湖南新田岩溶地下水碘分布特征及其控制因素分析

李小盼; 聂国权; 苏春田; 潘晓东

doi:10.11932/karst2023y024

湖南新田岩溶地下水碘分布特征及其控制因素分析

doi: 10.11932/karst2023y024

李小盼^{1, 2,},
聂国权^{1, 2, ,},
苏春田^{1, 2},
潘晓东^{1, 2}

1.
中国地质科学院岩溶地质研究所/自然资源部、广西岩溶动力学重点实验室/联合国教科文组织国际岩溶研究中心, 广西桂林 541004
2.
广西平果喀斯特生态系统国家野外科学观测研究站，广西平果 531406

基金项目: 广西自然科学基金项目（2022GXNSFBA035454）；中国地质调查项目（DD20160303、DD20190326）

详细信息

作者简介:
李小盼（1989－），女，助理研究员，从事岩溶水文地质环境地质研究。E-mail：lixiaopan@mail.cgs.gov.cn

通讯作者:
聂国权（1991－），男，助理研究员，从事地质构造研究。E-mail：nieguoquan@mail.cgs.gov.cn

中图分类号: P641.2
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出版历程
- 收稿日期: 2022-10-12
- 网络出版日期: 2023-11-28
- 刊出日期: 2023-11-28

Distribution characteristics of iodine in karst groundwater in Xintian county, Hunan Province and the analysis on the causes of high iodine

LI Xiaopan^{1, 2
,},
NIE Guoquan^{1, 2
, ,},
SU Chuntian^{1, 2},
PAN Xiaodong^{1, 2}

1.
Institute of Karst Geology, CAGS/ Key Laboratory of Karst Dynamics, MNR & GZAR/International Research Center on Karst under the Auspices of UNESCO, Guilin, Guangxi 541004, China
2.
Pingguo Guangxi, Karst Ecosystem, National Observation and Research Station, Pingguo, Guangxi 531406, China

摘要

摘要: 在湖南新田县部分岩溶区发现高碘地下水，威胁着周边居民的饮水安全，查明该区域地下水中碘的分布特征及其控制因素具有重要意义。采集新田县66组泉水样和45组井水样，采用水化学图解法、主成分分析法和GIS技术，分析了泉水和井水的水化学特征，查明了地下水中碘的空间分布特征，剖析了碘富集的主要控制因素。研究发现泉水与井水中碘含量分别为2.7~92.8 μg·L⁻¹和4.15~3 861 μg·L⁻¹，其中，53.3%井水样品碘含量超过《水源性高碘地区和高碘病区的划定》(GB 19380-2016)标准中的界定值100 μg·L⁻¹。受沉积环境、pH、Eh和地下水径流条件影响，高碘地下水主要沿着一条NE−SW向的河谷分布，从峰林谷地地区到地势低洼的河谷平原地带，地下水碘含量整体随着径流条件变差呈现逐渐增加的趋势。海相沉积所形成的富碘富有机质地层是高碘地下水形成的地质基础，发生有机质降解和竞争吸附的弱碱性偏还原环境是导致碘被释放到地下水中的主要因素；此外，水流滞缓的封闭地下水环境也是控制高碘地下水形成的重要因素。
- 岩溶地下水 /
- 碘 /
- 空间分布 /
- 主成分分析 /
- 控制因素
Abstract: Iodine is one of the essential trace elements for human body, which maintains the growth and normal metabolism of the organism. Iodine deficiency or excess will have different degrees of impact on human health. A large field of strontium-rich mineral water was discovered in Xintian county, Hunan Province. However, the iodine content in some strontium-rich groundwater is abnormal, threatening the drinking water safety of local residents. Therefore, it is important to find out the distribution characteristics of iodine in groundwater and the controlling factors of the formation of high iodine groundwater so as to implement the project for the safety of drinking water and to prevent endemic iodine diseases in the study area.In a hydrogeological survey, 66 groups of spring water samples and 45 groups of well water samples were collected in Xintian county to analyze their hydrochemical characteristics, identify the spatial distribution characteristics of iodine in groundwater and analyze the main factors controlling iodine content in groundwater by means of hydrochemical graphical method, principal component analysis and GIS technology. The results showed that the iodine concentration in spring water and well water ranged from 2.7 to 92.8 μg·L⁻¹ and 4.15 to 3,861 μg·L⁻¹, respectively, with the respective median value of 5.4 μg·L⁻¹ and 168 μg·L⁻¹. It can be seen that all the groundwater with high iodine was well water, and 53.3% of well water samples had iodine concentration exceeding the permitted national standard of 100 μg·L⁻¹ (GB 19380-2016). In contrast, the iodine content in spring water was relatively low, and the overall iodine-deficient groundwater was predominant. High iodine groundwater was mainly distributed along a river valley in the northeast-southwest direction. The iodine content in groundwater showed a gradual increase from the peak-forest valley to the plain area of low-lying river valley, and the hydrochemical type also changed from water with single HCO₃-Ca type to water with complex HCO₃-Na, HCO₃-Na·Ca type, etc.The marl stratum formed by marine sedimentation of Shetianqiao Formation is rich in iodine and organic matter, which provides good geological conditions for the enrichment of iodine in groundwater. The microbial degradation of organic matter occurs in the closed and partially reducible groundwater environment of the marl aquifer. CO₂ generated by organic matter decomposition exists in groundwater mainly in the form of ${\rm{HCO}}_3^{-}$, which will compete with I^- for adsorption. Meanwhile, the process of organic matter decomposition to form ${\rm{HCO}}_3^{-}$ is accompanied by the release and migration of iodine deposited on it, making the iodine content in the groundwater increases with the increase of ${\rm{HCO}}_3^{-}$ content. At the same time, the alkaline karst water environment can increase the electronegativity of organic matter surface to reduce the adsorption of iodine ions by organic matter. OH⁻ in groundwater also competes with I⁻ for adsorption, which accelerates the release and migration of adsorbed iodine into groundwater, and hence increases the iodine content. The distribution area of high iodine groundwater is located in a groundwater discharge area. It is also an area distributed with strata rich in iodine and organic matter. In this area, the sluggish groundwater flow due to flat topography, together with a relatively closed groundwater environment, further facilitates the enrichment of iodine. The strata rich in iodine and organic matter formed by marine sediments, closed and partial reduction chemical environment with karst water of weak alkalinity and sluggish groundwater runoff are the main factors controlling the formation of high iodine groundwater in the study area.
- karst groundwater /
- iodine /
- spatial distribution /
- principal component analysis /
- controlling factors

HTML

图 1 新田含水岩组与取样点分布图

Figure 1. Distribution of the Xintian water-bearing rock formation and sampling points

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图 2 新田地下水Piper三线图

Figure 2. Three-line diagram of the Xintian groundwater pipeline

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图 3 地下水碘含量分布图

Figure 3. Distribution of the groundwater iodine content

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图 4 地下水中碘含量与${\rm{HCO}}_3^{-}$关系图

Figure 4. Relationship between the iodine content in groundwater and ${\rm{HCO}}_3^{-}$

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图 5 地下水中碘含量与pH（a）、Eh（b）、${\rm{NO}}_3^{-}$（c）关系图

Figure 5. Relationship between the iodine content in groundwater and pH (a), Eh (b) and ${\rm{NO}}_3^{-}$ (c)

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表 1 研究区地下水样品水化学分析统计表

Table 1. Hydrochemical analysis of groundwater samples in the study area

参数	单位	最小值	最大值	平均值	中间值	标准差	变异系数
TDS	mg·L⁻¹	136.91	732.81	334.20	322.52	118.05	0.35
总硬度	mg·L⁻¹	65.56	612.20	271.70	254.13	88.49	0.33
Eh	mV	−96.2	123.9	47.8	64.5	50.13	1.05
pH		6.74	8.91	7.25	7.23	0.29	0.04
K⁺	mg·L⁻¹	0.06	24.00	2.11	1.13	3.44	1.63
Na⁺	mg·L⁻¹	0.28	219.72	15.61	2.29	34.76	2.23
Ca²⁺	mg·L⁻¹	14.85	159.42	89.99	85.23	28.09	0.31
Mg²⁺	mg·L⁻¹	0.94	59.05	11.40	4.94	13.39	1.17
Cl⁻	mg·L⁻¹	1.30	93.32	11.69	6.36	14.95	1.28
${\rm{SO}}_4^{2-}$	mg·L⁻¹	4.89	236.34	25.48	16.17	27.02	1.06
${\rm{HCO}}_3^{-}$	mg·L⁻¹	132.50	630.30	316.55	297.19	97.99	0.31
${\rm{NO}}_3^{-}$	mg·L⁻¹	1.78	91.12	11.76	5.51	17.02	1.45
NO$_2^{−}$	mg·L⁻¹	<0.002	8.650	0.290	<0.002	1.31	4.58
F⁻	mg·L⁻¹	0.04	3.50	0.35	0.16	0.55	1.58
TFe	mg·L⁻¹	<0.003	1.260	0.140	0.061	0.22	1.62
I⁻	ug·L⁻¹	2.7	3 861.0	116.7	12.5	401.83	3.44
COD_Mn	mg·L⁻¹	<0.50	2.29	0.53	0.54	0.53	1.00
游离CO₂	mg·L⁻¹	1.06	12.67	4.73	4.51	2.51	0.53
Sr²⁺	ug·L⁻¹	2.9	8 465.0	1 002.2	195.0	1 811.83	1.81

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表 2 新田岩溶地下水旋转因子载荷矩阵

Table 2. Rotation factor loading matrix of Xintian karst groundwater

因子	泉水			井水
因子	F₁	F₂	F₃	F₁	F₂	F₃	F₄
TDS	0.648	0.729	0.180	0.348	0.855	0.261	0.237
TH	0.444	0.857	0.085	−0.647	0.697	0.228	0.010
pH	−0.062	-0.723	−0.119	0.764	−0.092	0.102	−0.047
K⁺	0.821	0.011	0.179	−0.025	0.136	−0.001	0.887
Na⁺	0.689	0.282	0.450	0.950	0.139	0.084	0.026
Ca²⁺	0.291	0.901	0.130	-0.739	0.527	−0.364	0.075
Mg²⁺	0.545	0.116	−0.100	−0.004	0.381	0.880	−0.091
Cl⁻	0.842	0.171	0.194	−0.071	0.747	0.022	0.117
${\rm{SO}}_4^{2-}$	0.740	0.277	0.435	−0.039	0.545	0.335	0.373
${\rm{HCO}}_3^{-}$	0.071	0.960	0.023	0.534	0.606	0.321	−0.260
${\rm{NO}}_3^{-}$	0.904	−0.010	−0.031	−0.121	0.114	−0.170	0.882
F⁻	0.380	−0.017	0.809	0.844	−0.015	0.169	−0.034
I⁻	−0.043	0.466	0.789	0.829	0.191	−0.116	−0.135
Sr²⁺	−0.263	0.695	0.409	0.217	0.064	0.908	−0.077
特征值	6.749	2.813	1.292	4.675	3.603	1.892	1.156
贡献率/%	48.2	20.1	9.2	33.4	25.7	13.5	8.3
累计方差贡献率/%	48.2	68.3	77.5	33.4	59.1	72.6	80.9

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