. & \(\bullet\) & [PERSON] and [PERSON] [54] \\ \hline \end{tabular}
\end{table} 
Table 2: Gaseous emissions at different stages of aeolian erosion processes. (R\({}_{\rm h}\)), and the temperature-sensitivity coefficients (Q\({}_{\rm 10}\)) were 3.39, 2.52, and 2.79 for R\({}_{\rm a}\), R\({}_{\rm h}\), and R\({}_{\rm t}\), respectively. Vegetation cover plays an important role in wind erosion and loss of SOC by dust-blown sediments. In a desert grassland of southern New Mexico, USA, [PERSON] et al. [56] observed that wind erosion rates and loss by dust emissions (nutrients including C) are strongly affected by plant cover.