溶质示踪测量径流流速方法及其在融水侵蚀中的应用研究
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摘要
坡面径流流速是表征坡面水蚀动力特性的重要参数,与径流的剥蚀和输运能力直接相关。坡面薄层水流流速的测量对土壤侵蚀研究与应用方程重要。
本研究根据电解质脉冲边界模型测量的流速随距离增长的关系,提出了电解质脉冲边界模型测量最小距离优选方法。流速越大,电解质脉冲边界模型测量流速需要的测量距离越大。当设置土壤坡度为5°、10°、15°,流量为12、24、48L/mmin时,模拟未冻土壤表面误差限为5%、10%时分别需要2.5m、2.0m的测量距离。
在室内不同坡度(5°、10°、150)和流量(12、24、48L/mmin)条件下,用电解质脉冲边界模型以及染色剂示踪法进行冻土坡面、冰坡面径流流速测量的对比研究。结果表明,冻土坡面径流流速随坡度、流量增大。电解质脉冲边界模型测得的流速与实际流速相差5%和10%所需测量距离分别为1.7-2.7m以及1.4～2.1m。冻土坡面径流流速为0.45～0.98m/s,是未冻土壤坡面径流流速的1.43倍。冰坡面径流流速随坡度、径流增加,介于0.49-1.09m/s。未冻土壤坡面相对冰坡面,径流流速小26-51%；冻土坡面与冰坡面径流流速相比小5～23%。不同大小粒径表碛覆盖下冰坡面径流流速介于0.015～0.217m/s,随坡度增加,基本不随流量变化。
对比了传统盐液示踪法、电解质脉冲边界模型、染色剂示踪法,研究了溶质示踪法测量流速校正系数。在设定的坡度(5°、10°、15°)、流量(12、24、48L/mmin)条件下,最大流速换算质心流速的校正系数均值大小为0.580,并且基本不随坡度变化。优势流速换算质心流速的校正系数均值为0.884,并随流量增加,受坡度影响不显著。
用溶质示踪法测量了浅沟流速。结果表明,浅沟径流流速随流量和坡度增加。传统盐液示踪法测量得到的流速在0.55-1.60m/s之间,而染色剂示踪法测量得到的流速为0.71-1.45m/s,略小于传统盐液示踪法测量结果。水流对示踪剂稀释及紊流对视觉影响,流速快和测量距离短产生的人体视觉反应误差可能导致测量流速降低,电解质示踪法测量的流速具有其合理性。
融水径流流速对研究融水径流剥蚀、泥沙输运过程以及开发以过程研究为基础的物理预报模型具有重要意义。
The overland flow velocity is an important parameter to characterize the dynamic characteristics of slope erosion, is a key determinant of the erosion forces and transport capabilities. The measurement of the overland velocity is important to the mechanism study of soil erosion and the soil erosion prediction mpdel.
A method to determinate the optimum measurement distance of the Pulse Boundary Model is proposed from the relationship of velocity and distance, and applied to simulated non-frozen slope and gravel layer. For the velocity measurement of flow along the simulated non-frozen slope using an electrolyte tracer method with a Pulse Boundary Model, the minimum distances for measured velocity with an error limit of5%was2.5m and those for an error limit of10%was2.0m from the injector under the given flow rates (5°,10°,15°) and slope gradients (12,24,36L/min).
A series of comparative flume experiments were conducted to study the flow velocity over frozen slopes and simulated ice slope with Pulse Boundary Model method and Dye Tracer method, along both the frozen slopes and non-frozen slope. The results showed that the water flow velocities over frozen slope increased with slope gradients and flow rates. The minimum distances for measured velocity with an error limit of5%was1.7-2.7m and those for an error limit of10%was1.4-2.1m from the injector under the given flow rates and slope gradients. The velocities, over frozen slopes, measured by the Pulse Boundary Model method under the given experimental conditions ranged from0.45m/s to0.98m/s, which were1.43times of those over non-frozen slopes. The velocities, over simulated ice slopes, measured by the Pulse Boundary Model method under the given three flow rates (12,24and48L/min) and three slope gradients (5°,10°and15°), ranged from0.49m/s to1.09m/s. which were5-23%higher of those over frozen slopes, and26-51%higher than those over the non-frozen slopes. The flow velocities over ice slope increased with slope gradients and flow rate, while those over ice slope covered by superglacial moraine increased with slope gradients, but stayed steady generally when the flow rate changed. The velocities, over simulated ice slopes covered by superglacial moraine, measured by the Pulse Boundary Model method under the given four flow rates (3,6,12, and24L/min) and four slope gradients (5°,10°,15°and25°), ranged from0.015m/s to0.217m/s.
A series of comparative flume experiments were conducted to measure the shallow water flow velocity, with a computerized electrolyte tracer method and dye tracer method. Centroid velocities, leading edge velocities, peak concentration velocities and velocities estimated by Pulse Boundary Model along the flume were computed for comparison purposes. The correction factor αE by which multiplied the leading egde velocity to obtain the centroid velocity were0.530-0.629, with a mean calue of0.580. The correction factor βE by which multiplied the peak concentration velocity to obtain the centroid velocity were0.819-0.975, with a mean calue of0.884.
A series of flume experiments were conducted to measure ephemeral gully water flow velocity with2methods, the electrolyte tracer method. The results showed that the velocity of ephemeral gully water flow increased with flow rate and slope gradient. The velocity measured by the electrolyte tracer method under the given experimental condition ranged from0.55m/s to1.60m/s, as compared with0.71m/s to1.45m/s by the dye tracer method. The velocities measured by the two methods were compared under different slope gradients and flow rates. The velocities measured by the dye tracer tended to be lower than those measured by the electrolyte tracer method. Considering the strong dilution and disturb effects of high rate water flow and strong turbulence on dye tracer, visual detection of dye movement should have caused later detection of the dye movement in water flow. All these indicate that the measured velocity of ephemeral flow seems rational.
The study on the melt water runoff velocity is of importance to the study of the machenism of soil erosion under melt water runoff.
本研究根据电解质脉冲边界模型测量的流速随距离增长的关系,提出了电解质脉冲边界模型测量最小距离优选方法。流速越大,电解质脉冲边界模型测量流速需要的测量距离越大。当设置土壤坡度为5°、10°、15°,流量为12、24、48L/mmin时,模拟未冻土壤表面误差限为5%、10%时分别需要2.5m、2.0m的测量距离。
在室内不同坡度(5°、10°、150)和流量(12、24、48L/mmin)条件下,用电解质脉冲边界模型以及染色剂示踪法进行冻土坡面、冰坡面径流流速测量的对比研究。结果表明,冻土坡面径流流速随坡度、流量增大。电解质脉冲边界模型测得的流速与实际流速相差5%和10%所需测量距离分别为1.7-2.7m以及1.4～2.1m。冻土坡面径流流速为0.45～0.98m/s,是未冻土壤坡面径流流速的1.43倍。冰坡面径流流速随坡度、径流增加,介于0.49-1.09m/s。未冻土壤坡面相对冰坡面,径流流速小26-51%；冻土坡面与冰坡面径流流速相比小5～23%。不同大小粒径表碛覆盖下冰坡面径流流速介于0.015～0.217m/s,随坡度增加,基本不随流量变化。
对比了传统盐液示踪法、电解质脉冲边界模型、染色剂示踪法,研究了溶质示踪法测量流速校正系数。在设定的坡度(5°、10°、15°)、流量(12、24、48L/mmin)条件下,最大流速换算质心流速的校正系数均值大小为0.580,并且基本不随坡度变化。优势流速换算质心流速的校正系数均值为0.884,并随流量增加,受坡度影响不显著。
用溶质示踪法测量了浅沟流速。结果表明,浅沟径流流速随流量和坡度增加。传统盐液示踪法测量得到的流速在0.55-1.60m/s之间,而染色剂示踪法测量得到的流速为0.71-1.45m/s,略小于传统盐液示踪法测量结果。水流对示踪剂稀释及紊流对视觉影响,流速快和测量距离短产生的人体视觉反应误差可能导致测量流速降低,电解质示踪法测量的流速具有其合理性。
融水径流流速对研究融水径流剥蚀、泥沙输运过程以及开发以过程研究为基础的物理预报模型具有重要意义。
The overland flow velocity is an important parameter to characterize the dynamic characteristics of slope erosion, is a key determinant of the erosion forces and transport capabilities. The measurement of the overland velocity is important to the mechanism study of soil erosion and the soil erosion prediction mpdel.
A method to determinate the optimum measurement distance of the Pulse Boundary Model is proposed from the relationship of velocity and distance, and applied to simulated non-frozen slope and gravel layer. For the velocity measurement of flow along the simulated non-frozen slope using an electrolyte tracer method with a Pulse Boundary Model, the minimum distances for measured velocity with an error limit of5%was2.5m and those for an error limit of10%was2.0m from the injector under the given flow rates (5°,10°,15°) and slope gradients (12,24,36L/min).
A series of comparative flume experiments were conducted to study the flow velocity over frozen slopes and simulated ice slope with Pulse Boundary Model method and Dye Tracer method, along both the frozen slopes and non-frozen slope. The results showed that the water flow velocities over frozen slope increased with slope gradients and flow rates. The minimum distances for measured velocity with an error limit of5%was1.7-2.7m and those for an error limit of10%was1.4-2.1m from the injector under the given flow rates and slope gradients. The velocities, over frozen slopes, measured by the Pulse Boundary Model method under the given experimental conditions ranged from0.45m/s to0.98m/s, which were1.43times of those over non-frozen slopes. The velocities, over simulated ice slopes, measured by the Pulse Boundary Model method under the given three flow rates (12,24and48L/min) and three slope gradients (5°,10°and15°), ranged from0.49m/s to1.09m/s. which were5-23%higher of those over frozen slopes, and26-51%higher than those over the non-frozen slopes. The flow velocities over ice slope increased with slope gradients and flow rate, while those over ice slope covered by superglacial moraine increased with slope gradients, but stayed steady generally when the flow rate changed. The velocities, over simulated ice slopes covered by superglacial moraine, measured by the Pulse Boundary Model method under the given four flow rates (3,6,12, and24L/min) and four slope gradients (5°,10°,15°and25°), ranged from0.015m/s to0.217m/s.
A series of comparative flume experiments were conducted to measure the shallow water flow velocity, with a computerized electrolyte tracer method and dye tracer method. Centroid velocities, leading edge velocities, peak concentration velocities and velocities estimated by Pulse Boundary Model along the flume were computed for comparison purposes. The correction factor αE by which multiplied the leading egde velocity to obtain the centroid velocity were0.530-0.629, with a mean calue of0.580. The correction factor βE by which multiplied the peak concentration velocity to obtain the centroid velocity were0.819-0.975, with a mean calue of0.884.
A series of flume experiments were conducted to measure ephemeral gully water flow velocity with2methods, the electrolyte tracer method. The results showed that the velocity of ephemeral gully water flow increased with flow rate and slope gradient. The velocity measured by the electrolyte tracer method under the given experimental condition ranged from0.55m/s to1.60m/s, as compared with0.71m/s to1.45m/s by the dye tracer method. The velocities measured by the two methods were compared under different slope gradients and flow rates. The velocities measured by the dye tracer tended to be lower than those measured by the electrolyte tracer method. Considering the strong dilution and disturb effects of high rate water flow and strong turbulence on dye tracer, visual detection of dye movement should have caused later detection of the dye movement in water flow. All these indicate that the measured velocity of ephemeral flow seems rational.
The study on the melt water runoff velocity is of importance to the study of the machenism of soil erosion under melt water runoff.
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