Geochemistry and genesis of the formation water in Huagang Formation of the Tiantai Inversion Zone, the Xihu Depression of the East China Sea Basin
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摘要: 通过对西湖凹陷天台反转带花港组20口井地层水地球化学特征进行研究，进一步揭示地层水成因、来源以及保存条件。研究结果表明，花港组地层水离子组成以Cl−、Na+、Ca2+以及HCO3−为主，其中Na+和Cl−浓度与矿化度（TDS）之间呈现较好的线性关系，具有高浓缩地层水的特征。水型以氯化钙Ⅳ型和Ⅴ型为主；钠氯系数和脱硫系数均较小，远低于海水；钙镁系数高于深层水，均指示花港组地层封闭性好，处于交替停滞带，有利于油气的聚集与保存。Na+轻微亏损主要受钠长石化作用影响；Ca2+富集除了钠长石化作用外，有机质成熟过程中伴生的有机酸，对长石和含钙矿物的溶蚀作用，也促进地层水中Ca2+的富集；Mg2+亏损可能与高岭石、绿泥石以及白云岩化紧密相关。花港组地层水来源于陆相沉积水，受沉积环境、水-岩反应、蒸发浓缩作用以及流体混合作用共同控制，表现出富Ca2+，贫Mg2+，略微贫Na+的特点。Abstract: Based on the geochemical features of the formation water in Huagang Formation collected from 20 wells on the Tiantai structure of Xihu Depression, the genesis, source and preservation conditions of the formation water are discussed in this paper. The water is dominated by Cl−, Na+, Ca2+ and HCO3−. And the concentrations of Na+ and Cl− show an obvious linear relationship with TDS which suggests a kind of highly concentrated formation water. The water is mainly of types CaCl2 Ⅳ and Ⅴ. r(Na+)/r(Cl−) and 100×(rSO42−)/r(Cl−) are lower than those in seawater; while r(Ca2+)/r(Mg2+) are higher in deep water. All of these features indicate that the Huagang Formation has effective sealing capability and is deposited in an alternative stagnation zone, which is conducive as well to oil and gas accumulation and preservation. The slight loss of Na+ is mainly caused by albitization. In addition to the formation of sodium feldspar, organic acids associated with the maturation of organic matter and the dissolution of feldspar and calcium-bearing minerals, also promoted the enrichment of Ca2+ in the formation water. The deficiency of Mg2+ may be closely related to the formation of kaolinite and chlorite in addition to dolomitization. The formation water of Huagang Formation originally came from land water and therefore is controlled by sedimentary environment, water-rock reaction, evaporation and concentration and fluid mixing characterized by rich Ca2+, poor Mg2+ and slightly poor Na+.
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图 3 研究区地层水钠氯系数与矿化度关系图
Figure 3. Relationship between r（Na+）/r（Cl−） and TDS of formation water in study area
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图 4 研究区地层水r(Cl−)-TDS和r(Na+)-TDS关系图
Figure 4. r（Cl−）-TDS and r（Na+）-TDS diagrams of formation water in study area
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图 5 地层水Cl−与各种离子浓度关系图
海水蒸发线据文献[36]，海水数据据文献[37]，河水数据据文献[38]。 a. lg(Cl−)-lg(Ca2+), b.lg(Cl−)-lg(Mg2+), c.lg(Cl−)-lg(Na+)。
Figure 5. The relations of Cl− with Ca2+ , Mg2+ and Na+ in formation water
Seawater evaporation line according to literature [36], seawater data from literature [37], river water data from literature [38].
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图 6 研究区花港组砂岩铸体薄片及扫描电镜照片
a. 3 554.0 m，岩石中发育丰富斜长石；b-c. 3 884.2 m，铁白云石充填粒间孔隙，并胶结交代碎屑颗粒；d. 4 065.0 m，铁方解石充填孔隙，使粒间孔缩小甚至消失，并见铁方解石完全交代碎屑颗粒；e. 3 970.0 m，自生高岭石充填粒间孔，使粒间孔微孔化，可见长石粒内溶孔；f. 3 943.3 m，见块状钠长石表面剧烈溶蚀，并见针叶状绿泥石分布在钠长石颗粒表面产出；g. 3 860.0 m，钠长石沿解理溶蚀，粒内孔隙发育；h. 3 860.0 m，针叶状绿泥石充填钠长石粒内孔隙。
Figure 6. Casting slice and SEM images of Huagang Formation sandstone
a. 3 554.0 m, plagioclases are abundant in rocks; b-c. 3 884.2 m, ankerite fills intergranular pores, and replaced particles are cemented; d. 4 065.0 m, ferrocalcite fills pores and makes the intergranular pores shrink or even disappear, ferrocalcite completely replaced detrital particles; e. 3 970.0 m, authigenic kaolinite fills intergranular pores to make intergranular pores smaller by microporosization, feldspar interagranular dissolution pores are observed; f. 3 943.3 m, the surface of lump albite was severely dissolved, and the coniferous chlorite was distributed on the surface of albite particles; g. 3 860.0 m, albite dissolves along cleavage, intragranular pores are developed; h. 3 860.0 m, the coniferous chlorite fills the intergranular pores of albite.
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表 1 研究区地层水地化参数
Table 1 Geochemical parameters of formation water in study area
油气田 井号 层位 TDS/
(mg/L)水型 钠氯系数[r(Na+)/
r(Cl−)]脱硫酸系数[100×(rSO42−)/
r(Cl−)]钙镁系[r(Ca2 +)/
r(Mg2+)]阳离子交换系数
( IBE)δ18O‰
(VSMOW)δD‰
(VSMOW)T油气田 A1S 花港组 21 761.3 NaHCO3 0.87 0.17 12.02 0.08 −3.0 −30.6 A2 23 743.6 CaCl2 0.55 0.05 14.25 0.43 −3.4 −31.7 A4 27 058.0 CaCl2 0.44 0.26 86.53 0.55 −2.9 −30.2 A6 15 181.0 NaHCO3 0.71 0.24 591.87 0.19 −1.7 −27.8 A7S 14 437.6 NaHCO3 0.68 0.34 4.87 0.25 −3.2 −29.3 A9 25 492.0 CaCl2 0.46 0.31 154.46 0.53 −3.1 −31.4 A10 17 481.8 NaHCO3 0.72 0.50 17.19 0.20 −3.7 −28.5 C1 25 409.0 CaCl2 0.53 0.10 12.22 0.46 −3.9 −28.8 C2 9 476.4 CaCl2 0.56 0.16 29.38 0.42 −3.9 −39.0 C3 27 682.6 CaCl2 0.52 0.04 15.46 0.46 −2.6 −28.1 C4 29 182.2 CaCl2 0.51 0.05 13.08 0.47 −5.0 −30.5 C7 20 833.0 CaCl2 0.51 0.08 13.87 0.47 −4.1 −32.8 C9 25 310.9 CaCl2 0.44 0.07 22.29 0.54 −2.8 −30.7 C10 26 538.5 CaCl2 0.43 0.05 36.89 0.55 −3.0 −29.2 C11 25 972.7 CaCl2 0.47 0.13 16.70 0.51 −3.1 −30.2 C12 26 556.5 CaCl2 0.52 0.05 8.19 0.46 −2.8 −28.0 C油气田 A4H 花港组 30 649.3 CaCl2 0.52 0.05 5.35 0.45 −4.5 −40.1 A6 23 810.7 CaCl2 0.56 0.30 9.61 0.42 −5.1 −42.6 A7 13 151.3 NaHCO3 0.78 0.56 16.37 0.16 −4.0 −42.3 A8 29 482.7 CaCl2 0.53 0.05 4.98 0.45 −4.2 −38.0 
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表 2 博雅尔斯基[26]对氯化钙型水的分类
Table 2 Classification of calcium chloride type water by Burson Marsteller Chhabra
水型 r(Na+)/r(Cl−) 石油地质意义 Ⅰ型 ＞0.85 水速度大，水动力活跃；油气保存条件差，几乎不存在油气藏 Ⅱ型 0.75～0.85 沉积盆地水动力带与较稳定的静水带之间的过渡带；保存油气能力较差 Ⅲ型 0.65～0.75 水动力条件平缓，有利于保存油气；保存烃类较好的有利环境 Ⅳ型 0.50～0.65 有利于烃类聚集，封闭条件良好；烃类保存的有利地带 Ⅴ型 ＜0.50 水流慢或静止，封存的古代残余海水；烃类聚集最有希望的区域
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