Study on the spatial vriability of hydraulic conductivity of underground reservoir in Fuping section of Shichuan River
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摘要:
渗透系数的空间变异性研究是进行地下水库人工回灌的基础。为研究石川河富平地下水库渗透系数的空间变化规律，引入Box-Cox变换及Johnson变换对库区65组野外双环渗水试验及勘探孔数据进行预处理，并以变异函数为工具，运用传统统计学和地统计学方法分析渗透系数的空间变异性。结果表明：库区等效渗透系数变化范围为0.02~6.44 m/d，既服从对数正态分布也服从Box-Cox变换的正态分布。渗透系数空间相关程度中等，最优拟合模型为高斯模型。基于最优模型，渗透系数插值结果整体上呈现西北方向较大、东南方向较小的特点，在梅家坪镇及南社乡附近最大，范围为2.84~6.44 m/d，空间变异尺度小；在觅子乡、庄里镇附近变化明显，空间变异尺度大；在东上官乡南部最小，均小于0.2 m/d，变异尺度小。空间变异受地形、地貌、地层岩性、水文气象条件、试验点及勘探点分布、人类活动等因素的综合影响。回灌位置应选择在梅家坪镇等渗透系数大，空间变异尺度小及受人为扰动影响小的地段。研究结果可为地下水库建设提供理论参考。
Abstract:The study on the spatial variability of hydraulic conductivity is the basis for artificial recharge of groundwater reservoir. In order to study the spatial variability of the hydraulic conductivity of underground reservoirs in Fuping section of Shichuan River, Box-Cox transform and Johnson transform were introduced to preprocess the field double-loop percolation test and exploration hole data. Traditional statistical methods and geostatistical methods were applied to analyze the hydraulic conductivity of the reservoir area with the variation function as a tool. The results show that the hydraulic conductivity of the reservoir area varies from 0.02 m/d to 6.44 m/d and obeys both logarithmic normal distribution and Box-Cox transformation normal distribution, the spatial correlation of the hydraulic conductivity is medium, and the best fitting model is Gaussian model. The Kriging interpolation results based on the optimal model show that the hydraulic conductivity as a whole is larger in the northwest and smaller in the southeast. The hydraulic conductivity is the largest near Meijiaping Township and Nanshe Township, ranging from 2.84 m/d to 6.44 m/d, with small spatial variation scale. It varies significantly near Mizi Township and Zhuangli Township, with large spatial variation scale. It is the smallest in the south of Dongshangguan Township, all less than 0.2 m/d, with small variation scale. The spatial variation is influenced by the combination of topography, geomorphology, distribution of stratigraphic lithology, hydro-meteorological conditions, distribution of test sites and exploration sites, human activities and other factors. The location of recharge should be chosen in Meijiaping town and other locations with large hydraulic conductivity, small spatial variation scale and low influence by human disturbance. The research results can provide theoretical references for the construction of underground reservoirs.
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表 1 各点位岩层厚度及等效渗透系数
Table 1. Statistical results of rock thickness and hydraulic conductivity at each point
编号 岩层厚度/m 等效渗透系数/（m·d−1） 编号 岩层厚度/m 等效渗透系数/（m·d−1） 编号 岩层厚度/m 等效渗透系数/（m·d−1） S-1 41.50 1.20 S-23 38.50 0.15 11 56.20 0.56 S-2 46.00 1.26 S-24 36.00 0.34 12 52.70 0.58 S-3 39.10 5.68 S-25 24.90 0.16 13 53.30 0.90 S-4 47.20 0.93 S-26 14.80 0.02 14 59.15 1.79 S-5 54.10 1.45 S-27 17.00 0.22 15 39.00 0.39 S-6 54.70 0.62 S-28 23.50 0.37 16 31.90 0.93 S-7 44.00 1.26 S-29 21.00 0.11 17 59.70 0.29 S-8 55.10 0.48 S-30 20.20 0.14 18 31.60 0.21 S-9 54.40 0.44 S-31 15.00 0.17 19 40.60 0.37 S-10 51.30 2.90 S-32 18.00 0.10 20 57.50 0.32 S-11 52.80 1.24 S-33 36.00 0.09 21 59.00 0.51 S-12 53.80 1.07 S-34 37.20 0.06 22 56.04 0.36 S-13 53.90 3.08 1 23.80 6.44 23 56.04 0.40 S-14 44.30 0.10 2 28.80 1.54 24 65.20 0.14 S-15 52.70 2.03 3 31.00 1.12 25 63.80 0.11 S-16 53.00 2.09 4 39.60 0.50 26 15.10 0.03 S-17 46.10 2.34 5 43.50 0.11 27 26.30 0.02 S-18 38.30 5.92 6 39.00 0.17 28 36.90 0.05 S-19 38.80 0.08 7 52.20 0.15 29 48.10 0.02 S-20 42.50 1.46 8 53.20 0.56 30 39.50 0.03 S-21 44.00 0.28 9 53.10 0.81 31 41.90 0.02 S-22 32.50 0.68 10 54.20 0.15 
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表 2 变换函数类型
Table 2. Transformation function type
一般公式 分布类型 
X服从Johnson SL分布（即对数分布） 
X服从Johnson SB分布 
X服从Johnson SU分布
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表 3 变异函数理论模型
Table 3. Theoretical model of variation function
变异函数理论模型 一般公式 变程 球状模型 
a 指数模型 
3a 高斯模型 
注：C0为块金值；C表示空间变量最大的变异程度；C0+C为基台值；h为步长；a为变程，表示最大自相关距离，当距离大于a时，变量相互独立。
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