运用染色示踪方法研究土壤质地对土壤水非均匀流动特征的影响

为研究土壤质地对土壤水流运动非均匀特征的影响,在砂土、壤土和粉质粘土中采用亮蓝(砂土)和碘离子(壤土和粉质粘土)作为示踪剂分别开展了2个、5个和4个不同入渗条件(土壤初始含水率和入渗水量)的染色示踪试验,通过计算活动流场模型(Active Region Model,ARM)分形特征参数(γ)来定量描述和比较不同入渗条件下土壤水流运动的非均匀特征。研究结果表明,(1)活动流场模型较好的捕捉到了土壤水流运动整体的非均匀信息;(2)当其它入渗条件(土壤初始含水率和入渗水量)相同时,土壤水在细质地土壤中运动的非均匀程度要高于其在粗质地土壤中运动的非均匀程度。     

入渗水量和试验尺度对土壤水非均匀流动的影响

[目的]研究入渗水量和试验尺度对土壤水非均匀流动(最大入渗深度和平均入渗深度、土壤水流运动非均匀程度和土壤优先流尺寸的影响)的影响,为农业灌溉施肥的高效利用、地下水环境保护以及流域水文过程预测等方面提供理论支撑。[方法]采用亮蓝染色示踪方法在砂土条件下开展了9组18个(每组2个重复)不同入渗水量(分别为1.25,2.5和5.0cm)和试验尺度(分别为0.25m×0.25m,0.5m×0.5m和1.0m×1.0m)的入渗试验。[结果](1)相同试验尺度条件下,土壤水最大入渗深度和平均入渗深度均随着入渗水量的增大而增大;土壤水流运动非均匀程度随入渗水量的增大而先增大后减小。(2)相同入渗水量条件下,当入渗水量较小时,土壤水最大入渗深度和土壤水流运动非均匀程度随着试验尺度的增大而增大;当入渗水量很大时,试验尺度的变化对最大入渗深度和土壤水流运动非均匀程度的影响不明显。(3)入渗水量的增加和试验尺度的增大都将使得优先流通道尺寸增大。[结论]入渗水量和试验尺度对土壤优先流运动有重要影响。     

土壤性质对入渗再分布影响的显色示踪试验研究

同时使用染色剂和碘离子作为示踪剂,染色剂用于示踪大孔隙通道,根据碘-淀粉显色反应确定实际流动模式。开展了6组试验,研究了土壤大孔隙特征和非均匀流动特性,比较了粉土和粘土2种土壤,入渗水量分别为20、40、60和80 mm以及不同流动边界条件下的土壤水和溶质再分布特性。实验资料显示,入渗水再分布主要受到湿润模式的影响。入渗水量较小的情况下,水流运动主要发生在大孔隙中,随着入渗水量增大,入渗模式与孔隙发育表现出显著的区别,随着入渗水量的增加,水流运动非均匀性表现出先增加,随后减小的趋势。溶质迁移非均匀性取决于水流非均匀流动特性,然而表现出更多的不确定性。     

土壤非均匀水流运动和溶质迁移显色示踪方法研究

根据碘-淀粉显色原理示踪土壤非均匀流动,探讨非均匀水流运动和溶质迁移描述方法。在1.0m×1.0m尺度上开展试验,60mm碘离子溶液入渗后,在70cm深度内逐层开挖剖面,剖面中水流经过的区域喷洒淀粉溶液后显色,采用图像分析和率定的方法建立了土壤显色和碘离子浓度之间的关系。采用环状直方图,从浓度空间分布和信息量两个方面对流动非均匀性进行了描述。碘-淀粉显色示踪方法较好地显现了非均匀流动模式,环状直方图分析表明,浓度分布的离散程度随浓度值的减小而增加,描述流动的非均匀性需要考虑水平和垂直方向上流动非均匀特征,非均匀流动的相似性随着距离的增加而明显下降。     

黄土高原南部黄土渗流特征的染色示踪研究

为探究黄土中的渗流特征,明确不同初始条件对优先流的影响程度,使用亮蓝和离子染色剂,并控制入渗水量和初始含水率,在黄土高原南部进行染色示踪试验,根据获取的染色剖面图像,从定性和定量2个方面分析了优先流程度。结果表明：亮蓝染色剂在黄土中的染色深度有限,而离子染色剂经显色反应后能很好地示踪水的渗流;黄土高原南部黄土中优先流类型随土层深度从小到大为基质流—非均质指流—高相互作用大孔隙流—混合相互作用大孔隙流;优先流评价指数试坑A(0.55)>试坑C(0.48)>试坑B(0.46),优先流程度由高到低为试坑A—试坑C—试坑B;在其他条件相同时,黄土中更多的入渗水量、更大的初始含水率抑制优先流的发育,使基质入渗深度更大,基质流程度更高,优先流程度降低。研究结果可为黄土地区灾害防治、探明地下水污染机制提供参考。     

利用染色示踪法研究四面山两种林地优先路径分布特征

[目的]研究不同林种土壤的优先路径分布特征,为土壤水的高效利用以及植物生长环境改善等方面的研究提供理论参考。[方法]以重庆四面山张家山的针阔混交林和楠竹林为研究对象,在林地土壤存在优先路径的情况下,运用染色示踪法研究了水分及溶质的运移,并对采集的垂直剖面染色图像进行处理分析。[结果]两种林地对水分入渗的响应不同,染色路径宽度和染色路径数量在同一剖面不同深度处及不同剖面同一深度处均呈现明显的异质性:(1)针阔混交林染色路径宽度曲线呈"倒阶梯型";(2)楠竹林染色路径宽度曲线呈S形。两种林地的土壤优先流宽度和数量在一定范围内均随着深度增加而逐渐下降。[结论]两种林地均存在优先流现象,随着深度增加优先流路径不均匀递减,在0—20cm深度内,植物根系对土壤优先流影响较大。     

山地土壤优先流路径的染色示踪研究

在山地林区开展土壤大孔隙及优先流的实验研究,可深化对森林土壤涵养水源机理的认识,为山区的水土流失防治和植被恢复提供依据。利用剖面染色与图像分析相结合的方法,沿长江三峡大老岭-邓村一线,对山地不同垂直带内土壤优先流特征进行了调查,分析了优先流路径对剖面水分入渗过程的影响。结果显示,中山常绿落叶针阔混交林-山地黄棕壤、低山暖性针叶林-山地黄壤中大孔隙孔径大、分布广,有利于优先流的形成和入渗。受耕作扰动的弃耕土壤中大孔隙结构遭到破坏,优先流路径与森林土壤不同,且渗流强度较弱,染色区域较浅。森林土壤各发生层内优先流特征差异显著,腐殖质层内以洞穴流为主,水分与土壤基质域交换较少,多通过大孔隙快速下渗。淋溶淀积层内洞穴流消失或减弱,侧向渗透增强。低山暖性针叶林-山地黄壤质地较粗,出现以裂隙为主的大孔隙,优先流表现为裂隙流。弃耕土壤各发生层都表现为指流,染色面积随深度减小,侧向渗透基本稳定。植被-土壤垂直地带性分布是山地土壤优先流存在差异的主要原因,山区生态环境建设中应促进土壤优先流路径的发育。     

灌水效率碘—淀粉显色示踪试验

该文旨在研究不同土质、灌水量和灌水方法情况下入渗模式、灌水效率,并探讨不同灌水条件下溶质分布和水流运动模式之间的关系。根据碘－淀粉显色原理示踪水流运动和溶质迁移,分别在壤土和黏土条件下、开展了重力灌溉和微灌方式下的12组入渗试验,采用适用效率、深层渗漏损失率、有效储水率和均匀度对灌水效率进行综合评价。结果表明,入渗水再分布主要受到湿润模式的影响,有效储水率和均匀度随着灌水量的增加而提高,然而深层渗漏损失率也明显增大。溶质分布的均匀程度和深层渗漏损失率均小于水量分布的均匀程度和损失率,根据入渗后水分和溶质的再分布情况对灌水效率进行评价更为直接和全面。     

非均匀流动示踪试验及活动性流场模型的应用

采用显色和离子示踪方法,研究水流运动和溶质迁移非均匀特性,并分析活动性流场模型(ARM)描述水流运动和溶质迁移的有效性。运用碘-淀粉显色方法观测水流非均匀流动模式,用溴、氯和硝酸根三种离子示踪水流的非均匀运动特性。ARM耦合非均匀流动所具有的分形特性,该模型本构关系参数反映活动性流场面积比例和土壤水有效饱和度之间的分形关系。与连续性模型相比,ARM模拟土壤水流和溶质迁移结果与测定值更符合。在水平剖面三种离子浓度均表现出正态或对数正态分布规律,且总体上分布离散程度表现出随深度增加而减小的趋势,ARM有效地描述了非均匀流动下水流运动和溶质迁移所表现出的宏观特性。     

非均匀土壤区域SVAT模型中土壤水动力学参数的整合研究

荷兰Cabauw地区一个 10km×10km区域内的四种主要土壤的水动力学参数用一种实验室直接测定法 (Wind氏蒸发法 )和两种间接方法 (“分段土壤推导函数”、“连续土壤推导函数”)确定 ,而该区域水动力学特性参数的整合则采用两组方案 (聚合土壤参数法和有效土壤参数法 )进行。一个SVAT模型的模拟输出结果———感热通量、潜热通量与实测数据的比较分析表明 :(1)对于用“分段土壤推导函数”确定的土壤水动力学参数的区域整合 ,以“逆模拟法”(有效土壤参数法 )较为可行 ,其模拟感热、潜热的精确性接近参比方案 (“模拟 平均法”) ;(2 )对于实验室直接测定的参数 ,则以几何平均vanGenuchten Mualem经验公式参数的方案 (聚合土壤参数法 )为佳 ;(3)对于“连续土壤推导函数”推导的水动力学参数 ,几何平均土壤组分方案 (聚合土壤参数法 )和“逆模拟法”方案 (有效土壤参数法 )二者均可得到优于参比方案 (“模拟 平均法”)的模拟结果 ,其中以前者最佳 ;(4 )所有区域化参数整合方案中 ,以水平几何平均区域内实验室直接测定的参数的方案最优 ;同时 ,“连续土壤推导函数”法的土壤组分几何平均方案的模型输出精确性接近该最优方案     

土壤裂隙及其优先流研究进展

土壤在干燥脱水的过程中易收缩产生裂隙。裂隙的产生是土壤性质与外界条件等多种因素综合作用的结果,其形态结构也非常复杂,难以准确描述。裂隙能够作为优先流的路径,增加农田水分和养分的流失以及地下水污染的风险。本文总结和归纳了裂隙产生的影响因素、裂隙的表征指标与测定方法、裂隙导致的优先流的研究方法、裂隙对优先流的影响和模拟等方面的研究进展。今后应进一步加强裂隙产生机理的全面深入的研究;构建和完善裂隙三维指标体系及其测定方法;推进裂隙导致的优先流的定量化和数学模拟研究;加大田间原位裂隙及其优先流的研究。     

土壤优先流研究现状与发展趋势

优先流是近年来针对土壤水运动所提出的术语,是土壤中水运动机制研究由均匀走向非均匀领域的标志,是指在土壤各向异性的情况下,水分和溶质在多重因素的共同作用下,沿着特定的路径向下发生非稳定渗流的现象.优先流是造成降雨型滑坡、泥石流等地质灾害以及地下水质污染、农业土壤中养分流失等现象的主要诱因之一,所以深入开展优先流的研究显得尤为重要.本文从优先流的界定出发,主要介绍回顾了优先流数学模型的发展和研究优先流所采用的技术手段和方法,最后总结并探讨了优先流研究中存在的问题和发展趋势.     

土壤初始含水率对优先流的影响简

土壤中优先流的存在会造成肥料利用率降低以及土壤深层甚至地下水污染.为确定土壤初始含水率对优先流的影响,通过室内含大孔隙土柱定水头入渗实验,以长武黑垆土及渭河砂土为研究对象,分析不同土壤初始含水率对优先流的影响.结果表明：1）相同质地,当土壤初始含水率大于其斥水性的峰值含水率时,湿润锋运移深度随着土壤初始含水率的增大而增大,反之湿润锋运移深度随着初始含水率的增加而减少,不同质地土壤湿润锋运移速度随土壤粉粒质量分数升高而减慢;2）累积入渗量受到土壤储水性及斥水性的双重影响,导致与湿润锋的运移趋势并不一致,黑垆土对照CK组及优先流O-C-30组（除7.04％含水率外）累积入渗量随着土壤初始含水率的增大而减小,渭河砂土CK组及O-C-30组均呈现2阶段特征,累积入渗量先随着土壤初始含水率的增加而减少,之后随土壤初始含水率的增加而增加;3）Kostiakov入渗模型能很好地拟合累积入渗量随时间的变化过程,适用于存在优先流的土壤入渗模拟.该研究结果对土壤优先流水分模拟具有一定的指导意义.     

土壤优先流运动的活动流场模型分形特征参数计算

活动流场模型分形特征参数控制着优先流的产生和发展,因此准确获得活动流场模型分形特征参数值对提高模型的模拟预测精度具有重要意义。该研究采用染色示踪方法,将优先流流场从流动背景中显示出来,通过数字图像分析和采样分析获得优先流流场和流场内土壤含水率的分布模式,根据活动流场模型本构方程拟合活动流场模型分形特征参数值;针对3种常见的入渗后染色区内土壤含水率分布模式,分别提供了相应的活动流场模型分形特征参数的计算方法。研究结果显示,1）由于入渗后土壤水重分布的影响,活动流场区域和染色区域在整个入渗深度范围并不完全重合,因此仅可选择活动流场与染色区域相重合深度范围内受土壤初始含水率影响较小的数据来拟合活动流场模型分形特征参数值;2）土壤质地对入渗后染色区内土壤含水率的分布模式有显著影响,细质地土壤中入渗后染色区土壤含水率沿入渗方向逐渐减小,粗质地土壤中入渗后染色区土壤含水率沿入渗方向先增大后减小。     

Investigating preferential flow in a large intact soil block under pasture

Abstract. A large soil block was constructed to determine the importance of preferential flow routes compared with matric flow pathways at a pasture site in mid-Devon. The sandy loam soil was well structured and uniform. The soil block measured 5 m×3 m×1 m and was instrumented with an array of 54 tensiometers, TDR wave guides and suction samplers connected to an in situ chloride analysis system. Four steady state irrigation experiments were conducted with a range of rainfall intensities. During each experiment chloride and nitrate tracers were applied and the patterns of movement were observed. Although the application of tracer was uniform and the soil was relatively homogeneous, there was large variability across the block in terms of time taken to reach the peak concentration (TPC) and the peak concentration itself. About 44 samplers operated at the greatest intensities (10–2 mm h⁻¹) and only 35 at the smallest (1 mm h⁻¹). No relationship was found between TPC and depth. The fastest TPC and largest concentrations were associated with the greatest rainfall intensities. Relative importance of the individual water pathways was a function of soil heterogeneity: parts of the soil block were highly active with several pathways having short TPCs and conductivities in excess of 4 m day⁻¹ whereas other areas had longer TPCs and conductivities of 1–2 m day⁻¹. The pattern was also dynamic, with conductivities of the pathways changing through time, though most of the faster pathways maintained their greater conductivities for more than one year.     

Modeling daily soil water dynamics during vertical drainage using the incoming flow concept

Crop management models require simulation of daily soil water dynamics. The objective of this study was to develop a model to simulate the daily soil water dynamics during vertical drainage with reasonable accuracy using the incoming flow concept. The execution of this model, which has been developed based on the conservation of mass law, consists of two steps. First, calculating the potential daily change of soil water content (Δθp) for each soil layer in the profile assuming each one receives no water from the above layer. Then, calculating the actual daily change of soil water (Δθa) for each soil layer in the profile by adjusting Δθp using the incoming water flow, which can be defined as the amount of drainage water that reaches a layer in a soil profile from the above layer. The model was compared with the Suleiman and Ritchie [Suleiman, A.A., Ritchie, J.T., 2004. Modifications to the DSSAT vertical drainage model for more accurate soil water dynamics estimation. Soil Sci. 169 (11), 745–757] vertical drainage model (SRVDM) and HYDRUS-1D for diverse soils and was tested using drainage experimental data of a Eutric Regosol in Bekkevoort, Belgium and a sandy soil in Georgia, U.S. The difference in Δθp between the new model and HYDRUS-1D for diverse soils ranged from − 0.01 to 0.016 m³ m^− 3 for the first day and from − 0.005 to − 0.025 m³ m^− 3 for the second day while the difference in Δθp between the SRVDM and HYDRUS-1D for these soils ranged from 0.014 to 0.062 m³ m^− 3 for the first day and from − 0.01 to 0.026 m³ m^− 3 for the second day. The relative maximum absolute errors in Δθa between the new model and HYDRUS-1D was 10% while the relative maximum absolute errors in Δθa between the SRVDM and HYDRUS-1D was 112%. In the experiments, the root mean square difference of the soil water content for the new model was lower than that for the SRVDM at the different soil depths. These results indicated that the new model outperformed the SRVDM in simulating Δθp and Δθa for diverse soil. It can be concluded that the new model was robust and reasonably accurate for diverse soils at different soil depths. The implementation of such model will improve the accuracy and applicability of regional soil water dynamics simulation and will reduce considerably the computational time and the required inputs.     

Three-dimensional visualization and quantification of soil macroporosity and water flow patterns using computed tomography

Abstract. Efforts to assess the role of soil structure in soil and water processes have been limited by data based on two dimensional geometry or disturbed samples. Computed tomography (CT) is a non-invasive technique that allows for the three dimensional, non-destructive examination of heterogeneous materials. X-ray CT scanning was used to acquire serial images of contrasting soil types that could be used to render, and hence, quantify important soil constituents in three dimensions. By repeating the scanning techniques after an infiltration period, it was also possible to examine the nature of water movement in real time. Macropore architecture between different soil types was highly variable and generally appeared as unconnected pore segments at the resolution examined. As expected, water flow characteristics were similar to macropore structure, with wetting patterns resembling both Darcian and preferential flow identified in different soils. From this, it was found that in the sandy clay soil c . 90% of macropore space was active following infiltration, compared with c . 50% for the sandy loam soil. In addition, it was possible to visualize the three dimensional distribution of stones and other mineral material. The results illustrated the benefits of computed tomography over more conventional analyses of soil structure, and its potential as a tool for examining dynamic soil processes. However, problems associated with accessibility, resolution and artefacts still provide limitations of the technique.