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    地下水流动对砷迁移的影响: 大同盆地试验场的观测与模拟

    余倩 谢先军 马瑞 吴亚 李俊霞 王焰新

    余倩, 谢先军, 马瑞, 吴亚, 李俊霞, 王焰新, 2013. 地下水流动对砷迁移的影响: 大同盆地试验场的观测与模拟. 地球科学, 38(4): 877-886. doi: 10.3799/dqkx.2013.086
    引用本文: 余倩, 谢先军, 马瑞, 吴亚, 李俊霞, 王焰新, 2013. 地下水流动对砷迁移的影响: 大同盆地试验场的观测与模拟. 地球科学, 38(4): 877-886. doi: 10.3799/dqkx.2013.086
    YU Qian, XIE Xian-jun, MA Rui, WU Ya, LI Jun-xia, WANG Yan-xin, 2013. Impact of Groundwater Flow on Arsenic Transport: A Field Observation and Simulation in Datong Basin. Earth Science, 38(4): 877-886. doi: 10.3799/dqkx.2013.086
    Citation: YU Qian, XIE Xian-jun, MA Rui, WU Ya, LI Jun-xia, WANG Yan-xin, 2013. Impact of Groundwater Flow on Arsenic Transport: A Field Observation and Simulation in Datong Basin. Earth Science, 38(4): 877-886. doi: 10.3799/dqkx.2013.086

    地下水流动对砷迁移的影响: 大同盆地试验场的观测与模拟

    doi: 10.3799/dqkx.2013.086
    基金项目: 

    国家自然科学基金重点项目 40830748

    详细信息
      作者简介:

      余倩(1986-), 女, 博士研究生, 地下水科学与工程专业.E-mail: yuqian308@126.com

      通讯作者:

      王焰新, E-mail: yx.wang@cug.edu.cn

    • 中图分类号: X141

    Impact of Groundwater Flow on Arsenic Transport: A Field Observation and Simulation in Datong Basin

    • 摘要: 地下水流动特征对水文地球化学特征具有重要控制作用, 研究分析了大同盆地地下水流动特征对高砷水迁移的影响.以山阴县桑干河南岸地下水试验场(SYFS)的监测数据为基础, 建立了河岸带三维非稳定地下水流模型.结果表明, 灌溉在很大程度上影响着地下水位动态变化.灌溉活动减慢了地下水埋深和水平地下水流速, 加速了不同岩性地层之间的垂向水量交换.粉土(L1、L2、L3和L4)、粘土1(L5)和砂1(L6)之间始终存在由上至下的垂向水量交换, 粘土2(L7)、砂2(L8)、粘土3(L9)和砂3(L10)以水平水量交换为主.灌溉水和大气降水从地表向下垂直入渗至含水层的过程中, 推动了地表和包气带沉积物中的砷逐渐向下迁移; 到达含水层后, 水平交换量占主导, 地下水在水平方向上频繁的水量交换促使As在含水层中发生水平迁移.

       

    • 图  1  (a) 山阴试验场平面图和监测井;(b)穿过桑干河的地层剖面;(c)平行桑干河的地层平面

      Fig.  1.  (a) Plan view of the SY field site and the experimental wells; (b) Hydrogeologic cross section across Sanggan river; (c) Hydrogeologic cross section paralle Sanggan river

      图  2  (a) 2011年5月份试验场地地下水位等值线图;(b)地下水位随时间的波动,well1-2, well 2-2, well 3-2, well 4-2, well5-2

      Fig.  2.  (a) Contour map of water level observed in May 2011; (b) Temporal change of water level at well 1-2, well 2-2, well 3-2, well 4-2 and well 5-2, respectively

      图  3  模拟区概化

      a为平面示意;b为剖面示意

      Fig.  3.  Model domain

      图  4  模型校正结果(S、M、D分别代表浅层、中层和深层监测井)

      Fig.  4.  Model calibrations results to the tube wells

      图  5  2011年2月—2011年11月间地面以下13m深度处的水平地下水流速特征

      Fig.  5.  Horizontal groundwater flow velocities simulated at z=-13m from February to November, 2011

      图  6  (a) L1~L6各层之间垂向地下水流净交换量(正值表示方向垂直向下);(b)X=17.5m和X=57.5m位置处,L6~L10各层之间水平地下水流净交换量(正值表示交换量方向由A'到A,负值表示由AA')

      Fig.  6.  (a) Net vertical groundwater flux between L1-L6 (the positive values indicate movement downwards through the model layers); (b) Net horizontal groundwater flux at AA' profile from L6 to L10 with X=17.5m and X=57.7m, respectively

      图  7  AA'剖面地下水砷含量的分布特征(实线箭头示意地下水流向,垂向坐标轴放大两倍)

      Fig.  7.  Simulated flow field overlain with As concentration. As concentrations are shown as shaded counters, and values in parentheses indicate range of intervals

      表  1  地下水流模型中的水力学参数

      Table  1.   Hydraulic properties of aquifers used in model simulations

      水力传导系数K(m/d)a 单位储水系数Ssb 单位给水度Sya 有效孔隙度a 总孔隙度a
      粉土 0.5 1E-4 0.16 0.22 0.35
      粘土 8.64E-4 5E-4 0.01 0.2 0.45
      15 1E-4 0.22 0.25 0.25
      a.据Fetter, 1994;b.据Thangarajan et al., 1999.
      下载: 导出CSV
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    • 收稿日期:  2012-11-02
    • 刊出日期:  2013-07-01

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