Iodine Species and Causes of Iodine Enrichment in Saline Groundwater in Plain Area of Lower Reaches of Kashigar River
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摘要: 新疆喀什噶尔河位于典型的干旱-半干旱区，河流下游平原区地下水溶解性总固体（TDS）和碘含量异常，严重威胁当地用水安全. 以喀什噶尔河下游平原区为研究区，通过对地下水水化学特征、Cl/Br摩尔比、氢氧稳定同位素、赋存环境与水文地球化学作用的分析确定该区地下咸水中碘的分布与碘富集的影响因素. 结果表明，研究区地下水碘含量变化范围为 < 0.40~435.00 μg/L（均值为123.50 μg/L），其中潜水和承压水碘含量均值分别为58.75 μg/L和188.25 μg/L，高碘水占比分别为25.0%和75.0%，水化学类型主要为Cl·SO4型和SO4·Cl型. 地下水TDS变化范围为3 079.13~15 249.50 mg/L，主要为中性至弱碱性咸水（87.5%），其次为盐水（12.5%）. 碘元素的存在形态主要为I-（87.5%），其次为IO3-（12.5%），且无共存形态，亚氧化环境和亚还原环境分别利于碘元素以IO3-和I-形态存在. 高TDS、细粒岩性、平缓的地势、地下水浅埋条件及碱性环境均有利于地下水碘的富集. 潜水碘富集主要受蒸发浓缩作用和蒸发岩溶解作用的影响，承压水碘富集主要受还原条件下含铁矿物的溶解和冲积-湖积物的影响. Cl-与Cl/Br摩尔比值表明高碘潜水受到一定程度蒸发浓缩作用的影响.Abstract: Kashgar River in Xinjiang is located in a typical arid and semi-arid area. The abnormal contents of total dissolved solids (TDS) and iodine in groundwater in the lower reaches of the river seriously threaten the local water security. Taking the plain area in the lower reaches of Kashigar River as the study area, the distribution of iodine in saline groundwater and its influence on iodine enrichment were determined through analysis of the hydrochemical characteristics, Cl/Br mole ratio, stable isotopes of hydrogen and oxygen, occurrence environment of groundwater and hydrogeochemical process. The results showed that the iodine content of groundwater in the study area varies from < 0.40 μg/L to 435.00 μg/L (mean 123.50 μg/L). The mean iodine content of unconfined groundwater and confined groundwater is 58.75 μg/L and 188.25 μg/L, respectively, and the proportion of high iodine groundwater is 25.0% and 75.0%, respectively. The main hydrochemical types are Cl·SO4 and SO4·Cl. TDS of groundwater ranged from 3 079.13 mg/L to 15 249.50 mg/L, mainly in neutral to slightly alkaline saline groundwater (87.5%), followed by saline groundwater (12.5%). The main form of iodine is I- (87.5%), followed by IO3-(12.5%), and there is no coexistence form. The existence of iodine in IO3- and I- forms in the suboxidizing environment and the subreducing environment is favorable, respectively. High TDS, fine lithology, gentle topography, shallow burial conditions of groundwater and alkaline environment are all conducive to the accumulation of iodine in groundwater. The iodine enrichment in unconfined groundwater is mainly affected by evaporation concentration and the dissolution of evaporite, while the iodine enrichment in confined groundwater is mainly affected by the dissolution of iron-bearing minerals under reduction conditions and alluvial-lacustrine sediments. The Cl- to Cl/Br mole ratio indicates that the high iodine water in unconfined groundwater is obviously affected by evaporation.
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Key words:
- high iodine /
- Kashgar River /
- groundwater /
- saline groundwater /
- iodine species /
- hydrogeochemical process
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图 1 喀什噶尔河下游平原区地下水取样点分布（a）、水文地质图（b）及水文地质剖面图（c）
Fig. 1. Distribution of groundwater sampling sites in plain area(a), hydrogeologic (b) and hydrogeological profile(c) of lower reaches of Kashigar river
图 3 地下水碘含量与TDS（a）、碘含量与井深（b）、TDS与井深（c）的关系
Fig. 3. Relationship between iodine content and TDS (a), iodine content and well depth (b), TDS and well depth (c) of groundwater
图 5 研究区地下水碘含量与Eh(a)、pH(b)、Fe(c)、SI（菱铁矿）(d)的关系
Fig. 5. Correlation between iodine content and Eh (a), pH (b), Fe (c), Siderite SI (d) of groundwater
图 6 研究区地下水碘含量与γCa2+/γCl-的关系
Fig. 6. Correlation between iodine content and γCa2+/γCl- of groundwater
图 8 地下水Cl-和Cl/Br摩尔比
Fig. 8. Correlation between Cl- concentration and Cl/Br molar ratio of groundwater
图 11 地下水γCa2+/γNa2+和γHCO3-/γNa2+端元图
Fig. 11. End members of correlation between γCa2+/γNa2+ and γHCO3-/γNa2+ ratio in groundwater
图 12 地下水中矿物相的饱和指数随TDS的变化关系
Fig. 12. The relationship between the saturation index of mineral phase and TDS in groundwater
表 1 研究区地下水化学组分含量统计表
Table 1. Statistics of hydrogeochemical composition content in groundwater
样品编号 K1 K2 K3 K4 K5 K6 K7 K8 地下水类型 潜水 潜水 潜水 承压水 承压水 潜水 承压水 承压水 井深(m) 123 35 18 70 52 45 40 40 Eh(mV) 24.90 1.50 4.90 2.80 8.50 -11.10 1.50 -0.30 pH值 7.20 7.36 7.36 7.65 7.35 7.51 7.49 7.38 K++Na+(mg/L) 4 254.02 877.27 1 191.38 1 087.74 1 609.80 502.79 1 624.04 1 017.36 Ca2+(mg/L) 858.96 538.11 603.48 542.13 535.09 361.69 663.83 372.15 Mg2+(mg/L) 411.18 308.08 331.87 277.58 333.09 135.68 336.75 333.09 Cl-(mg/L) 5 574.51 985.51 1 683.88 1 581.07 1 648.43 566.49 2 339.70 1 403.82 SO42-(mg/L) 3 887.76 2 489.01 2 359.42 2 084.10 3 098.04 1 340.00 2 651.30 1 934.57 HCO3-(mg/L) 521.32 463.94 512.77 324.76 452.95 329.64 277.14 411.44 I(μg/L) 144.0 51.0 < 40.0 435.0 96.0 < 40.0 101.0 121.0 总Fe(mg/L) 0.25 8.25 0.89 0.19 0.32 6.82 0.32 2.11 TH(mg/L) 3 837.58 2 611.97 2 873.16 2 496.44 2 707.41 1 461.70 3 043.95 2 300.54 TDS(mg/L) 15 249.50 5 439.40 6 428.22 5 736.79 7 452.60 3 079.13 7 755.45 5 269.71 Br-(mg/L) 1.76 0.20 0.23 0.46 0.37 0.14 1.16 0.35 DOC(mg/L) 0.81 2.74 2.14 0.92 1.40 1.53 1.14 1.26 δD (‰) -47.40 -72.08 -73.30 -65.86 -74.71 -72.73 -68.94 -70.07 δ18O(‰) -6.19 -9.50 -9.76 -8.12 -10.16 -9.59 -8.70 -8.51 
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