模拟降雨下坡面微地形量化及其与产流产沙的关系
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摘要
为揭示坡面微地形对土壤侵蚀过程的响应,该文通过人工模拟降雨试验,结合三维激光扫描仪技术,研究了不同雨强连续降雨条件下黄土坡面微地形变化特征及其与产流产沙的响应关系。结果表明所选取的5个常规地形因子(微坡度、地形起伏度、地表切割度、洼地蓄积量、地表粗糙度)对坡面侵蚀的响应表现出相似的趋势,即随着侵蚀的加剧,地形因子数值逐渐增大;场降雨后,地表粗糙度的增幅最小,分别是3%、8%、17%,对侵蚀的响应最弱,洼地蓄积量的增幅最大,分别增大11.82、18.86、83.33倍,对侵蚀的响应最强;同一雨强下随着连续降雨的进行,产流率稳定,1 mm/min雨强下输沙率基本稳定,1.5与2 mm/min下输沙率不断减小;2 mm/min雨强下输沙率和累积输沙量,远大于其他2个雨强处理;地形因子之间有很强的相关性,但能从不同侧面反映地形的信息,而且都与产流率和累积产沙量之间有较好的线性关系。研究可为进一步揭示黄土区坡面土壤侵蚀机理提供参考。
The micro topography condition reflects surface change and erosion degree, and thus is one of the important factors affecting soil erosion. It is necessary to figure out how the micro topography affects the soil erosion. The objective of this study was to quantify micro topography at loess slope and to demonstrate the relationship between micro topography and soil erosion. In order to achieve the objective, an indoor artificial rainfall experiment was conducted at Key Laboratory of Northwest Water Resources and Environment Ecology of Ministry of Education, Xi'an University of Technology in 2013. Three rain intensity treatments of 1, 1.5, and 2 mm/min. For each treatment, continuous rainfall was carried out for 4 times. During the experiment, runoff volume and sediment yield were measured. 3D point cloud data of the slope before and after rain were collected by Trimber FX 3 D laser scanner. After pretreatment such as denoising, the data were used to calculate index of micro topography. To avoid bias of a single indicator, 5 index were used to quantify micro topography of slope including slope(S), roughness(R), relief amplitude(RA), surface incision(SI), and depression storage(DS). The results showed that the topographic index varied with continuous rainfall. During the continuous rainfall, the slope increased from 5.740° to 8.026°, 8.677°, 9.053°, and 9.153° with rain intensity of 1 mm/min, from 5.506° to 8.317°, 9.300°, 10.908°, and 10.909°with rain intensity of 1.5 mm/min, from 5.857° to 14.306°, 16.546°, 17.196°, and 17.924°with rain intensity of 2 mm/min. After the last rainfall, the SA increased by 3%, 8%, and 17% respectively under rain intensity of 1, 1.5, and 2 mm/min. The DS increased by 11.82, 18.86, and 83.33 times respectively under rain intensity of 1, 1.5, and 2 mm/min. The change of SA was smallest and that of DS was largest among the 5 indexes. Therefore, the response to erosion was smallest for SA but largest for DS; During the four times of rainfall, the runoff rates were 43.509, 45.739, 44.212, 46.702 L/(m2·h) successively with rain intensity of 1 mm/min, 55.226, 60.306, 61.146, 61.399 L/(m2·h) successively with rain intensity of 1.5 mm/min, and 89.134, 106.384, 111.142, 115.869 L/(m2·h) successively with rain intensity of 2 mm/min. The sediment discharge after each of the four rainfall were 0.648, 0.512, 0.615, and 0.688 kg/(m2·h) successively with rain intensity of 1 mm/min, 1.948,1.297,0.946, and 0.576 kg/(m2·h) successively with rain intensity of 1.5 mm/min, 9.491, 7.291, 4.252, and 2.213 kg/(m2·h) successively with rain intensity of 2 mm/min. Runoff rate and sediment discharge with rain intensity 1 mm/min were stable during the continuous rainfall process, and sediment discharge with rain intensity of 1.5 and 2 mm/min decreased until the rainfall continued a certain period of time. After the fourth rain, the accumulative runoff volume were 135.123, 178.558, 307.892 L/m2 respectively with rain intensity of 1, 1.5, and 2 mm/min, and the accumulative sediment discharge were 8.490, 16.502, 73.320 kg/m2 respectively. So the total runoff coefficients are 0.751, 0.659, 0.847 respectively. The sediment discharge and the accumulative sediment discharge with rain intensity of 2 mm/min were far larger than those with other two rainfall intensity. There were high correlations among topographic indicators and parameters of runoff and sediment. Principal components analysis(PCA) revealed one component and the weight of S, R, RA, SI, and DS for the component were 0.997, 0.993, 0.999, 0.999, and 0.987 respectively. It indicated that one component could include all information that the 5 micro topography factors expressed. Even so, these index could describe the topographic information from different aspects. The results can provide valuble information for further studies on the loess area and for clarifying mechanism of slope soil erosion.
The micro topography condition reflects surface change and erosion degree, and thus is one of the important factors affecting soil erosion. It is necessary to figure out how the micro topography affects the soil erosion. The objective of this study was to quantify micro topography at loess slope and to demonstrate the relationship between micro topography and soil erosion. In order to achieve the objective, an indoor artificial rainfall experiment was conducted at Key Laboratory of Northwest Water Resources and Environment Ecology of Ministry of Education, Xi'an University of Technology in 2013. Three rain intensity treatments of 1, 1.5, and 2 mm/min. For each treatment, continuous rainfall was carried out for 4 times. During the experiment, runoff volume and sediment yield were measured. 3D point cloud data of the slope before and after rain were collected by Trimber FX 3 D laser scanner. After pretreatment such as denoising, the data were used to calculate index of micro topography. To avoid bias of a single indicator, 5 index were used to quantify micro topography of slope including slope(S), roughness(R), relief amplitude(RA), surface incision(SI), and depression storage(DS). The results showed that the topographic index varied with continuous rainfall. During the continuous rainfall, the slope increased from 5.740° to 8.026°, 8.677°, 9.053°, and 9.153° with rain intensity of 1 mm/min, from 5.506° to 8.317°, 9.300°, 10.908°, and 10.909°with rain intensity of 1.5 mm/min, from 5.857° to 14.306°, 16.546°, 17.196°, and 17.924°with rain intensity of 2 mm/min. After the last rainfall, the SA increased by 3%, 8%, and 17% respectively under rain intensity of 1, 1.5, and 2 mm/min. The DS increased by 11.82, 18.86, and 83.33 times respectively under rain intensity of 1, 1.5, and 2 mm/min. The change of SA was smallest and that of DS was largest among the 5 indexes. Therefore, the response to erosion was smallest for SA but largest for DS; During the four times of rainfall, the runoff rates were 43.509, 45.739, 44.212, 46.702 L/(m2·h) successively with rain intensity of 1 mm/min, 55.226, 60.306, 61.146, 61.399 L/(m2·h) successively with rain intensity of 1.5 mm/min, and 89.134, 106.384, 111.142, 115.869 L/(m2·h) successively with rain intensity of 2 mm/min. The sediment discharge after each of the four rainfall were 0.648, 0.512, 0.615, and 0.688 kg/(m2·h) successively with rain intensity of 1 mm/min, 1.948,1.297,0.946, and 0.576 kg/(m2·h) successively with rain intensity of 1.5 mm/min, 9.491, 7.291, 4.252, and 2.213 kg/(m2·h) successively with rain intensity of 2 mm/min. Runoff rate and sediment discharge with rain intensity 1 mm/min were stable during the continuous rainfall process, and sediment discharge with rain intensity of 1.5 and 2 mm/min decreased until the rainfall continued a certain period of time. After the fourth rain, the accumulative runoff volume were 135.123, 178.558, 307.892 L/m2 respectively with rain intensity of 1, 1.5, and 2 mm/min, and the accumulative sediment discharge were 8.490, 16.502, 73.320 kg/m2 respectively. So the total runoff coefficients are 0.751, 0.659, 0.847 respectively. The sediment discharge and the accumulative sediment discharge with rain intensity of 2 mm/min were far larger than those with other two rainfall intensity. There were high correlations among topographic indicators and parameters of runoff and sediment. Principal components analysis(PCA) revealed one component and the weight of S, R, RA, SI, and DS for the component were 0.997, 0.993, 0.999, 0.999, and 0.987 respectively. It indicated that one component could include all information that the 5 micro topography factors expressed. Even so, these index could describe the topographic information from different aspects. The results can provide valuble information for further studies on the loess area and for clarifying mechanism of slope soil erosion.
引文
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[2]赵文武,傅伯杰,陈利顶.陕北黄土丘陵沟壑区地形因子与水土流失的相关性分析[J].水土保持学报,2003,17(3):66-69.Zhao Wenwu,Fu Bojie,Chen Liding.Correlations between topographical factors and Soil and water loss in hilly and gully area of Loess Plateau in Northern Shaanxi[J].Journal of Soil and Water Conservation,2003,17(3):66-69.(in Chinese with English abstract)
[3]Sun Wenyi,Shao Quanqin,Liu Jiyuan,et al.Assessing the effects of land use and topography on soil erosion on the Loess Plateau in China[J].Catena,2014,121:151-163.
[4]Darboux F,Davy Ph,Gascuel-Odoux C,et al.Evolution of soil surface roughness and flowpath connectivity in overland flow experiments[J].Catena,2001,46(2/3):125-139.
[5]Darboux F,Huang C.Does soil surface roughness increase or decrease water and particle transfers?[J].Soil Science Society of America Journal,2005,69(3):748-756.
[6]张青峰,王健,赵龙山,等.基于M-DEM黄土人工锄耕坡面微地形特征研究[J].干旱区资源与环境,2012,26(9):149-153.Zhang Qingfeng,Wang Jian,Zhao Longshan,et al.MDEM-based micro-topography characteristics of artificial tillage loess slope[J].Journal of Arid Land Resources and Environment,2012,26(9):149-153.(in Chinese with English abstract)
[7]Torri D,Poesen J,Borselli L,et al.Spatial variation of bed roughness in eroding rills and gullies[J].Catena,2012,90:76-86.
[8]王龙生,蔡强国,蔡崇法,等.黄土坡面发育平稳的细沟流水动力学特性[J].地理科学进展,2014,33(8):1117-1124.Wang Longsheng,Cai Qiangguo,Cai Chongfa,et al.Hydrodynamic characteristics of stable growth-rill flow on loess slopes[J].Progress in Geography,2014,33(8):1117-1124.(in Chinese with English abstract)
[9]邝高明,朱清科,赵磊磊,等.黄土丘陵沟壑区陡坡微地形分布研究[J].干旱区研究,2012,29(6):1083-1088.Kuang Gaoming,Zhu Qingke,Zhao Leilei,et al.Study on distribution of microrelieves on steep slopes in a Loess Hilly-gully Region[J].Arid Zone Research,2012,29(6):1083-1088.(in Chinese with English abstract)
[10]赵龙山,梁心蓝,张青峰,等.裸地雨滴溅蚀对坡面微地形的影响与变化特征[J].农业工程学报,2012,28(19):71-77.Zhao Longshan,Liang Xinlan,Zhang Qingfeng,et al.Variation characteristics and effects of splash erosion on slope micro-relief in bare fields[J].Transactions of the Chinese Society of Agricultural Engineering(Transactions of the CSAE),2012,28(19):71-77.(in Chinese with English abstract)
[11]郑子成,吴发启,何淑勤,等.片蚀与细沟间侵蚀过程中地表微地形的变化[J].土壤学报,2011,48(5):931-937.Zheng Zicheng,Wu Faqi,He Shuqin,et al.Change in surface micro-relief during the course of sheet erosion and inter-rill erosion[J].Acta Pedologica Sinica,2011,48(5):931-937.(in Chinese with English abstract)
[12]Gascuel-Odoux C,Bruneau P,Curmi P.Runoff generation:Assessment of relevant factors by means of soil microtopography and micromorphology analysis[J].Soil Technology,1990,4(3):209-219.
[13]Gómez J A,Nearing M A.Runoff and sediment losses from rough and smooth soil surfaces in a laboratory experiment[J].Catena,2005,59(3):253-266.
[14]Saleh A.Soil roughness measurement:Chain method[J].Journal of Soil and Water Conservation,1993,48(6):527-529.
[15]Jester W,Klik A.Soil surface roughness measurement-methods,applicability,and surface representation[J].Catena,2005,64(2/3):174-192.
[16]Stefan Martin Strohmeier,Sayjro Kossi Nouwakpo,Huang Chihua,et al.Flume experimental evaluation of the effect of rill flow path tortuosity on rill roughness based on the Manning–Strickler equation[J].Catena,2014,118:226-233.
[17]Darboux F,Hang C.An instantaneous-profile laser scanner to measure soil surface microtopography[J].Soil Science Society of American Journal,2003,67(1):92-97.
[18]张利超,杨伟,李朝霞,等.激光微地貌扫描仪测定侵蚀过程中地表糙度[J].农业工程学报,2014,30(22):155-162.Zhang Lichao,Yang Wei,Li Zhaoxia,et al.Quantification of soil surface roughness during soil erosion using laser micro-topographical scanner[J].Transactions of the Chinese Society of Agricultural Engineering(Transactions of the CSAE),2014,30(22):155-162.(in Chinese with English abstract)
[19]李俊利,李斌兵,柳方明,等.利用照片重建技术生成坡面侵蚀沟三维模型[J].农业工程学报,2015,31(1):125-132.Li Junli,Li Binbing,Liu Fangming,et al.Generating 3D model of slope eroded gully based on photo reconstruction technique[J].Transactions of the Chinese Society of Agricultural Engineering(Transactions of the CSAE),2015,31(1):125-132.(in Chinese with English abstract)
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