坡沟系统是黄土丘陵沟壑区产沙的主要源地，深入理解其侵蚀产沙过程与机理对区域土壤侵蚀防治和过程模型构建具有重要意义。已有研究主要基于室内试验和回填土开展，鲜有研究开展自然坡沟系统侵蚀产沙过程精细化研究，尤其对地形变化—侵蚀产沙过程的交互作用及其机理认识不足。地面三维激光扫描技术（Terrestrial laser scanning，TLS）可快速、高效、无接触的监测地形变化，成为土壤侵蚀过程精细研究的有力工具，并已被应用于沟谷坡侵蚀产沙监测。然而，其对自然梁峁坡侵蚀的监测精度尚不清晰。鉴于此，本文以黄土丘陵沟壑区自然坡沟系统为研究对象，首先于两个梁峁坡径流小区各开展14场模拟放水冲刷试验，利用TLS扫描地形变化计算产沙量，并以实测产沙量评估计算结果，验证TLS在自然梁峁坡侵蚀监测精度。进而，开展五种放水流量（85 L min^-1、70 L min^-1、55 L min^-1、40 L min^-1、25 L min^-1）自然坡沟系统小区冲刷试验，基于试验前后TLS地形扫描结果，分析侵蚀产沙时空过程。最后，基于试验径流参数计算五种流量下的雷诺数、弗劳德数、Darcy-Weisbach阻力系数、Manning糙率系数、径流剪切力、径流功率、单位径流功率、过水断面单位能量等水动力学参数，根据地形扫描结果计算坡沟系统试验前后的地形粗糙度、高斯曲率、平均曲率等参数，分析不同流量下地形变化—水动力学参数—侵蚀产沙的关系，揭示地形变化与侵蚀产沙的关系及其机制。主要研究结果如下：

（1）TLS监测精度方面。基于TLS的梁峁坡累计计算产沙量精度明显高于基于TLS的单场次计算产沙量。当像元尺寸大于等于5 mm时，计算产沙量结果趋于稳定，像元尺寸不再对体积变化计算产生明显影响。其中，基于5 mm计算结果最精确。当选用5 mm像元计算体积变化时，两个梁峁坡径流小区单场次计算产沙量的绝对误差大小为1.67 kg（0.56 kg—4.76 kg），1.73 kg（0.28 kg—3.81 kg），相对误差为784.12 %（80.21 %—4705.44 %），466.21 %（153.15 %—1180.65 %），计算产沙量和实测产沙量之间的线性拟合R²分别为0.11（p = 0.245），0.47（p = 0.006）。累计计算产沙量的绝对误差大小为0.87 kg（0.004 kg—1.79 kg），1.26 kg（0.12 kg—2.78 kg），相对误差为25.02 %（0.06 %—124.49 %），56.82 %（2.34 %—180.06 %），计算产沙量和实测产沙量之间的线性拟合R²分别为0.61（p < 0.001），0.82（p < 0.001）。表明TLS更适用于监测梁峁坡连续侵蚀过程。

（2）侵蚀时空过程方面。不同流量下的梁峁坡侵蚀时空过程中，侵蚀均主要集中在坡面中上部，沉积主要集中在坡面下部。在较大流量（85 L min^-1、70 L min^-1、55 L min^-1）下的五场试验后，梁峁坡侵蚀沉积已经逐渐稳定，不再产生大范围的分布变化。在较小流量（40 L min^-1、25 L min^-1）下的五场试验后，梁峁坡侵蚀、沉积、无变化区域的分布依然存在大范围的明显变化。研究还发现紧邻沟缘线周围都是侵蚀区域，沟缘线后退越活跃的位置，其周围侵蚀强度越大。在沟谷坡侵蚀过程中，不同流量下沉积都主要集中于坡底区域，较强侵蚀区域都位于沟缘线后退位置的下方，但较强侵蚀、较弱侵蚀、无变化区域分布存在差异。

（3）侵蚀机理研究方面。不同流量下的地形起伏度随时间呈对数曲线增大，且放水流量越大，数值越高。在85 L min^-1、55 L min^-1流量下，地形起伏度的增大对侵蚀产沙有着抑制作用（R²在0.54—0.99，p < 0.001至p = 0.155），在其余流量下二者关系不明确。不同流量下的梁峁坡水动力学与侵蚀产沙之间未发现统一明确的关系（R²在0.001—0.94之间，p = 0.007至p = 0.990）。在较大流量（85 L min^-1、70 L min^-1、55 L min^-1）下，梁峁坡径流功率随地形起伏度增大而增大（R²在0.62—0.97之间，p = 0.002至p = 0.112），沟谷坡Darcy-Weisbach阻力系数、Manning糙率系数、径流剪切力、径流功率四种参数与坡沟系统产沙之间正相关（R²在0.45—0.99，p < 0.001至p = 0.213）。在85 L min^-1、55 L min^-1、40 L min^-1、25 L min^-1流量下，沟谷坡Darcy-Weisbach阻力系数和径流剪切力都因地形粗糙程度的增大而减小（R²在0.63—0.99， p < 0.001至p = 0.111）。综上结果表明，径流侵蚀导致的地形变化会反向抑制径流侵蚀作用，削弱坡沟系统产沙能力。地形起伏变化应当作为区域水土保持措施优化和侵蚀模型开发中的重要因素。

The slope-gully system provide the major source of sediment yield in the hilly and gully loess plateau, and an in-depth understanding of erosion process and mechanism is of great significance for regional soil erosion control and process-based erosion model development. Previous erosion process studies were undertaken mainly based on indoor experiments and backfill soil, but few studies have been conducted to study the erosion process of natural slope-gully system, and in particular the interaction between topographic changes and erosion process and its underlying mechanism were not well understood. Terrestrial Laser Scanning (TLS), which is able to monitor topographic changes efficiently in a non-invasive manner, has become a powerful tool for a high-resolution study of soil erosion processes and has already often been applied to monitor gully erosion processes. However, its accuracy of hillslope erosion monitoring was still unclear. In view of these, this study investigated the processes and mechanisms of slope-gully systems through runoff scouring experiments and teresstiral laser scanning conducted on erosion plots established on a natural sope of a typical small catchment (i.g. Xindiangou catchment) in the hilly and gully loess plateau. Firstly, fourteen runoff scouring experiments were conducted on two plots. The sediment yield was calculated based on topographic changes achieved by TLS, and the measured sediment yield was used to verify the accuracy of TLS-derived results. Five runoff scouring experiments were undertaken on each of five plots with different inflow discharges (85 L min^-1, 70 L min^-1, 55 L min^-1, 40 L min^-1, 25 L min^-1) and TLS was employed to investigate the spatiotemporal patterns of erosion based on the terrain information achieved by the TLS before and after each of the experiments. Finally, the hydrodynamic parameters such as reynolds number, froude number, Darcy-Weisbach friction coefficient, Manning roughness coefficient, shear stress, runoff power, unit runoff power, and unit energy of water-carrying section were derived based on the runoff relevant parameters measured during the experiments. Pre-experiment and post-experiment roughness, gaussian curvature, and mean curvature of the slope-gully system were also calculated based on the achieved high-resolution terrain information. The interaction among terrain change, hydrodynamic parameters and sediment yield under different runoff discharges was also studied. The main findings are as follows.

(1) The results demonstrated that the accuracy of the TLS-derived cumulative sediment yield from hillslope of the two plots was apparently higher than that of TLS-derived consecutive sediment yield. When the cell size is greater than or equal to 5 mm, the results of calculated sediment yield tend to be stable, and the cell size no longer has a significant effect on the calculation of volume change. Among them, the results based on 5 mm are the most accurate. When a 5 mm grid-cell size was chosen to calculate the volume change, the magnitude of absolute error for the calculated consecutive sediment yield was 1.67 kg (0.56 kg—4.76 kg) and 1.73 kg (0.28 kg—3.81 kg), the magnitude of relative error for the calculated consecutive sediment yield from hillslopes of the two plots was 784.12 % (80.21 %—4705.44 %) and 466.21 % (153.15 %—1180.65 %), and the R² of the linear relationships between the calculated and measured consecutive sediment yield were 0.11 (p = 0.245) and 0.47 (p = 0.006), respectively. The magnitude of absolute error for the calculated cumulative sediment yield was 0.87 kg (0.004 kg—1.79 kg) and 1.26 kg (0.12 kg—2.78 kg), the magnitude of relative error for the calculated cumulative sediment yield from hillslopes of the two plots was 25.02 % (0.06 %—124.49 %) and 56.82 % (2.34%—180.06 %), and the R² of the linear relationships between the calculated and measured cumulative sediment yield were 0.61 (p < 0.001) and 0.82 (p < 0.001), respectively. This demonstrated that TLS was more suited to monitor hillslope erosion over a relative long time period rather than individual rainfall events.

(2) With regard to the spatiotemporal process of hillslope erosion under different flow discharge, the erosion was mainly concentrated in the middle and upper part of the slope, and the deposition was mainly concentrated in the lower part of the slope. After five scouring experiments under large flow charges (85 L min^-1, 70 L min^-1, 55 L min^-1), the spatial distribution of erosion and deposition on the hillslope gradually stabilized. After five field experiments under small flow (40 L min^-1, 25 L min^-1), the distribution of erosion, deposition and unchanged area of hillslope still changed considerably. It is also found that there were erosion areas near the gully shoulder line. The more active the retreat of the gully shoulder line, the more eroded area around it. In the process of gully slope erosion, the deposition under different flows were mainly concentrated in the slope bottom area, and the intensive erosion areas were located below the retreat position of the gully shoulder line, but the distribution of intensive erosion, weak erosion and unchanged areas was different.

(3) The topographic relief at different runoff discharges increased logarithmically throughout time, and topographic relief was also higher for plots with higher input flow. At 85 L min^-1 and 55 L min^-1 runoff discharges, the increase in topographic relief decreased erosion (R² =0.54—0.99, p < 0.001—0.155), and the relationship between them was not clear for other runoff discharges. No strong and significantrelationships were found between the hydrodynamics and erosion on the hillslopes at different runoff discharges (R² = 0.001—0.94, p = 0.007—0.990). At higher runoff discharges, the relationship between topographic variation and runoff power of the hillslopes was more significant (R² = 0.62—0.97, p = 0.002—0.112), and the Darcy-Weisbach friction coefficient, Manning roughness coefficient, shear stress and runoff power of gullyslope had positive correlations with the sediment yield of slope-gully system  (R² = 0.45—0.99, p <0.001—0.213). At 85 L min^-1, 55 L min^-1, 40 L min^-1, and 25 L min^-1 runoff discharges, the Darcy-Weisbach fricion coefficient and shear stress of gullyslope decreased with increasing terrain roughness (R² = 0.63—0.99, p < 0.001—0.111). In summary, the results indicated that topographic changes due to runoff erosion could inversely inhibit the subsequent erosion and lowered the sediment yield from slope-gully systems. Topographic relief changes should be used as a indicator in the optimization of regional soil and water conservation measures and erosion model development.

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