Hydrogeochemical modeling of groundwater formation mechanism at the Beishan preselected site for high-level radioactive waste disposal
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摘要:
研究地下水化学特性对于高放废物处置库选址和长期性能安全评价是十分必要的。采用水文地球化学综合分析和模拟方法，探讨了我国高放废物处置库预选区甘肃北山地区基岩裂隙水的基本化学特征、水平分带性以及不同水文地质区水化学形成机制。结果表明：区内地下水化学类型主要为Cl·SO4-Na型和SO4·Cl-Na型，pH值多在7.5～8.3之间。基岩裂隙水对岩盐、石膏、萤石、绿泥石以及长石类等矿物多处于未饱和状态，而对黏土类矿物则多处于过饱和状态。从补给区到排泄区，基岩裂隙水化学分布表现出较为明显的水平分带性。马鬃山一带是区域地下水主要补给区，地下水矿化度低，水化学组分形成主要受溶滤作用控制；沉积盆地是地下水主要排泄区，地下水矿化度高，水化学组分形成主要受蒸发作用控制；在径流区，地下水化学形成主要受岩盐、石膏等矿物的溶解控制，而碳酸盐类和硅酸盐类矿物的溶解或沉淀作用微弱。该区基岩裂隙水化学形成主要受蒸发浓缩作用及水−岩相互作用的影响和控制，该结果为高放废物处置库选址提供了地下水化学基础信息和数据。
Abstract:Objective Hydrogeochemical characteristics play a pivotal role in site selection and long-term safety assessment for high-level radioactive waste (HLW) disposal repositories.
Methods This study employs integrated hydrogeochemical analysis and modeling to investigate the basic hydrogeochemical characteristics, horizontal zoning, and formation mechanisms in different hydrogeological zones of the Beishan preselected site for HLW disposal in Gansu Province, China.
Results The results show that the predominant hydrogeochemical types were Cl·SO4-Na and SO4·Cl-Na, Province with pH values generally ranging from 7.5 to 8.3. Fractured bedrock groundwater is typically undersaturated with respect to halite, gypsum, fluorite, glauconite, and feldspar, and oversaturated with respect to clay minerals. A distinct horizontal zonation is observed in the hydrogeochemical composition from the recharge area to the discharge area. The Mazongshan region serves as the primary recharge zone, characterized by low mineralization, where hydrogeochemical composition is mainly controlled by leaching processes. The sedimentary basins act as the main discharge areas with high mineralization, where evaporation processes dominate. The water-rock interaction processes along the flow path are primarily driven by the dissolution of halite and gypsum, while the effect of carbonate and silicate dissolution or precipitation remains relatively weak.
Conclusion Overall, the hydrogeochemical formation of fractured bedrock groundwater in the Beishan area is predominantly governed by evaporation and water-rock interaction processes. This study provides fundamental hydrogeochemical data and insights to support the site selection of the HLW disposal repository.
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图 1 北山地区DEM影像和地下水位等值线图(a)、区域水文地质简图(b)及典型剖面水文地质简图(c)
Figure 1. DEM image and groundwater level contour map (a), the regional hydrogeological map (b) and the representative hydrogeological cross-section (c) of the Beishan area
图 2 典型水文地质区位置(a)及剖面水文地质简图(b～g)
Figure 2. Location of typical hydrogeological zones (a) and hydrogeological cross-section maps (b-g)
图 3 研究区不同类型地下水Piper三线图
Figure 3. Piper diagrams of different groundwater types in the study area
图 4 北山地区基岩裂隙水主要化学指标相关性矩阵图
*p≤0.05，**p≤0.01；p值为观察到当前样本数据比当前数据更极端数据的概率
Figure 4. Correlation coefficients of the main parameters of fractured bedrock groundwater in the Beishan area
图 6 基岩裂隙水中主要矿物饱和指数计算结果
Figure 6. Calculated saturation indices of major minerals in fractured bedrock groundwater
图 7 北山地区不同水文地质区典型剖面反向地球化学模拟结果
Figure 7. Inverse hydrogeochemical simulation results for representative cross-sections in different hydrogeological zones of the Beishan area
图 8 北山地区地下水化学分带特征及演化示意图（A−B剖面位置见图1b；meq/L=mmol/L×原子价）
Figure 8. Schematic of hydrogeochemical zoning characteristics and evolution of groundwater in the Beishan area
表 1 各模拟路径上地下水取样信息和水化学参数分析
Table 1. Groundwater sampling information and hydrogeochemical parameter analysis along the simulation flow path
采样点 取样深度/m F− Cl− ${\mathrm{SO}}^{2-}_4 $ Na+ K+ Mg2+ Ca2+ $ {\mathrm{HCO}}^{-}_3 $ Si Al3+ pH值 温度/℃ 岩性 质量浓度ρB/(mg·L−1) 1073 -2井2.5～5.0 0.70 179.0 171.0 154 5.79 13.7 80.7 173.0 1.867 0.00289 7.75 13.09 砂砾石 1072 泉0 0.74 236.0 255.0 222 7.65 19.3 112.0 287.0 2.800 0.00365 7.95 13.90 花岗岩 头道泉 0 0.81 480.0 519.0 463 13.50 34.1 120.0 391.0 3.733 0.00416 8.32 13.27 花岗岩 N26 2.6～30 0.76 95.4 126.3 107 2.68 10.8 52.7 176.3 2.947 0.00368 7.90 12.38 花岗岩 滴石泉 0 1.35 696.0 1291.0 703 11.70 111.0 220.0 164.0 9.671 0.00661 7.53 12.18 变质岩 BET 50 1.90 836.0 828.0 820 7.20 19.6 121.0 226.0 4.542 0.01120 7.58 11.77 花岗岩 BSQ20 10～30 3.00 1209.0 1048.0 944 12.00 48.6 286.0 109.0 5.347 0.01530 7.68 9.66 花岗岩 BSQ05 6.5～30 0.82 446.0 401.0 403 8.03 22.4 106.0 236.0 4.309 0.00345 7.83 12.60 花岗岩 金钻孔 3.6～60 1.39 498.0 539.0 490 9.24 28.5 156.0 383.0 4.395 0.01300 7.80 11.83 变质岩 老王井 65～100 0.66 386.0 496.0 466 6.48 8.1 51.9 180.0 4.072 0.01070 7.83 10.80 花岗岩 BSQ34 15～30 1.72 448.0 601.0 496 8.53 18.4 106.0 157.0 5.019 0.02560 7.71 10.42 变质岩 BS60 59～70 1.04 176.0 170.0 232 2.83 4.3 30.0 169.0 3.875 0.00318 7.98 11.43 花岗岩 BSQ36 37～60 1.40 867.0 1426.0 884 9.28 57.4 296.0 100.0 10.200 0.00898 7.52 12.81 花岗岩 
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表 2 北山地区水化学指标统计
Table 2. Statistical summary of hydrogeochemical indicators in the Beishan area
地下水类型 水质指标 最大值 最小值 平均值 标准差 偏度 变异系数/% 基岩裂隙水
(样品数N=147)ρ(Na++K+)/(mg·L−1) 19870.50 61.62 1785.27 2811.68 4.02 157.49 ρ(Ca2+)/(mg·L−1) 3002.00 29.50 315.64 366.06 3.65 115.97 ρ(Mg2+)/(mg·L−1) 1952.90 5.40 126.59 227.10 4.77 179.40 ρ(Cl−)/(mg·L−1) 39175.60 65.50 2319.26 4586.38 5.08 197.75 $\rho ({\mathrm{SO}}^{2-}_4 )/({\mathrm{mg}}\cdot{\mathrm{L}}^{-1})$ 10213.80 84.50 1635.30 1670.44 2.19 102.15 $\rho ({\mathrm{HCO}}^{-}_3 )/({\mathrm{mg}}\cdot{\mathrm{L}}^{-1}) $ 1428.40 37.60 227.94 197.52 3.30 86.65 $\rho ({\mathrm{NO}}^{-}_3 )/({\mathrm{mg}}\cdot{\mathrm{L}}^{-1}) $ 250.00 < 0.08 15.02 26.30 5.56 175.10 pH值 8.35 6.80 7.74 0.30 −0.63 3.88 ρ(TDS)/(mg·L−1) 67383.45 387.11 6312.65 9075.08 3.81 143.76 松散岩类
孔隙水
(样品数N=158)ρ(Na++K+)/(mg·L−1) 36467.00 22.26 1734.24 4406.60 6.11 254.09 ρ(Ca2+)/(mg·L−1) 1040.00 16.70 210.74 199.02 2.13 94.44 ρ(Mg2+)/(mg·L−1) 490.00 2.50 41.20 48.71 5.59 118.23 ρ(Cl−)/(mg·L−1) 25667.00 41.20 1025.09 2188.66 9.28 213.51 $\rho ({\mathrm{SO}}^{2-}_4 )/({\mathrm{mg}}\cdot{\mathrm{L}}^{-1}) $ 7192.00 43.50 1045.87 946.63 2.79 90.51 $\rho ({\mathrm{HCO}}^{-}_3 )/({\mathrm{mg}}\cdot{\mathrm{L}}^{-1}) $ 859.00 11.30 224.68 122.61 2.31 54.57 $\rho ({\mathrm{NO}}^{-}_3 )/({\mathrm{mg}}\cdot{\mathrm{L}}^{-1}) $ 138.00 < 0.08 19.18 21.84 2.10 113.87 pH值 8.58 6.71 7.76 0.30 −0.17 3.87 ρ(TDS)/(mg·L−1) 53343.52 370.02 3408.98 4724.61 7.75 138.59
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