土石混合介质水分溶质运移的试验研究
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摘要
由于成土原因和人类活动,不同数量、不同种类的碎石覆盖表土和嵌入土壤以及碎石夹层经常存在,碎石的存在不仅会改变土壤的某些物理和化学性质,还会进而影响地表水文过程、土壤水分运动及有效性。但因为碎石存在增大了取样的困难,大部分研究将土壤概化为均质介质,因此含有碎石的土壤的水文过程研究还相当有限。本文根据室内土柱模拟试验和神木六道沟流域及露天煤矿复垦土壤的田间试验小区观测试验,对不同碎石的含量,碎石直径及碎石种类对土壤水分溶质运移的影响进行研究,主要取得了以下结论:
(1)不同碎石含量、碎石直径、碎石夹层位置及碎石种类均对土壤水分运动过程产生较大影响。含有砾石、料礓石及煤矸石的土壤的入渗过程均可用Kostiakov入渗模型和Philip公式进行较好的表述;且湿润锋随时间的变化过程可以用幂函数进行较好拟合。三种碎石的存在,均对土壤水分入渗过程产生阻碍作用。形状规则、磨圆度接近1的砾石对土壤水分累积入渗量及湿润锋变化过程的影响效应基本一致。一定入渗历时内,二者均与碎石含量及直径成负相关性。饱和导水率随砾石含量先增大后减小,随砾石直径增大而减小,与砾石直径成指数函数关系;利用Peck-Watson和Bouwer-Rice方程对饱和导水率进行估算,砾石直径介于0.2-1.0cm时,结果较精确,砾石直径介于1.0-5.0cm时,估算结果偏大。含有形状较不规则的块状料礓石的混合介质土壤水分累积入渗量、湿润锋深度及饱和导水率小于均质土壤的累积入渗量,且随料礓石含量先减小后增加,在料礓石含量为40%时达到最低。Peck-Watson方程和Bouwer-Rice方程估算的饱和导水率的结果仅在料礓石含量10%及20%时较接近试验结果。料礓石夹层对土壤水分入渗过程阻渗作用,一定入渗历时内,料礓石夹层对累积入渗量及湿润锋深度变化明显减弱,使整个入渗过程进入稳渗阶段。形状不规则的片状煤矸石对累积入渗影响显著,一定入渗历时内,累积入渗量随煤矸石含量的增加而降低,湿润锋深度随煤矸石含量先增加而后减小,在煤矸石含量为30%时达到最小值。煤矸石存在可以减缓土壤水分蒸发作用,不同含量煤矸石的累积蒸发量的大小为:0>15%>30%>45%>60%>75%。相同碎石含量及直径条件下,煤矸石混合介质稳定入渗率及饱和导水率最大;碎石含量较低时,砾石与料礓石混合介质稳定入渗率差异不显著,随含量继续增加,料礓石混合介质入渗速率大于砾石混合介质。
(2)含有砾石、料礓石、煤矸石的土壤的氯离子穿透曲线无论碎石含量高低,直径大小,均可获得与均质土壤类似的平滑穿透曲线,且CDE方程和两区模型均可对土石混合介质的溶质运移过程进行较好描述。砾石、料礓石、煤矸石的存在较均质土壤对溶质运移过程均产生较大影响。砾石含量较高情况下,初始穿透时间较早,但拖尾现象严重。粒径为0.5cm的砾石直径是初始穿透时间的转折点。当砾石直径小于0.5cm时,初始穿透时间增加,拖尾现象显著;但随砾石直径继续增加,并无明显相关关系。当料礓石含量为60%时,溶质初始穿透时间最小,相对浓度达到最大时所需时间相对较长;但当料礓石含量为40%时,溶质完全穿透时间最长;煤矸石混合介质开始穿透时间均小于均质土壤所需时间,且随煤矸石含量增加先减少而后增加,在含量为30%时达到最小。
(3)砾石含量小于40%的土石混合介质,其弥散度均小于均质土壤。弥散度随砾石含量的增加先减小后增加,与砾石直径无显著相关关系。料礓石混合介质拟合参数Peclet值均远大于1,因此,含有料礓石的溶质运移过程中,对流为主要的运移方式,料礓石的存在抑制了溶质的弥散运动。β值在料礓石含量为10%-30%区间,变化不明显,当料礓石含量达到极限值时,β值急剧增加,但随料礓石含量继续增加,这种变化不再明显。煤矸石混合介质的溶质运移过程随煤矸石含量增加,穿透曲线变缓,弥散度变大;延迟因子随煤矸石含量增加先增加而后减小,在煤矸石含量为30%时达到最小,且煤矸石混合介质所得延迟因子数值均大于1;拟合参数β随煤矸石含量变化差异性显著,其值随煤矸石含量先降低而后增加,在煤矸石含量为30%时达到最小。碎石对于溶质运移过程阻碍作用显著,砾石及料礓石混合介质均在最大含量时最早检测出穿透氯离子,弥散度在碎石含量为40%时达到最大,而煤矸石恰与之相反。
(4)田间试验小区分析不同含量及种类的碎石对土壤水分运动过程的影响,结果表明:不同吸力处理下,同一类型碎石的初始入渗速率在最初水头(-15 cm)下最大,而稳定入渗速率均表现为0 cm >-3 cm >-15 cm;同一吸力下,在碎石含量逐渐增加的过程中,不同碎石类型的稳定入渗率变化不同。对于砾石,较大稳定入渗率值出现在碎石含量51.5%,最小值出现在砾石含量31.5%;对于煤矸石,最小值出现在60%碎石含量,最大值出现在15%碎石含量;而对于料礓石,稳定入渗率最小值出现在碎石含量20%处,最大值出现在碎石含量50%处。一定含量的碎石对增加入渗,减小产流具有积极作用,并因碎石类型不同,促进作用也有所不同。煤矸石含量15%和30%时的饱和导水率分别是均质土壤饱和导水率的1.33和1.21倍;料礓石含量为15%时的饱和导水率是均质土壤饱和导水率的1.48倍。
(5)马家塔露天煤矿复垦区四种不同土地利用类型的复垦土壤因回填填充材料及方法的不同,使得复垦土壤物理性质及水文性质产生较大差异。不同土地利用类型下的土壤水分入渗速率为:草地>林地>灌木>荒地,其特征在负压0cm时最为显著,且初始入渗速率与土壤初始含水量呈负相关关系。在入渗初期,负压对入渗速率影响效果不显著;随入渗历时增加,不同负压下四种土地利用类型的土壤入渗速率随入渗历时增加呈减小趋势明显,草地在三种不同负压下入渗速率随时间的变化趋势显著,荒地的变化趋势最弱。草地的土壤饱和导水率最大,其次是林地和灌木,荒地最小。饱和导水率与土壤容重成负相关关系。
(6)料礓石覆盖度及料礓石嵌入含量均对入渗补给系数产生显著影响,且料礓石含量对于入渗补给系数的影响大于料礓石覆盖度的影响。随料礓石覆盖度增加,入渗补给系数逐渐减小,低碎石含量情况下,料礓石含量同样与入渗补给系数具有负相关关系。料礓石嵌入小区的平均入渗速率随料礓石含量的增加而缓慢增加。料礓石覆盖的试验小区,初始径流时间大于料礓石嵌入的试验小区。料礓石覆盖度较大,即达到45.6%和62.7%时,初始入渗速率最大。入渗速率基本随料礓石含量的增大而呈减小趋势。Kostiakov入渗经验公式和Philip方程均可以对降雨入渗过程进行描述。
本文的研究结果及理论分析,有助于提高人们对含有碎石的土壤水分及溶质运移过程和机理的认识,,为土石山区生态恢复和环境改善具有重要意义。
Rock fragments are often present in soils as a result of soil genesis and human activity. The rock fragments are different in contents; species and some soils are covered or inserted by the rock fragments. Rock fragments in the soil may affect the soil structure and the tortuosity of water flow paths, which may further influence the hydrological process, soil water movement and its validity. Owing to the difficulties in soil sampling and the heterogeneous distribution of rock fragment, soil is taken as a conceptual medium with homogeneous and uniform particle composition in most of the studies. As a result, it is poorly understood for soil and water processes in stony soil. In this study, water movement and solute transport processes of different rock fragment contents, sizes, position, and species are studied through columns of disturbed soil samples and field soils containing rock fragments at Liudaogou small catchment and Majiata coalmine reclamation area in the wind-water erosion crisscross region of the Loess Plateau. The main results are as followings:
(1) Different rock fragment contents, sizes, positions and species have great effect on soil water movement.The infiltration process of the soil containing gravels, caliches and gangues can be both described by Kostiakov infiltration model and Philip equation very well. The wetting front change with time can be described by a power function. The presence of all these rock fragments in the soil impended infiltration. The smoothing gravels, of which the psephicity is equal to 1, have the same influences on cumulative infiltration and wetting front. For a given time period, both of them have a negative relationship with gravel contents and sizes. Saturated hydraulic conductivity (Ks) firstly decreased with the increases of the stone contents, and then increased. The relation between them followed binomial function; Ks decreased with the increases of the mean diameters of the stones; the relation between them followed index function. The values calculated by the equation of Peck-Watson and Bouwer-Rice were much greater than measured data when the stone sizes were between 1.0 and 5.0cm.The cumulative infiltration, wetting front and Ks of soil containing caliches with irregular shape were all smaller than those of homogenized soils. The cumulative infiltration initially decreased with increasing rock fragment content to minimum values for Rc = 40%, and then increased. The Peck-Watson and Bouwer-Rice equations predicted Ks for low rock fragment contents but failed to forecast the Ks for higher fragment contents. The soil infiltration process was impended by the caliches layers. The cumulative infiltration and wetting front decreased seriously at the caliches layer and then became stable. The gangue, of irregular sheet shape, had great impact on cumulative infiltration. The cumulative infiltration decreased with the increased of gangue contents and the wetting front decreased with increasing rock fragment content to minimum values for Rc = 30%, and then increased. The existence of gangues could reduce the evaporation. The effect of gangue contents on cumulative evaporation were as follows: 0>15%>30%>45%>60%>75%. The rock fragment species also affect the soil water infiltration process. The stable infiltration rates in soil with gangues were the largest; the stable infiltration rates of soil with gravels and soil with caliches were almost the same at a low rock fragment contents, and with the increase of the contents, the infiltration rate became much larger in soil with caliches.
(2) Smooth breakthrough curves were obtained in soils containing rock fragments with different contents, sizes and species, which followed a similar trend to those typical for a homogeneous soil without stones. Solute transport processes were described accurately by both the convection-dispersion equation and the two-region model. Comparing to the homogenous soil, the existences of gravels; caliches and gangues affect the solute transport process significantly. When the gravel content was higher, the initial time was much smaller but the tailing phenomenon was very seriously. When the gravel size were between 0.2-0.5cm and 3.0-5.0cm, the initial breakthrough time and the fully breakthrough time were increased obviously with the gravel contents. When the gravel size is between 0.2-0.5cm, the initial breakthrough time was the shortest; but with the increase of the gravel contents, the differences are not obviously. When caliches content was 60%, solute was present in the effluent in a relatively short time, but it took a relatively long time for breakthrough to finish; it took the longest time to break though the column when the caliches content was 40%. The solute was present in the effluent much earlier in the soil containing gangues than that in homogeneous soil and the time first decreased with the gangue contents and then increased. The solute was detected latest in the effluent gangue content was 30%.
(3)The dispersivity first decreased with the increases of gravel contents and then increased, but had no relationship with the gravel sizes. When the gravel size was between 0.2-0.5cm, the retardation factor changed unobvious with gavel contents. The higher Peclet number indicates that the advection process dominates. Fraction in mobile water initially declined with increasing rock content but values did not vary greatly for contents between 10% and 30%. The fraction became significantly larger when Rc was 40% but again did not vary greatly when Rc was between 40% and 60%.With the increase of gangue contents, the breakthrough curves became very slow, and the dispersivity increased. The retardation factor first increased with the gangue content and then decreased to the minimum value for Rc=30%.The rock fragments also have the effect on the solute transport process. The chloride was first detected when the contents of gravel and caliches was biggest, and the dispersivity became the largest when at the content of 40% on a weight basis, but the opposite is true for the soil containing gangues.
(4)Through the study on the effect of rock fragments on soil water movement in field soils, the results were: the initial infiltration rate was the biggest when the negative pressure was -15cm and the stable infiltration rate of different negative pressure was as follows: 0 cm > -3 cm > -15 cm. The stable infiltration rate of different species changed variously with the gradually increases of rock fragment contents. The biggest stable infiltration rate of soil containing gravels appeared when the content was 51.5% and the smallest one arrived when the contents became 31.5%. As for the soil containing caliches and gangues, the special contents for the biggest infiltration rate were 60%, 15% and the smallest infiltration rate were 15%, 20%, respectively. The saturated hydraulic conductivity followed the same trend.
(5) As a result of different reclaiming materials and methods, the soil physical properties and soil water movement varied greatly of four landuse types in Majiata coalmine reclamation area. The infiltration rates of the four landuse types presented the tendency as follows: grass land >forest land>shrub land>barren land. The tendency was .significant when the negative pressure was 0cm.The initial infiltration rate had a negative relationship with the soil initial water content. During the initial stage of the infiltration process, the effect of the negative pressure was not significant; but with the infiltration proceeding, the infiltration rate of grass land changed most obviously but the changes are very weak for the barren land. The saturated hydraulic conductivity of the landuse types presented the same tendency to the infiltration rate and a negative relationship could be also found between the soil bulk density and saturated hydraulic conductivity.
(6)Caliches coverage and contents had a great effect on recharge coefficient and the effect of the latter was much bigger. The recharge coeffient reduced gradually with the increase of caliches coverage and there was a negative relationship between the low caliches content and recharge coeffient. The initial runoff time of the plot with caliches covering was a little longer than that in the plot with caliches in it. The average infiltration rate in the plot with caliches in it decreased with the increase of caliches contents. The initial infiltration rate became the biggest at the caliches coverage of 45.6% and 62.7%.The Kostiakov infiltration model and Philip equation could describe the precipitation infiltration process well.
The experimental study and analyses in this dissertation are helpful to the understanding the processes and mechanisms of water and solute transport in stony soils which is of great importance for providing recommendations of environmental quality improvement in the related regions with stony soils.
(1)不同碎石含量、碎石直径、碎石夹层位置及碎石种类均对土壤水分运动过程产生较大影响。含有砾石、料礓石及煤矸石的土壤的入渗过程均可用Kostiakov入渗模型和Philip公式进行较好的表述;且湿润锋随时间的变化过程可以用幂函数进行较好拟合。三种碎石的存在,均对土壤水分入渗过程产生阻碍作用。形状规则、磨圆度接近1的砾石对土壤水分累积入渗量及湿润锋变化过程的影响效应基本一致。一定入渗历时内,二者均与碎石含量及直径成负相关性。饱和导水率随砾石含量先增大后减小,随砾石直径增大而减小,与砾石直径成指数函数关系;利用Peck-Watson和Bouwer-Rice方程对饱和导水率进行估算,砾石直径介于0.2-1.0cm时,结果较精确,砾石直径介于1.0-5.0cm时,估算结果偏大。含有形状较不规则的块状料礓石的混合介质土壤水分累积入渗量、湿润锋深度及饱和导水率小于均质土壤的累积入渗量,且随料礓石含量先减小后增加,在料礓石含量为40%时达到最低。Peck-Watson方程和Bouwer-Rice方程估算的饱和导水率的结果仅在料礓石含量10%及20%时较接近试验结果。料礓石夹层对土壤水分入渗过程阻渗作用,一定入渗历时内,料礓石夹层对累积入渗量及湿润锋深度变化明显减弱,使整个入渗过程进入稳渗阶段。形状不规则的片状煤矸石对累积入渗影响显著,一定入渗历时内,累积入渗量随煤矸石含量的增加而降低,湿润锋深度随煤矸石含量先增加而后减小,在煤矸石含量为30%时达到最小值。煤矸石存在可以减缓土壤水分蒸发作用,不同含量煤矸石的累积蒸发量的大小为:0>15%>30%>45%>60%>75%。相同碎石含量及直径条件下,煤矸石混合介质稳定入渗率及饱和导水率最大;碎石含量较低时,砾石与料礓石混合介质稳定入渗率差异不显著,随含量继续增加,料礓石混合介质入渗速率大于砾石混合介质。
(2)含有砾石、料礓石、煤矸石的土壤的氯离子穿透曲线无论碎石含量高低,直径大小,均可获得与均质土壤类似的平滑穿透曲线,且CDE方程和两区模型均可对土石混合介质的溶质运移过程进行较好描述。砾石、料礓石、煤矸石的存在较均质土壤对溶质运移过程均产生较大影响。砾石含量较高情况下,初始穿透时间较早,但拖尾现象严重。粒径为0.5cm的砾石直径是初始穿透时间的转折点。当砾石直径小于0.5cm时,初始穿透时间增加,拖尾现象显著;但随砾石直径继续增加,并无明显相关关系。当料礓石含量为60%时,溶质初始穿透时间最小,相对浓度达到最大时所需时间相对较长;但当料礓石含量为40%时,溶质完全穿透时间最长;煤矸石混合介质开始穿透时间均小于均质土壤所需时间,且随煤矸石含量增加先减少而后增加,在含量为30%时达到最小。
(3)砾石含量小于40%的土石混合介质,其弥散度均小于均质土壤。弥散度随砾石含量的增加先减小后增加,与砾石直径无显著相关关系。料礓石混合介质拟合参数Peclet值均远大于1,因此,含有料礓石的溶质运移过程中,对流为主要的运移方式,料礓石的存在抑制了溶质的弥散运动。β值在料礓石含量为10%-30%区间,变化不明显,当料礓石含量达到极限值时,β值急剧增加,但随料礓石含量继续增加,这种变化不再明显。煤矸石混合介质的溶质运移过程随煤矸石含量增加,穿透曲线变缓,弥散度变大;延迟因子随煤矸石含量增加先增加而后减小,在煤矸石含量为30%时达到最小,且煤矸石混合介质所得延迟因子数值均大于1;拟合参数β随煤矸石含量变化差异性显著,其值随煤矸石含量先降低而后增加,在煤矸石含量为30%时达到最小。碎石对于溶质运移过程阻碍作用显著,砾石及料礓石混合介质均在最大含量时最早检测出穿透氯离子,弥散度在碎石含量为40%时达到最大,而煤矸石恰与之相反。
(4)田间试验小区分析不同含量及种类的碎石对土壤水分运动过程的影响,结果表明:不同吸力处理下,同一类型碎石的初始入渗速率在最初水头(-15 cm)下最大,而稳定入渗速率均表现为0 cm >-3 cm >-15 cm;同一吸力下,在碎石含量逐渐增加的过程中,不同碎石类型的稳定入渗率变化不同。对于砾石,较大稳定入渗率值出现在碎石含量51.5%,最小值出现在砾石含量31.5%;对于煤矸石,最小值出现在60%碎石含量,最大值出现在15%碎石含量;而对于料礓石,稳定入渗率最小值出现在碎石含量20%处,最大值出现在碎石含量50%处。一定含量的碎石对增加入渗,减小产流具有积极作用,并因碎石类型不同,促进作用也有所不同。煤矸石含量15%和30%时的饱和导水率分别是均质土壤饱和导水率的1.33和1.21倍;料礓石含量为15%时的饱和导水率是均质土壤饱和导水率的1.48倍。
(5)马家塔露天煤矿复垦区四种不同土地利用类型的复垦土壤因回填填充材料及方法的不同,使得复垦土壤物理性质及水文性质产生较大差异。不同土地利用类型下的土壤水分入渗速率为:草地>林地>灌木>荒地,其特征在负压0cm时最为显著,且初始入渗速率与土壤初始含水量呈负相关关系。在入渗初期,负压对入渗速率影响效果不显著;随入渗历时增加,不同负压下四种土地利用类型的土壤入渗速率随入渗历时增加呈减小趋势明显,草地在三种不同负压下入渗速率随时间的变化趋势显著,荒地的变化趋势最弱。草地的土壤饱和导水率最大,其次是林地和灌木,荒地最小。饱和导水率与土壤容重成负相关关系。
(6)料礓石覆盖度及料礓石嵌入含量均对入渗补给系数产生显著影响,且料礓石含量对于入渗补给系数的影响大于料礓石覆盖度的影响。随料礓石覆盖度增加,入渗补给系数逐渐减小,低碎石含量情况下,料礓石含量同样与入渗补给系数具有负相关关系。料礓石嵌入小区的平均入渗速率随料礓石含量的增加而缓慢增加。料礓石覆盖的试验小区,初始径流时间大于料礓石嵌入的试验小区。料礓石覆盖度较大,即达到45.6%和62.7%时,初始入渗速率最大。入渗速率基本随料礓石含量的增大而呈减小趋势。Kostiakov入渗经验公式和Philip方程均可以对降雨入渗过程进行描述。
本文的研究结果及理论分析,有助于提高人们对含有碎石的土壤水分及溶质运移过程和机理的认识,,为土石山区生态恢复和环境改善具有重要意义。
Rock fragments are often present in soils as a result of soil genesis and human activity. The rock fragments are different in contents; species and some soils are covered or inserted by the rock fragments. Rock fragments in the soil may affect the soil structure and the tortuosity of water flow paths, which may further influence the hydrological process, soil water movement and its validity. Owing to the difficulties in soil sampling and the heterogeneous distribution of rock fragment, soil is taken as a conceptual medium with homogeneous and uniform particle composition in most of the studies. As a result, it is poorly understood for soil and water processes in stony soil. In this study, water movement and solute transport processes of different rock fragment contents, sizes, position, and species are studied through columns of disturbed soil samples and field soils containing rock fragments at Liudaogou small catchment and Majiata coalmine reclamation area in the wind-water erosion crisscross region of the Loess Plateau. The main results are as followings:
(1) Different rock fragment contents, sizes, positions and species have great effect on soil water movement.The infiltration process of the soil containing gravels, caliches and gangues can be both described by Kostiakov infiltration model and Philip equation very well. The wetting front change with time can be described by a power function. The presence of all these rock fragments in the soil impended infiltration. The smoothing gravels, of which the psephicity is equal to 1, have the same influences on cumulative infiltration and wetting front. For a given time period, both of them have a negative relationship with gravel contents and sizes. Saturated hydraulic conductivity (Ks) firstly decreased with the increases of the stone contents, and then increased. The relation between them followed binomial function; Ks decreased with the increases of the mean diameters of the stones; the relation between them followed index function. The values calculated by the equation of Peck-Watson and Bouwer-Rice were much greater than measured data when the stone sizes were between 1.0 and 5.0cm.The cumulative infiltration, wetting front and Ks of soil containing caliches with irregular shape were all smaller than those of homogenized soils. The cumulative infiltration initially decreased with increasing rock fragment content to minimum values for Rc = 40%, and then increased. The Peck-Watson and Bouwer-Rice equations predicted Ks for low rock fragment contents but failed to forecast the Ks for higher fragment contents. The soil infiltration process was impended by the caliches layers. The cumulative infiltration and wetting front decreased seriously at the caliches layer and then became stable. The gangue, of irregular sheet shape, had great impact on cumulative infiltration. The cumulative infiltration decreased with the increased of gangue contents and the wetting front decreased with increasing rock fragment content to minimum values for Rc = 30%, and then increased. The existence of gangues could reduce the evaporation. The effect of gangue contents on cumulative evaporation were as follows: 0>15%>30%>45%>60%>75%. The rock fragment species also affect the soil water infiltration process. The stable infiltration rates in soil with gangues were the largest; the stable infiltration rates of soil with gravels and soil with caliches were almost the same at a low rock fragment contents, and with the increase of the contents, the infiltration rate became much larger in soil with caliches.
(2) Smooth breakthrough curves were obtained in soils containing rock fragments with different contents, sizes and species, which followed a similar trend to those typical for a homogeneous soil without stones. Solute transport processes were described accurately by both the convection-dispersion equation and the two-region model. Comparing to the homogenous soil, the existences of gravels; caliches and gangues affect the solute transport process significantly. When the gravel content was higher, the initial time was much smaller but the tailing phenomenon was very seriously. When the gravel size were between 0.2-0.5cm and 3.0-5.0cm, the initial breakthrough time and the fully breakthrough time were increased obviously with the gravel contents. When the gravel size is between 0.2-0.5cm, the initial breakthrough time was the shortest; but with the increase of the gravel contents, the differences are not obviously. When caliches content was 60%, solute was present in the effluent in a relatively short time, but it took a relatively long time for breakthrough to finish; it took the longest time to break though the column when the caliches content was 40%. The solute was present in the effluent much earlier in the soil containing gangues than that in homogeneous soil and the time first decreased with the gangue contents and then increased. The solute was detected latest in the effluent gangue content was 30%.
(3)The dispersivity first decreased with the increases of gravel contents and then increased, but had no relationship with the gravel sizes. When the gravel size was between 0.2-0.5cm, the retardation factor changed unobvious with gavel contents. The higher Peclet number indicates that the advection process dominates. Fraction in mobile water initially declined with increasing rock content but values did not vary greatly for contents between 10% and 30%. The fraction became significantly larger when Rc was 40% but again did not vary greatly when Rc was between 40% and 60%.With the increase of gangue contents, the breakthrough curves became very slow, and the dispersivity increased. The retardation factor first increased with the gangue content and then decreased to the minimum value for Rc=30%.The rock fragments also have the effect on the solute transport process. The chloride was first detected when the contents of gravel and caliches was biggest, and the dispersivity became the largest when at the content of 40% on a weight basis, but the opposite is true for the soil containing gangues.
(4)Through the study on the effect of rock fragments on soil water movement in field soils, the results were: the initial infiltration rate was the biggest when the negative pressure was -15cm and the stable infiltration rate of different negative pressure was as follows: 0 cm > -3 cm > -15 cm. The stable infiltration rate of different species changed variously with the gradually increases of rock fragment contents. The biggest stable infiltration rate of soil containing gravels appeared when the content was 51.5% and the smallest one arrived when the contents became 31.5%. As for the soil containing caliches and gangues, the special contents for the biggest infiltration rate were 60%, 15% and the smallest infiltration rate were 15%, 20%, respectively. The saturated hydraulic conductivity followed the same trend.
(5) As a result of different reclaiming materials and methods, the soil physical properties and soil water movement varied greatly of four landuse types in Majiata coalmine reclamation area. The infiltration rates of the four landuse types presented the tendency as follows: grass land >forest land>shrub land>barren land. The tendency was .significant when the negative pressure was 0cm.The initial infiltration rate had a negative relationship with the soil initial water content. During the initial stage of the infiltration process, the effect of the negative pressure was not significant; but with the infiltration proceeding, the infiltration rate of grass land changed most obviously but the changes are very weak for the barren land. The saturated hydraulic conductivity of the landuse types presented the same tendency to the infiltration rate and a negative relationship could be also found between the soil bulk density and saturated hydraulic conductivity.
(6)Caliches coverage and contents had a great effect on recharge coefficient and the effect of the latter was much bigger. The recharge coeffient reduced gradually with the increase of caliches coverage and there was a negative relationship between the low caliches content and recharge coeffient. The initial runoff time of the plot with caliches covering was a little longer than that in the plot with caliches in it. The average infiltration rate in the plot with caliches in it decreased with the increase of caliches contents. The initial infiltration rate became the biggest at the caliches coverage of 45.6% and 62.7%.The Kostiakov infiltration model and Philip equation could describe the precipitation infiltration process well.
The experimental study and analyses in this dissertation are helpful to the understanding the processes and mechanisms of water and solute transport in stony soils which is of great importance for providing recommendations of environmental quality improvement in the related regions with stony soils.
引文
[1]来剑斌.土壤水分运动特征及参数确定[D].博士论文,陕西:西安理工大学,2003.
[2]马东豪.黄土区土石混合介质水分运动试验研究及数值模拟[D].博士论文,北京:中国科学院地理科学与资源研究所,2008.
[3] Meyer L D,Johnson C B,Foster G R.Stone and woodchip mulches for erosion control on construction sites[J]. Journal of Soil and Water Conservation,1972,27:264～269
[4]符素华.土壤中砾石存在对入渗影响研究进展[J].水土保持学报,2005,19(1):171～175.
[5] Posesen J, Lavee H. Rock fragments in top soils: significance and processes[J].Catena,1994, 23:1-28
[6] CoileT S.Moisture content of small stone in soil[J]. Soil Sci.1953,75:203-207
[7]吕国安,陈明亮,王春潮。丹江口库区石渣土土壤水分特性研究[J].华中农业大学学报,2000,19(4):342-345.
[8]侯庆春.神木试区自然条件及环境整治综合分析[A].中国科学院水利部西北水土保持研究所集刊, 1993, 18: 136-144.,
[9]贾恒义,雍少萍,王富乾.神木试区的土壤资源[A].中国科学院水利部西北水土保持研究所集刊, 1993, 18: 36-46.
[10]唐克丽,侯庆春,王斌科,张平仓.黄土高原水蚀风蚀交错带和神木试区的环境背景及整治方法[A].中国科学院水利部西北水土保持研究所集刊, 1993, 18: 2-15.
[11] Ugolini F C, Corti G, Agnelli A 1,et al. Mineralogical, Physical, and Chemical properties of rock fragments in soil[J]. Soil Sci. 1996,161(8):521-542, August.
[12] Williams R D, Schuman G E. Reclaiming mine soils and overburned in western United States, analytic parameters and procedures[C].Soil Conser Soc of Amer, 1987, 259-282.
[13]Wesemael B V,Poesen J, de Figueriedo T. Effect of rock fragments on physical degradationof cultivatied soils by rainfall[J].Soil and Till Res,1995,33(3):229-250.
[14] Sauer Th J, Logsdon S D. Hydraulic and physical properties of stony soils in a small watershed[J].Soil Sci. Soc. Am. J 2002,66:1947-1956
[15] PoesenJ. Surface sealing as influenced by slope angle and position of simulated stones in the top layer of loose sediments[J]. Earth Surf.Process.Landforms,1986,11:1-10
[16] Corti G, Ugolini F C, Agnelli A et al .The soil skeleton, a forgotten pool of carbon and nitrogen in soil[J]. Euro J .Soil Sci, 2002,53(2 ) :283-288.
[17] Flint AL, Childs S.Development and calibration of an irregular hole bulk density sampler[J]. Soil Sci. Soc. Am. 1984, 48:374-378
[18] Ravina, I.; Magier,J., Hydraulic conductivity and water retention of clay soils containing rock fragments[J]. Soil Sci. Soc. Am. J. 1984, 48:736-740
[19]王慧芳.黄土高原土石混合介质水分溶质运移试验研究[D].博士论文,陕西:中国科学院水土保持研究所,2007.
[20] Corti G, Ugolini F C, Agnelli A et al. The soil skeleton, a forgotten pool of carbon and nitrogen in soil[J]. European Journal of Soil Science 2002,53(2 ) :283-288.
[21] Posesen J,Lavee,H. Rock fragments in top soils: significance and processes[J]. Catena,1994, 23:1-28
[22] Meyer L D, Johnson C B, Foster G R. Stone and woodchip mulches forerosion control on constructionsites[J].Soil Water Conser.,1972,27:246-269
[23] Brakensiek D L, RawlsW J, Stephenson G R. A note on determining soil properties for soils containing rock fragments, [J] J .RangManage,1986a,50(3):408-409
[24] Shipp R F, Matelski R P. Bulk-density and coarse-fragment determinations on some pennsylvania soils[J].Soil Sci.1965,99:392-397
[25] Torri D,Poesen J.Monaci F,Busoni E.Rock fragment content and fine soil bulk density[J].Catena,1994,23:65-71·
[26] Cerda,A. Effects of rock fragment cover on soil infiltration, interrill runoff and erosion[J]. European J.of Soil Sci.2001,52:59-68
[27] ReinhartK. The problem of stones in soil-moisture measurements[J]. Soil Sci.Soc.Am.Proc. 1961, 25:268-270
[28] Epstein E, Grant W J and Struchtemeyer R A. Effects of stone on runoff,erosion and soil moisture[J]. Soil Sci. Soc. Proc: 1966,638-640.
[29] Petersen G W ,Cunningham R L,Matelski R P. Moisture characteristic of Pennsylvania soils:II.Soil factors affecting moisture retention within a textural class-silt loam [J].Soil Sci Soc Amer Proc:1968,32(6):866-870
[30] Ingelmo F, Cuadrado S., Ibanes A and et al. Hydric properties of some Spanish soils in relation to their rock fragment content: influence for runoff and vegetation In: Poesen, J.; 32 Lavee ,H (Editors)Rock fragment content: surface dynamics[J]. Catena,1994,23;73-85
[31] Poesen J.Surface sealing as influenced by slope angle and position of simulated stones in the top layer of loose sediments [J].Earth Surf.Proc.Landforms,1986,11:1-10
[32] Box J E.The effects of surface slaty fragments on soil erosion by water[J].Soil Sci.Soc.Am.J,1981,45:111-116
[33] Valentin C,Casenave A, Infiltration into sealed soils as influenced by gravel cover[J]. Soil Sci. Soc. Am.J. 1992, 56:1667-1673
[34] Wilcox B P,Wood M K.Factors influencing interrill erosion from semiarid slopes in New Mexico[J].J . Range Management. l988,42:66-70.
[35] Abrahams A D, Parsons A J. Relation between infiltration and stone cover on a semiarid hillslope .southern Arizona [J]. J.Hydrol.1991,122:49-59
[36] Poesen J; Torri.D Mechanisms governing incipient motion of ellipsoidal rock fragments in concentrated overland flow[J].Earth Surf, Process Landforms 1989,14:469480
[37] Peck A J, Watson,J.D.Hydraulic conductivity and flow in non-uniform soil. In:Workshop on Soil Physics and Field heterogeneity CSIRO Div. of Environmental Mechanics[R].Canberra,1979,31-39
[38] Flint A L, Childs S. Development and Calibration of an Irregular Hole Bulk Density Sampler[J]. Soil Sci. Soc. Am.J,1984, 48:374-378
[39] Brakensiek D L,Rawls W J. Soil containing rock fragments: effects on infiltration[J]. Catena, 1994,23:99-110
[40] Bouwer H, Rice R C. Hydraulic properties of stony vadose zones[J]. Ground Water, 1984, 22(6) 696-705
[42] Mehuys G R, Stolzy L H, Levey J and et al. Effects of stones on the hydraulic conductivity of relatively dry desert soils[J]. Soi Sci. Am.Proc.1975, 39:37-42
[43] Corey A T, Kemper W D. Conservation of soil water by gravel mulches[D].Hydrology papers no. 30.Colorado State University, Fort Collins, 1986, 23
[44] Marion G M, Kummerow J, Miller P C.Predicting nitrogen mineralization in chaparral soils[J]. Soil Sci. Am. J., 1981, 45: 956-961.
[45] Gleason K J, Krantz W B,Caine N.,George S H and et al. Geometrical aspects of sorted patterned ground in recurrently frozen soil[J]. Scicence, 1986, 232: 216-220.
[46] Govers G, Poesen J. Field experiments on the transport of rock fragments by animal trampling on scree slopes[J]. Geomorphology, 1998, 23, 193– 203.
[47] Govers G,Vandaele K,Desmet P and et al. The role of tillage in soil distribution on hill slopes [J]. Eur. J. Soil Sci., 1994, 45: 469-478.
[48] Kemper W D,Nick A D,Corey A T.Accumulation of water in soils under gravel and sand mulches[J].Soil Sci. Soc. Am. J, 1994,58:56-63
[49]许秀元,陈同斌.土壤中溶质运移模拟的理论与应用[J].地理研究.1998, 17(1),23-28.
[50]李学恒.土壤化学[M].北京:高等教育出社.2001,151-225
[51]石元舂,等.盐渍土的水盐运动[M].北京:北京农业大学出版社,1986.
[52]李韵珠,李保国.土壤溶质运移[M],北京:科学出版社。1998
[53] Russo D. Leaching characteristics of a stony desert soil[J].Soil Sic. Soc. Am. J 1983, 47:431-438
[54] Schulin R, Wierenga P J ,et al. Solute transport through a stony soil[J]. Soil Sci. Soc. Am. J. 1987,51:36-42
[55] Buchter B, Hinz C, Feller M G and et al. Heterogeneous flow and solute transport in an unsaturated stony soil monolith[J]. Soil Sci. Soc. Am.J 1995,59:14-21
[56]Buchter B, Hinz C,Feller M G and et al. Cadmium Transport in an unsaturated stony sub soil monolith[J]. Soil Sci.Soc.Am.J. 1996, 60:716-721
[57]康世永.马家塔露天矿土地复垦方式的探讨[J].露天采煤技术, 1998, 2: 48-49.
[58] Meyer L D,Johnson C B,Foster G R.Stone and woodchip mulches for erosion control on construction sites [J].J. Soil Water Conser,1972,27:264～269
[59]Grant W J,Struchtemeyer R A.Effect of stones on runoff, erosion,and soil moisture[J]. Soil Sci. Soc. Amer. Proc.,1966,30:638～640
[60] Reigner I C, Phillips J J. Variations in bulk density and moisture content within two new Jersey coastal plain soils, Lakeland and Lakehurst sands[J]. Soil Sci. Soc.Amer. Proc, 1964, 28: 287～289
[61]符素华,段淑怀,刘宝元.密云石匣小流域土地利用对土壤粗化的影响[J].地理研究,2001,20(6):697—702.
[62] Grant R, Struchtemeyer R A.Influnce of coarse fraction in two Marine potato soils on infiltration,runoff and erosion[J].Soil Sci Soc of Amer Proc,1959,23: 391-394
[63]Abrahams A D, Parsons A J. Hydraulic of interrill overland flow on stone-covered desert surfaces[J]. Catena, 1994, 23: 111-140
[64] Valentin C. Surface sealing as affected by various rock fragment covers in West Africa[J]. Catena, 1994, 23:87-97
[65] Govers G,Vandaele K,Desmet Pand et al. The role of tillage in soil distribution on hill slopes[J]. Eur. J. Soil Sci., 1994, 45: 469-478.
[66]邵明安.非饱和土壤导水参数的推求[A].1:理论.中国科学院西北水土保持研究所集刊,1991,13:13～25.
[67]周蓓蓓,邵明安。不同碎石含量及直径对土壤水分入渗的影响[J].土壤学报,44(2007) 801-801.
[68] Wilcox B P, Wood M K, Tromble J M. Factors influencing infiltrability of semiarid mountain slopes[J]. J.Range Manage, 1988, 41(3), 197~206
[69]Reigner I C, Phillips J J. Variations in bulk density and moisture content within two new Jersey coastal plain soils, Lakeland and Lakehurst sands[J]. Soil Sci. Soc.Amer. Proc, 1964, 28: 287～289
[70] Grant R, Struchtemeyer R A.Influnce of coarse fraction in two Marine potato soils on infiltration,runoff and erosion[J].Soil Sci Soc Amer Proc,1959,23: 391～394
[71] Valentin C. Surface sealing as affected by variousrock fragment covers in West Africa[J]. Catena, 1994, 23:87～97
[72]张信宝,安芷生.黄土高原地区森林与黄土厚度的关系[J].水土保持通报,1994,14(6):1～3.
[73]王全久,邵明安.非饱和土壤导水特性分析[J].土壤侵蚀与水土保持学报,1998,4(6): 16～22.
[74]刘建国,王洪涛,聂永丰.多孔介质非饱和导水率预测的分型模型[J].水科学进展,2004, 15(3):269～275.
[75] Mehuys G R, Stolzy L H, Letey J, et al. Effect of stones on the hydraulic conductivity of relatively dry desert soils[J]. Soil Sci. Soc. Amer. Proc., 1975, 39: 37～42
[76]Wilcox B P, Wood M K, Tromble J M. Factors influencing infiltrability of semiarid mountain slopes[J]. Range Manage, 1988, 41(3), 197~206
[77]Bodman C B, Coleman E A. Moisture and energy conduction during down-ward entry of water into soil[J]. Soil Sci.Soc.Am.J,1944,2(8),166～182
[78]邹焱,陈洪松,苏以荣,邵明安.红壤积水入渗及土壤水分再分布规律室内模拟试验研究[J].水土保持学报,2005,19(3),174～177.
[79] Cousin I, Nicoulland B, Coutandeur C. Influence of rock fragment on the water retention and water percolation in a calcareous soil[J]. Catena, 2003, 53, 97~114
[80] Rawls W J, Brakensiek D L, Sinmanton J R, et al. Predication of soil cover and soil rock for rangeland infiltration[J]. Range Manage, 1988, 41(4), 307~308
[81]邵明安,王全久,黄明斌。土壤物理学[M]。北京:高等教育出版社,2006。
[82]周蓓蓓,邵明安。土石混合介质饱和导水率的研究[J].水土保持学报,2006,20(6):62-66。
[83] Cousin I N, coullaud B, Coutadeur C.Influence of rock fragments on the water retention and water percolation in a calcareous soil[J]. Catena, 2003,53:97-114
[84] Dadkhah M, Gifford G F.Influence of vegetation,rock cover and trampling on infiltration rates and sediment production[J].Water Resourc.Bull.,1980,16:979-986.
[85]朱元俊。黄土区土石混合介质中水分运动及有效性研究[D].博士论文,北京:中国科学院地理科学与资源研究所,2007.
[86] Zhou Beibei,Shao Ming’an. Effects of the rock fragments on water movement and solute transport in a Loess Plateau soil[J].C.R.Geoscience.(SCI) ,2009,3.
[87]张绍良.矿区煤矸石充填相关问题研究[D].中国矿业大学硕士论文, 1992.
[88]段永红,赵景逵.煤矸石山浅层水分含量的测定方法与水分状况模式初探[A] .矿山废地复垦与绿化[M] .北京:中国林业出版社, 1995. 40～44
[89] Van Wesemael B, Poesen J, Kosmas C S and et al. The role of rock fragments in evaporation form cultivated soils under Mediterranean climatic conditions[J].Phys, Chem.Earth.1995,20(3):293-299
[90] Cousin I, Nicoulland B, Coutandeur C. Influence of rock fragment on the water retention and water percolation in a calcareous soil[J]. Catena, 2003, 53, 97~114
[91] Rawls W J, Brakensiek D L, Sinmanton J R and et al. Predication of soil cover and soil rock for rangeland infiltration[J]. Range Manage, 1988, 41(4), 307~308
[92] Gupta V K. Fundamental problems in the stochastic convection-dispersion model of solute transport in aquifers and field soils [J]. Water Res Res, 1986, 22(1): 77- 88
[93] Tang D H, Frind E O. Contaminant transport in fractured porous media: analytical solution for a single fracture [J]. Water Res Res, 1981, 17(3):555- 564
[94] Lapidus L, Amundson N R. Mathematics of adsorption in beds [J]. J. Phys. Chem. 1952,56:584
[95]Van Genuchten M Th, Wagenet R J. Two-site/two-region models for pesticide transport and degradation: theoretical development and analytical solutions[J].Soil Sci. Soc. Am. J.,1989,53:1303-1310
[96]李韵株,李保国土壤溶质运移[M]北京:科学出版社1998, 9:129
[97]Bear J. Dynamics of fluids in porous media [M].Elservier, New York,1973.
[98]Bear J. Hydraulics of Groundwater [M].McGraw-Hill, New York,1979.
[99] Elprince A M , et al.Fitting solute breakthrough equations to data using two adjustable parameters[J].Soil Sci.Soc.Am.J.1977,(41):39-41
[100]DeSmedt F and P J Wierenga,1984.Dead-end pore volume and dispersion in porous media[J].Soc.Pet.Eng.J.4:73-84.
[101]Wierenga P J, Solute transport through soils[J].Mobile-immobile water concept,1982,272-278.
[102] Buchter B C. Heterogeneous flow and solute transport in an unsaturated stony soil monolith[J].Soil Sci.Soc.Am.J.1995,(59):14-21.
[103]Nkedi-Kizza P.Modeling trium and chloride transport through an aggregated oxisol[J].Water Resour.Res.1983,(19):691-700.
[104] Logsdon S D, Jaynes D B. M ethodo logy fo r determ ininghydraulic conduct ivity w ith tension infilt rometers[J ]. So ilSci Soc Am J , 1993, 57: 1426- 1431.
[105]Liu Z G, Ma X H. Effect of reclamation on soilenvironment in Sanjiang plain[J]. Pedosphere, 1997, 7 (1): 73-78
[106] McCormack DE, Carlson C L. Formulation of soilreconstruction and productivity standards. In: Carlson,Sarisher. eds. Innovative approaches to mined land reclamation[M]. Southern Illinois University Press, 1986, 19 -30
[107] National Resources Council. Surface mining: soil, coal and society[M]. Washington DC: National Academy Press, 1981.
[108]胡振琪.煤矿山复垦土壤剖面重构的基本原理与方法[J].煤炭学报, 1997, (6): 617 -618.
[109]胡振琪.,魏忠义,秦萍。矿山复垦土壤重构的概念与方法[J].土壤,2005(1):8-12.
[110]许明祥,刘国彬,卜崇峰等。圆盘入渗仪法测定不同利用方式土壤渗透性试验研究[J],农业工程学报,2007,18(4):54-58.
[111]李志强,曹永新,李伟光等,安家岭露天排土场复垦适宜性评价与效益分析[J].露天采矿技术,2007,2,58-60.
[112]白中科,赵景魁,李晋川等.大型露天煤矿生态系统受损研究-以平朔露天煤矿为例[J].生态学报,1999,19(6),870-875.
[113]杨文治,邵明安.黄土高原土壤水分的研究[M].北京:科学出版社,2000.173-196.
[114]李毅,邵明安.娄土坡面降雨水沙运移实验研究[J].水土保持学报,2007,21(4),29-33.
[115]雷志栋,杨诗秀,谢森传.土壤水动力学[M].北京:清华大学出版社,1988:78-79.
[2]马东豪.黄土区土石混合介质水分运动试验研究及数值模拟[D].博士论文,北京:中国科学院地理科学与资源研究所,2008.
[3] Meyer L D,Johnson C B,Foster G R.Stone and woodchip mulches for erosion control on construction sites[J]. Journal of Soil and Water Conservation,1972,27:264～269
[4]符素华.土壤中砾石存在对入渗影响研究进展[J].水土保持学报,2005,19(1):171～175.
[5] Posesen J, Lavee H. Rock fragments in top soils: significance and processes[J].Catena,1994, 23:1-28
[6] CoileT S.Moisture content of small stone in soil[J]. Soil Sci.1953,75:203-207
[7]吕国安,陈明亮,王春潮。丹江口库区石渣土土壤水分特性研究[J].华中农业大学学报,2000,19(4):342-345.
[8]侯庆春.神木试区自然条件及环境整治综合分析[A].中国科学院水利部西北水土保持研究所集刊, 1993, 18: 136-144.,
[9]贾恒义,雍少萍,王富乾.神木试区的土壤资源[A].中国科学院水利部西北水土保持研究所集刊, 1993, 18: 36-46.
[10]唐克丽,侯庆春,王斌科,张平仓.黄土高原水蚀风蚀交错带和神木试区的环境背景及整治方法[A].中国科学院水利部西北水土保持研究所集刊, 1993, 18: 2-15.
[11] Ugolini F C, Corti G, Agnelli A 1,et al. Mineralogical, Physical, and Chemical properties of rock fragments in soil[J]. Soil Sci. 1996,161(8):521-542, August.
[12] Williams R D, Schuman G E. Reclaiming mine soils and overburned in western United States, analytic parameters and procedures[C].Soil Conser Soc of Amer, 1987, 259-282.
[13]Wesemael B V,Poesen J, de Figueriedo T. Effect of rock fragments on physical degradationof cultivatied soils by rainfall[J].Soil and Till Res,1995,33(3):229-250.
[14] Sauer Th J, Logsdon S D. Hydraulic and physical properties of stony soils in a small watershed[J].Soil Sci. Soc. Am. J 2002,66:1947-1956
[15] PoesenJ. Surface sealing as influenced by slope angle and position of simulated stones in the top layer of loose sediments[J]. Earth Surf.Process.Landforms,1986,11:1-10
[16] Corti G, Ugolini F C, Agnelli A et al .The soil skeleton, a forgotten pool of carbon and nitrogen in soil[J]. Euro J .Soil Sci, 2002,53(2 ) :283-288.
[17] Flint AL, Childs S.Development and calibration of an irregular hole bulk density sampler[J]. Soil Sci. Soc. Am. 1984, 48:374-378
[18] Ravina, I.; Magier,J., Hydraulic conductivity and water retention of clay soils containing rock fragments[J]. Soil Sci. Soc. Am. J. 1984, 48:736-740
[19]王慧芳.黄土高原土石混合介质水分溶质运移试验研究[D].博士论文,陕西:中国科学院水土保持研究所,2007.
[20] Corti G, Ugolini F C, Agnelli A et al. The soil skeleton, a forgotten pool of carbon and nitrogen in soil[J]. European Journal of Soil Science 2002,53(2 ) :283-288.
[21] Posesen J,Lavee,H. Rock fragments in top soils: significance and processes[J]. Catena,1994, 23:1-28
[22] Meyer L D, Johnson C B, Foster G R. Stone and woodchip mulches forerosion control on constructionsites[J].Soil Water Conser.,1972,27:246-269
[23] Brakensiek D L, RawlsW J, Stephenson G R. A note on determining soil properties for soils containing rock fragments, [J] J .RangManage,1986a,50(3):408-409
[24] Shipp R F, Matelski R P. Bulk-density and coarse-fragment determinations on some pennsylvania soils[J].Soil Sci.1965,99:392-397
[25] Torri D,Poesen J.Monaci F,Busoni E.Rock fragment content and fine soil bulk density[J].Catena,1994,23:65-71·
[26] Cerda,A. Effects of rock fragment cover on soil infiltration, interrill runoff and erosion[J]. European J.of Soil Sci.2001,52:59-68
[27] ReinhartK. The problem of stones in soil-moisture measurements[J]. Soil Sci.Soc.Am.Proc. 1961, 25:268-270
[28] Epstein E, Grant W J and Struchtemeyer R A. Effects of stone on runoff,erosion and soil moisture[J]. Soil Sci. Soc. Proc: 1966,638-640.
[29] Petersen G W ,Cunningham R L,Matelski R P. Moisture characteristic of Pennsylvania soils:II.Soil factors affecting moisture retention within a textural class-silt loam [J].Soil Sci Soc Amer Proc:1968,32(6):866-870
[30] Ingelmo F, Cuadrado S., Ibanes A and et al. Hydric properties of some Spanish soils in relation to their rock fragment content: influence for runoff and vegetation In: Poesen, J.; 32 Lavee ,H (Editors)Rock fragment content: surface dynamics[J]. Catena,1994,23;73-85
[31] Poesen J.Surface sealing as influenced by slope angle and position of simulated stones in the top layer of loose sediments [J].Earth Surf.Proc.Landforms,1986,11:1-10
[32] Box J E.The effects of surface slaty fragments on soil erosion by water[J].Soil Sci.Soc.Am.J,1981,45:111-116
[33] Valentin C,Casenave A, Infiltration into sealed soils as influenced by gravel cover[J]. Soil Sci. Soc. Am.J. 1992, 56:1667-1673
[34] Wilcox B P,Wood M K.Factors influencing interrill erosion from semiarid slopes in New Mexico[J].J . Range Management. l988,42:66-70.
[35] Abrahams A D, Parsons A J. Relation between infiltration and stone cover on a semiarid hillslope .southern Arizona [J]. J.Hydrol.1991,122:49-59
[36] Poesen J; Torri.D Mechanisms governing incipient motion of ellipsoidal rock fragments in concentrated overland flow[J].Earth Surf, Process Landforms 1989,14:469480
[37] Peck A J, Watson,J.D.Hydraulic conductivity and flow in non-uniform soil. In:Workshop on Soil Physics and Field heterogeneity CSIRO Div. of Environmental Mechanics[R].Canberra,1979,31-39
[38] Flint A L, Childs S. Development and Calibration of an Irregular Hole Bulk Density Sampler[J]. Soil Sci. Soc. Am.J,1984, 48:374-378
[39] Brakensiek D L,Rawls W J. Soil containing rock fragments: effects on infiltration[J]. Catena, 1994,23:99-110
[40] Bouwer H, Rice R C. Hydraulic properties of stony vadose zones[J]. Ground Water, 1984, 22(6) 696-705
[42] Mehuys G R, Stolzy L H, Levey J and et al. Effects of stones on the hydraulic conductivity of relatively dry desert soils[J]. Soi Sci. Am.Proc.1975, 39:37-42
[43] Corey A T, Kemper W D. Conservation of soil water by gravel mulches[D].Hydrology papers no. 30.Colorado State University, Fort Collins, 1986, 23
[44] Marion G M, Kummerow J, Miller P C.Predicting nitrogen mineralization in chaparral soils[J]. Soil Sci. Am. J., 1981, 45: 956-961.
[45] Gleason K J, Krantz W B,Caine N.,George S H and et al. Geometrical aspects of sorted patterned ground in recurrently frozen soil[J]. Scicence, 1986, 232: 216-220.
[46] Govers G, Poesen J. Field experiments on the transport of rock fragments by animal trampling on scree slopes[J]. Geomorphology, 1998, 23, 193– 203.
[47] Govers G,Vandaele K,Desmet P and et al. The role of tillage in soil distribution on hill slopes [J]. Eur. J. Soil Sci., 1994, 45: 469-478.
[48] Kemper W D,Nick A D,Corey A T.Accumulation of water in soils under gravel and sand mulches[J].Soil Sci. Soc. Am. J, 1994,58:56-63
[49]许秀元,陈同斌.土壤中溶质运移模拟的理论与应用[J].地理研究.1998, 17(1),23-28.
[50]李学恒.土壤化学[M].北京:高等教育出社.2001,151-225
[51]石元舂,等.盐渍土的水盐运动[M].北京:北京农业大学出版社,1986.
[52]李韵珠,李保国.土壤溶质运移[M],北京:科学出版社。1998
[53] Russo D. Leaching characteristics of a stony desert soil[J].Soil Sic. Soc. Am. J 1983, 47:431-438
[54] Schulin R, Wierenga P J ,et al. Solute transport through a stony soil[J]. Soil Sci. Soc. Am. J. 1987,51:36-42
[55] Buchter B, Hinz C, Feller M G and et al. Heterogeneous flow and solute transport in an unsaturated stony soil monolith[J]. Soil Sci. Soc. Am.J 1995,59:14-21
[56]Buchter B, Hinz C,Feller M G and et al. Cadmium Transport in an unsaturated stony sub soil monolith[J]. Soil Sci.Soc.Am.J. 1996, 60:716-721
[57]康世永.马家塔露天矿土地复垦方式的探讨[J].露天采煤技术, 1998, 2: 48-49.
[58] Meyer L D,Johnson C B,Foster G R.Stone and woodchip mulches for erosion control on construction sites [J].J. Soil Water Conser,1972,27:264～269
[59]Grant W J,Struchtemeyer R A.Effect of stones on runoff, erosion,and soil moisture[J]. Soil Sci. Soc. Amer. Proc.,1966,30:638～640
[60] Reigner I C, Phillips J J. Variations in bulk density and moisture content within two new Jersey coastal plain soils, Lakeland and Lakehurst sands[J]. Soil Sci. Soc.Amer. Proc, 1964, 28: 287～289
[61]符素华,段淑怀,刘宝元.密云石匣小流域土地利用对土壤粗化的影响[J].地理研究,2001,20(6):697—702.
[62] Grant R, Struchtemeyer R A.Influnce of coarse fraction in two Marine potato soils on infiltration,runoff and erosion[J].Soil Sci Soc of Amer Proc,1959,23: 391-394
[63]Abrahams A D, Parsons A J. Hydraulic of interrill overland flow on stone-covered desert surfaces[J]. Catena, 1994, 23: 111-140
[64] Valentin C. Surface sealing as affected by various rock fragment covers in West Africa[J]. Catena, 1994, 23:87-97
[65] Govers G,Vandaele K,Desmet Pand et al. The role of tillage in soil distribution on hill slopes[J]. Eur. J. Soil Sci., 1994, 45: 469-478.
[66]邵明安.非饱和土壤导水参数的推求[A].1:理论.中国科学院西北水土保持研究所集刊,1991,13:13～25.
[67]周蓓蓓,邵明安。不同碎石含量及直径对土壤水分入渗的影响[J].土壤学报,44(2007) 801-801.
[68] Wilcox B P, Wood M K, Tromble J M. Factors influencing infiltrability of semiarid mountain slopes[J]. J.Range Manage, 1988, 41(3), 197~206
[69]Reigner I C, Phillips J J. Variations in bulk density and moisture content within two new Jersey coastal plain soils, Lakeland and Lakehurst sands[J]. Soil Sci. Soc.Amer. Proc, 1964, 28: 287～289
[70] Grant R, Struchtemeyer R A.Influnce of coarse fraction in two Marine potato soils on infiltration,runoff and erosion[J].Soil Sci Soc Amer Proc,1959,23: 391～394
[71] Valentin C. Surface sealing as affected by variousrock fragment covers in West Africa[J]. Catena, 1994, 23:87～97
[72]张信宝,安芷生.黄土高原地区森林与黄土厚度的关系[J].水土保持通报,1994,14(6):1～3.
[73]王全久,邵明安.非饱和土壤导水特性分析[J].土壤侵蚀与水土保持学报,1998,4(6): 16～22.
[74]刘建国,王洪涛,聂永丰.多孔介质非饱和导水率预测的分型模型[J].水科学进展,2004, 15(3):269～275.
[75] Mehuys G R, Stolzy L H, Letey J, et al. Effect of stones on the hydraulic conductivity of relatively dry desert soils[J]. Soil Sci. Soc. Amer. Proc., 1975, 39: 37～42
[76]Wilcox B P, Wood M K, Tromble J M. Factors influencing infiltrability of semiarid mountain slopes[J]. Range Manage, 1988, 41(3), 197~206
[77]Bodman C B, Coleman E A. Moisture and energy conduction during down-ward entry of water into soil[J]. Soil Sci.Soc.Am.J,1944,2(8),166～182
[78]邹焱,陈洪松,苏以荣,邵明安.红壤积水入渗及土壤水分再分布规律室内模拟试验研究[J].水土保持学报,2005,19(3),174～177.
[79] Cousin I, Nicoulland B, Coutandeur C. Influence of rock fragment on the water retention and water percolation in a calcareous soil[J]. Catena, 2003, 53, 97~114
[80] Rawls W J, Brakensiek D L, Sinmanton J R, et al. Predication of soil cover and soil rock for rangeland infiltration[J]. Range Manage, 1988, 41(4), 307~308
[81]邵明安,王全久,黄明斌。土壤物理学[M]。北京:高等教育出版社,2006。
[82]周蓓蓓,邵明安。土石混合介质饱和导水率的研究[J].水土保持学报,2006,20(6):62-66。
[83] Cousin I N, coullaud B, Coutadeur C.Influence of rock fragments on the water retention and water percolation in a calcareous soil[J]. Catena, 2003,53:97-114
[84] Dadkhah M, Gifford G F.Influence of vegetation,rock cover and trampling on infiltration rates and sediment production[J].Water Resourc.Bull.,1980,16:979-986.
[85]朱元俊。黄土区土石混合介质中水分运动及有效性研究[D].博士论文,北京:中国科学院地理科学与资源研究所,2007.
[86] Zhou Beibei,Shao Ming’an. Effects of the rock fragments on water movement and solute transport in a Loess Plateau soil[J].C.R.Geoscience.(SCI) ,2009,3.
[87]张绍良.矿区煤矸石充填相关问题研究[D].中国矿业大学硕士论文, 1992.
[88]段永红,赵景逵.煤矸石山浅层水分含量的测定方法与水分状况模式初探[A] .矿山废地复垦与绿化[M] .北京:中国林业出版社, 1995. 40～44
[89] Van Wesemael B, Poesen J, Kosmas C S and et al. The role of rock fragments in evaporation form cultivated soils under Mediterranean climatic conditions[J].Phys, Chem.Earth.1995,20(3):293-299
[90] Cousin I, Nicoulland B, Coutandeur C. Influence of rock fragment on the water retention and water percolation in a calcareous soil[J]. Catena, 2003, 53, 97~114
[91] Rawls W J, Brakensiek D L, Sinmanton J R and et al. Predication of soil cover and soil rock for rangeland infiltration[J]. Range Manage, 1988, 41(4), 307~308
[92] Gupta V K. Fundamental problems in the stochastic convection-dispersion model of solute transport in aquifers and field soils [J]. Water Res Res, 1986, 22(1): 77- 88
[93] Tang D H, Frind E O. Contaminant transport in fractured porous media: analytical solution for a single fracture [J]. Water Res Res, 1981, 17(3):555- 564
[94] Lapidus L, Amundson N R. Mathematics of adsorption in beds [J]. J. Phys. Chem. 1952,56:584
[95]Van Genuchten M Th, Wagenet R J. Two-site/two-region models for pesticide transport and degradation: theoretical development and analytical solutions[J].Soil Sci. Soc. Am. J.,1989,53:1303-1310
[96]李韵株,李保国土壤溶质运移[M]北京:科学出版社1998, 9:129
[97]Bear J. Dynamics of fluids in porous media [M].Elservier, New York,1973.
[98]Bear J. Hydraulics of Groundwater [M].McGraw-Hill, New York,1979.
[99] Elprince A M , et al.Fitting solute breakthrough equations to data using two adjustable parameters[J].Soil Sci.Soc.Am.J.1977,(41):39-41
[100]DeSmedt F and P J Wierenga,1984.Dead-end pore volume and dispersion in porous media[J].Soc.Pet.Eng.J.4:73-84.
[101]Wierenga P J, Solute transport through soils[J].Mobile-immobile water concept,1982,272-278.
[102] Buchter B C. Heterogeneous flow and solute transport in an unsaturated stony soil monolith[J].Soil Sci.Soc.Am.J.1995,(59):14-21.
[103]Nkedi-Kizza P.Modeling trium and chloride transport through an aggregated oxisol[J].Water Resour.Res.1983,(19):691-700.
[104] Logsdon S D, Jaynes D B. M ethodo logy fo r determ ininghydraulic conduct ivity w ith tension infilt rometers[J ]. So ilSci Soc Am J , 1993, 57: 1426- 1431.
[105]Liu Z G, Ma X H. Effect of reclamation on soilenvironment in Sanjiang plain[J]. Pedosphere, 1997, 7 (1): 73-78
[106] McCormack DE, Carlson C L. Formulation of soilreconstruction and productivity standards. In: Carlson,Sarisher. eds. Innovative approaches to mined land reclamation[M]. Southern Illinois University Press, 1986, 19 -30
[107] National Resources Council. Surface mining: soil, coal and society[M]. Washington DC: National Academy Press, 1981.
[108]胡振琪.煤矿山复垦土壤剖面重构的基本原理与方法[J].煤炭学报, 1997, (6): 617 -618.
[109]胡振琪.,魏忠义,秦萍。矿山复垦土壤重构的概念与方法[J].土壤,2005(1):8-12.
[110]许明祥,刘国彬,卜崇峰等。圆盘入渗仪法测定不同利用方式土壤渗透性试验研究[J],农业工程学报,2007,18(4):54-58.
[111]李志强,曹永新,李伟光等,安家岭露天排土场复垦适宜性评价与效益分析[J].露天采矿技术,2007,2,58-60.
[112]白中科,赵景魁,李晋川等.大型露天煤矿生态系统受损研究-以平朔露天煤矿为例[J].生态学报,1999,19(6),870-875.
[113]杨文治,邵明安.黄土高原土壤水分的研究[M].北京:科学出版社,2000.173-196.
[114]李毅,邵明安.娄土坡面降雨水沙运移实验研究[J].水土保持学报,2007,21(4),29-33.
[115]雷志栋,杨诗秀,谢森传.土壤水动力学[M].北京:清华大学出版社,1988:78-79.