Distribution Coefficient of Ra in Groundwater and Its Determination Technique

doi:10.19657/j.geoscience.1000-8527.2022.007

Abstract

Abstract:

In the past decade, the Ra isotope has attracted increasingly more research attention in the field of water environment and water resources. Important findings have been made on the application of Ra isotopes in estimating seabed groundwater discharge, calculating lake water balance, study of groundwater age and analysis of groundwater pollution source. This is due to the development of Ra isotope analytical technology and the enhanced understanding of Ra geochemical behavior. The Ra distribution coefficient (K_d) is a key parameter affecting the Ra migration in soil and aquifer, and its understanding is pivotal for accurate tracing of hydrological processes, especially groundwater cycle. We compiled a range of K_d value and analyzed the main influencing factors. We found that the K_d value in natural environment varies from 0.1-1×10⁶ mL·g^-1, extending across seven orders of magnitude between the maximum and minimum. The water salinity, pH, and Fe content in sediments have significant impact on K_d. The K_d determination methods were summarized and divided into four types, including the (1) “Rn” equilibrium, (2) thermodynamic adsorption equilibrium calculation, (3) experimental method, and (4) ion exchange equilibrium method. The pros and cons of each method were analyzed. We proposed the establishment of an accurate determination method of ion input recoil term in aqueous solution and to optimize analysis and calculation process, which is the technical idea of obtaining K_dvalue accurately. Our review and analysis can provide reference and technical support for studying the hydrogeochemical properties of Ra and its hydrologic applications.

Key words: distribution coefficient, radium, α-recoiled radium ion

CLC Number:

P641.3

HAO Xin, YI Lixin, LI Luxuan, YANG Yongpeng. Distribution Coefficient of Ra in Groundwater and Its Determination Technique[J]. Geoscience, 2022, 36(02): 552-562.

Figures/Tables 5

References 63

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研究者	测定方法	K_d/(mL·g^-1)	固体介质类型
Nathwani^[32]	实验法	10.1~1 779.7	粉质黏土、砂壤土、粉砂壤土、砂土
Vandenhove^[33]	实验法	12~950 000	亚黏土、砂土
Kırıs^[1]	实验法	2 185.9~7 882.9	沉积物
Vandenhove^[14]	实验法	38~446	砂土、壤土、黏土
Gonneea^[20]	实验法	210~475	砂
Rama^[14]	实验法	45	沉积物
Cable^[21]	实验法	0.15~296	石英砂
Briganti^[34]	实验法	0.1~77.9	二氧化锰、沸石、黏土、火山岩
Sun^[35]	实验法	4~85	沉积物
Krest^[36]	实验法	120~280	泥炭层沉积物
Colbert^[37]	实验法	1.2~6.4	长石、角闪石
Beck^[16]	实验法	0.1~1 535	砂
Li^[38]	实验法	235和2 100	沉积物
Kumar^[39]	实验法	1 000	砂土
Webster^[40]	离子交换法	75	高岭石、伊利石等黏土矿物
Liu^[22]	离子交换法	30~3 983	砂
谷河泉^[23]	离子交换法	24~450	粗粉砂、细砂
Urso^[28]	热动力学吸附平衡计算法	42~393	亚黏土、砂土
Krishnaswa^[41]	Rn平衡法	7 100~12 300	结晶岩和长石砂岩
Sturchio^[42]	Rn平衡法	1~10 000	碳酸盐岩
Weaver^[19]	Rn平衡法	16~160	砂岩
Stackelberg^[43]	Rn平衡法	0.2~1 200.0	砂岩和碳酸盐岩

研究者	测定方法	K_d/(mL·g^-1)	固体介质类型
Nathwani^[32]	实验法	10.1~1 779.7	粉质黏土、砂壤土、粉砂壤土、砂土
Vandenhove^[33]	实验法	12~950 000	亚黏土、砂土
Kırıs^[1]	实验法	2 185.9~7 882.9	沉积物
Vandenhove^[14]	实验法	38~446	砂土、壤土、黏土
Gonneea^[20]	实验法	210~475	砂
Rama^[14]	实验法	45	沉积物
Cable^[21]	实验法	0.15~296	石英砂
Briganti^[34]	实验法	0.1~77.9	二氧化锰、沸石、黏土、火山岩
Sun^[35]	实验法	4~85	沉积物
Krest^[36]	实验法	120~280	泥炭层沉积物
Colbert^[37]	实验法	1.2~6.4	长石、角闪石
Beck^[16]	实验法	0.1~1 535	砂
Li^[38]	实验法	235和2 100	沉积物
Kumar^[39]	实验法	1 000	砂土
Webster^[40]	离子交换法	75	高岭石、伊利石等黏土矿物
Liu^[22]	离子交换法	30~3 983	砂
谷河泉^[23]	离子交换法	24~450	粗粉砂、细砂
Urso^[28]	热动力学吸附平衡计算法	42~393	亚黏土、砂土
Krishnaswa^[41]	Rn平衡法	7 100~12 300	结晶岩和长石砂岩
Sturchio^[42]	Rn平衡法	1~10 000	碳酸盐岩
Weaver^[19]	Rn平衡法	16~160	砂岩
Stackelberg^[43]	Rn平衡法	0.2~1 200.0	砂岩和碳酸盐岩