Geochemical Composition and Origin Tracing of Structural Fissure and Pore Brine in Western Qaidam Basin
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摘要:
柴达木盆地西部构造裂隙孔隙卤水是我国重要的深层卤水资源之一，关于其成因争论较大. 对柴达木盆地西部碱石山、红三旱四号、鸭湖和俄博梁Ⅱ号四个地区构造裂隙孔隙卤水样品的常量、微量元素以及He、Ne、Ar同位素进行了研究. 结果表明，柴达木盆地西部构造裂隙孔隙卤水钠氯系数介于0.84~0.91，钾系数介于3.19~12.35，钾氯系数介于5.26~20.61，脱硫系数介于0.33~2.00；水化学类型在Piper图上显示为Cl-Na型；同位素中3He/4He介于0.01~0.16 Ra，40Ar/36Ar介于318~352，38Ar/36Ar介于0.182~0.193，20Ne/22Ne介于9.8~10.6，21Ne/22Ne介于0.025~0.032. 由此认为基岩山区岩石风化破碎，其盐分被地下水迁移至盆地内，经蒸发成盐、埋藏，与深部地下水发生水-岩作用，富集形成高矿化度构造裂隙孔隙卤水.
Abstract:The structural fissure and pore brine in western Qaidam Basin is the most important deep brine resources in China, and its causes have been debated over many years. In this paper, it discusses its geochemical causes by studying its major, trace element characteristics and He, Ne, Ar isotopes of the brine samples from the Jianshishan, Hongsanhan Ⅳ, Eboliang Ⅱ and Yahu areas in western Qaidam basin. It is shown that the sodium-chloride coefficients of structural fissure and pore brine in western Qaidam Basin range from 0.84 to 0.91, the potassium coefficients range from 3.19 to 12.35, the potassium-chlorine coefficients range from 5.26 to 20.61 and the desulfurization coefficients range from 0.33 to 2.00. The brine type is shown as the Cl-Na type on the Piper plot. The 3He/4He ratios range in 0.01-0.16 Ra, the 40Ar/36Ar ratios range from 318 to 352, the 38Ar/36Ar ratios range from 0.182 to 0.193, the 20Ne/22Ne ratios range from 9.8 to 10.6 and the 21Ne/22Ne ratios range from 0.025 to 0.032. Therefore, it is believed that the salt components formed by rock weathering were migrated to the basin by groundwater at first, and then evaporated into salt deposits, after being buried, the water-rock interaction occurred between these salt deposits and deep groundwater and then were enriched to form the structural fissure and pore brine with a high mineralization.
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图 1 柴达木盆地西部地质构造图与采样位置
1.山区基岩；2.拟冲断裂；3.走滑断裂；4.正断层；5.逆断层；6.性质不明断层；7.推测断层（裂）；8.背斜构造；9.山峰；10.地名；11.湖泊；12.采样钻孔位置
Fig. 1. Geological structure map and sampling location of western Qaidam Basin
图 2 柴达木盆地西部地层对比与样品采集垂向位置
1.第四系中下更新统；2.狮子沟组；3.上油砂山组；4.下油砂山组；5.上干柴沟组；6.下干柴沟组；7.粉砂粘土；8.粘土粉砂与粉砂、粉砂粘土互层；9.泥质灰岩；10.炭质泥岩；11.含石膏的泥岩；12.卤水样品采集位置；13.地质界限；14.钻孔位置
Fig. 2. Stratigraphic correlation and vertical location of sample collection in western Qaidam Basin
图 3 柴达木盆地西部构造裂隙孔隙卤水piper三线图
Fig. 3. Piper diagram of brines in structural fissure in western Qaidam Basin
图 4 柴达木盆地西部构造裂隙孔隙卤水R/Ra‒40Ar /36Ar图解
Fig. 4. R/Ra‒40Ar/36Ar diagram of pore brine in structural fissure in western Qaidam Basin
图 5 柴达木盆地西部构造裂隙孔隙卤水氖同位素组成
Fig. 5. Ne isotopic composition of brines in structural fissure in western Qaidam Basin
表 1 背斜构造区构造裂隙孔隙卤水含量(mg/L)分析结果
Table 1. Analysis results of brine content (mg/L) from structural fissure pores in anticline
采样位置 K+ Na+ Ca2+ Mg2+ C1‒ SO42‒ CO32‒ HCO3‒ Li+ B2O3 密度(g/cm3) 矿化度(g/L) 碱石1井 1 697.69 48 416.40 3 743.53 399.15 82 377.88 831.40 0.00 84.08 102.00 1 497.26 1.10 139.07 旱ZK01 1 093.49 54 630.29 7 125.17 869.52 98 435.25 652.50 0.00 19.60 49.59 829.91 1.11 164.26 鸭ZK01 357.57 36 820.83 5 339.40 774.82 68 035.67 681.59 0.00 50.02 34.96 402.73 1.07 112.47 鄂Ⅱ2井 293.32 22 436.10 2 024.58 601.31 38 538.12 1 538.03 0.00 63.65 31.65 694.20 1.05 66.19 
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表 2 背斜构造区构造裂隙孔隙卤水同位素分析结果
Table 2. Isotopic analysis results of brine from structural fissure pores in anticline
采样位置 He(10‒6) R/Ra 3He/4He 4He/20Ne Ne(10‒6) 20Ne/22Ne 21Ne/22Ne 40Ar/36Ar 38Ar/36Ar 碱石1井 507.3 0.03 4.21×10‒8 55 9.297 10.4 0.028 ‒ ‒ 旱ZK01 144.5 0.05 6.59×10‒8 11 13.623 9.8 0.032 332 0.182 鸭ZK01 41.0 0.16 2.27×10‒7 3 12.109 10.6 0.025 318 0.184 鄂Ⅱ2井 1 168.1 0.01 1.95×10‒8 904 1.292 9.8 ‒ 352 0.193
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表 3 背斜构造区构造裂隙孔隙卤水特征系数
Table 3. Characteristic coefficients of brine from structural fissure pores in anticline
采样位置 Σ盐 K×103/Σ盐 K×103/Cl Mg×102/Cl Cl×102/Σ盐 γNa/γCl SO4×102/2Cl 碱石1井 137 466.05 12.35 20.61 0.48 59.93 0.91 0.50 旱ZK01 162 806.22 6.72 11.11 0.88 60.46 0.86 0.33 鸭ZK01 112 009.89 3.19 5.26 1.14 60.74 0.84 0.50 鄂Ⅱ2井 65 431.46 4.48 7.61 1.56 58.90 0.90 2.00
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