川西中二叠统栖霞组白云岩形成机制及其与川东北下三叠统飞仙关组对比
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摘要
四川盆地西部二叠系的碳酸盐岩有良好的勘探前景，尤其是栖霞组二段的白云岩储层，是继四川盆地长兴组、飞仙关组和石炭系白云岩储层之后的勘探开发潜力储层。对于四川盆地西部下二叠统白云岩的成因，由于沉积背景总体上为海侵背景，缺乏蒸发岩沉积，与蒸发作用相关的白云岩化模式不适用，而混合水成因模式在近年来受到广泛的质疑。因此，有必要根据白云岩的特征及地质背景，研究适用于该区的白云岩成因机制，为白云岩储层分布预测提供合理的地质模型。川东北地区下三叠统飞仙关组白云岩的成因及其机制前人做了大量的工作，理论上已非常地成熟和完善。因此从川东北飞仙关组白云岩的岩石结构特征、地球化学特征、流体温度和盐度、白云岩成因机制和白云化模式与川西地区栖霞组白云岩做相应的对比，进一步说明川西栖霞组白云岩的形成机制。
前人对四川盆地基础地质工作的研究，诸如构造、沉积相、岩相古地理、成岩作用等方面的研究是我们的工作得以深入的基础。通过具体的室内外工作，从野外剖面实测、岩心观察、采样、磨样、薄片鉴定、阴极发光分析、电子探针分析、扫描电镜分析、能谱测试、碳氧同位素分析、X衍射分析、包裹体均一温度测试这些方法来获得栖霞组白云岩的岩石学及地球化学特征，并由此科学地反演白云化流体的性质及白云岩成因机制。
栖霞组白云岩类型单一，只有一种结晶白云岩，缺乏代表原始沉积的泥晶—微晶白云岩和膏盐沉积。白云岩的微量元素Mn、Fe、Sr含量的变化，相对于先驱灰岩来说表现为Mn、Fe含量增加，Sr含量降低。白云岩的Mn含量28.4~117ppm，Fe含量199.4~381.4ppm，Sr含量35.9~110.5ppm。除宏观的地表剖面和岩心常见的黄铁矿、沥青之外，借助薄片鉴定、扫描电镜、能谱测试等方法和手段，观察到栖霞组白云岩中存在较多的热液矿物，石英、萤石、伊利石、重晶石、磷灰石充填于白云石溶蚀的孔、洞中，还可见在过度白云化使岩石致密后，鞍形白云石溶蚀、破碎，又在其中沉淀方解石。栖霞组白云岩具有典型的晶面弯曲的鞍形白云石，在正交偏光下呈波状消光。且具有溶蚀、垮塌角砾化等特征，这些特征总与热液相伴。
栖霞组白云岩及伴生灰岩的δ13C（PDB）值分布在-0.66~3.84‰，白云岩的δ18O值介于-3.42~9.16‰，反映白云化的流体是海源流体。白云石基质包裹体均一温度67~243℃，鞍形白云石包裹体均一温度91~223℃，方解石包裹体均一温度54~215℃，从包裹体均一温度来看，白云石沉淀的温度至少比方解石沉淀高出10℃以上。包裹体均一温度高达243℃，远不是仅埋藏条件能够达到的温度。
据氧同位素和包裹体均一温度反演白云化流体与方解石沉淀的流体，白云石基质、孔洞白云石及鞍形白云石胶结物对应的流体的氧同位素主要在0~12‰（SMOW），少数的几个样品对应的流体氧同位素在-4~0‰（SMOW）区间，有2个样品（1个为白云石基质，另1个为鞍形白云石胶结物）投点在12~13.5%之间。对方解石的氧同位素及其包裹体均一温度投点，与白云石投点结果相似，流体的氧同位素主要投在-4~0‰（SMOW），0~8‰（SMOW），12~14.5‰（SMOW）之间，记录了50~100℃，100~170℃，190~250℃这几个沉淀期次。从反演的流体氧同位素来看，流体的盐度高于甚至远远高于同期海水。二叠纪同期海水87Sr/86Sr比值介于0.7085~0.7067之间，白云岩的87Sr/86Sr比值介于0.7076~0.7069之间，接近而略低于同期海水。热史演化记录了中、晚二叠世这一异常的热事件，在中二叠世末、晚二叠世初，大约在259Ma，古热流值达到极值,晚二叠世后热流值持续降低。白云化流体是受异常热事件“烘烤”的高温、高盐度的近同期海源流体。
结晶白云岩是川东北地区下三叠统飞仙关组的主要白云岩类型，也存在一些原始结构保存的粒屑白云岩和微晶白云岩。川东北地区白云岩具有低Mn（平均63.47ppm）、Fe含量（平均1019.67ppm），较高Sr含量（132.38ppm）。结晶白云岩具有较高的Sr含量，尤其是与其伴生的方解石胶结物具有很高的Sr含量；碳同位素接近同期海水的δ13C值；流体的氧同位素值δ18O值较高2~7‰（SMOW）；87Sr/86Sr比值高于相应的同期海水，从长兴组、飞仙关组、嘉陵江组和雷口坡组，白云岩的锶同位素比值与同期海水的锶同位素比值的差值越来越小，白云化流体逐渐趋向于完全同期的海水；包裹体均一温度较高介于85.85~142.24℃）；包裹体盐度较高（3.01~12.61%NaCl，大致是海水盐度的2倍以上）。因此，飞仙关组白云化流体是一种海源流体，来源于蒸发浓缩向下渗透回流的嘉陵江期海水，白云化时间出现在相对深埋藏条件下相对封闭的成岩系统中，是深埋藏条件下盐水的渗透机制。
Dolomite reservoir in Qixia Formation, Middle Permian, Western Sichuan Basinhas well exploration potential, cause depositional setting is marine transgression,lacking of evaporate rocks deposition, evaporation dolomitization is not applicable,while mixed water dolomitization are being questioned for the past few years. So it isnecessary to research the dolomitization mechanism and mode in this area, based onthe geological background and dolomite character. Researchers had done lots ofdetailed work about dolomite genesis and mechanism of Feixianguan Formation inNortheastern Sichuan Basin, which is approximate to technically maturation andtheoretically perfect. That’s why using dolomite of Qixia Formation contrast toFeixianguan Formation, incluing the following aspects: rock fabric, geochemicalcharacteristic, fluid inclusion homogenization temperature and salinity, dolomitegenesis and dolomitization mode, to make further explanation of dolomite genesis ofQixia Formation.
On the basis of our predecessors’ work on basic geology, such as tectonic,sedimentary facies, lithofacies paleogeography, diagenesis, etc. We gainedtremendous depth and insight form all of those work and influenced us to achievedgreat results. Using a series of methods to gain rock fabric and geochemicalcharacteristic, included field section measurement, core observation, sampling,ground sample, thin section examination, cathodoluminescence analysis, electronmicroprobe analysis, scanning electron microscopy analysis, energy spectrum analysis,carbon and oxygen isotopic analysis, x-ray diffraction analysis, fluid inclusionhomogenization temperature test, to invert dolomitization fluid and dolomite genesis.
The category of Qixia Formation dolomite is very mono, there is only one singlecrystalline dolomite, lack of micrite dolomite, and also lack of gypsum deposition.Trace element of dolomite changed contrast to pioneer limestone, showing the contentof Manganese (28.4~117ppm) and Ferrum (199.4~381.4ppm) increase, Sr(35.9~110.5ppm) decrease. Cause Pyrite and bitumen can often be seen at outcrop andcore, with the benefit of thin section examination, scanning electron microscopyanalysis, energy spectrum analysis, etc., there also have many hydrothermal mineralsdeposited in dolomite of Qixia Formation. These hydrothermal minerals includingquartz, fluorite, illite, barite and apatite filled in the corroded pores and vugs.Over-dolomitization means that the dolomite precipitated in the pores and vugs andthus made the rock more compact. After that the saddle dolomite dissolution, calciteprecipitate in the pores and vugs formed by dolomite dissolution. Dolomite of QixiaFormation has typical saddle crystal morphology and curved crystal faces, and appearwavy extinction in thin section under crossed-polarized light, also has dissolution,brecciation, all these features are associated with hydrothermal fluid.
The δ13C(PDB) of dolomite and limestone of Qixia Formation lie in the range of-0.66~3.84‰, the δ18O(PDB) of dolomite lie in the range of-3.42~9.16‰，reflectingthe fluid comes from marine. Homogenization temperature of matrix dolomite fluidinclusions show a range of67~243℃, homogenization temperature of saddle dolomitein a range of91~223℃, and the homogenization temperature of calcite in a range of54~215℃, demonstrating that the temperature dolomite precipitated higher more than10℃than calcite precipitated. And the homogenization temperature reach up to243℃,which is not only the burial condition can be reached.
Adopting oxygen isotope of minerals and the homogenization temperature offulid inclusions to invert the oxygen isotope of fluid. The δ18O of fluid correspondingwith matrix dolomite, void-filling dolomite and saddle dolomite lie in the range of0~12‰(SMOW), the δ18O of few samples’ corresponding fluid lie in the range of-4~0‰(SMOW), and there are2samples’(one is matrix dolomite, the other is saddledolomite) δ18O of fluid lie in the range of12~13.5%(SMOW). The δ18O of fulid thatcalcite precipitate lie in the range of-4~0‰(SMOW),0~8‰(SMOW),12~14.5‰(SMOW), and recorded the multi-periods of50~100℃,100~170℃,190~250℃, and the salinity of fulid is higher or much higher than the coeval seawater.The87Sr/86Sr ratios of coeval sewater in Permian lies in0.7085~0.7067, while the87Sr/86Sr ratios of dolomite of Qixia Formation lies in0.7076~0.7069and is lowerthan the coeval seawater. Thermal history recorded the temperature anomaly between Middle and Late Permian, the maximum paleo-heat flow reached in the early stage ofLate Permian at approximately259Ma, after that the paleo-heat flow decreased topresent. Meaning the dolomitization fluid mainly derived from the coeval seawaterwhich influenced by the abnormal heat.
The crystalline dolomites are the mainstream dolomite phases in FeixianguanFormation of Lower Triassic, Northeastern Sichuan Basin. And there also exist somefabric-retentive dolomitic grainstones and micritic dolomites. The dolomites inNortheastern Sichuan Basin have low manganese contents (average of63.47ppm),low Ferrum contents (average of1019.67ppm) and high strontium contents (averageof132.39ppm). The crystalline dolomite phases have high strontium contents, and theassociated calcite cements have extreme high strontium contents. The δ13C values areclose to the compositions of coeval seawater. The precipitating fluids of thesedolomite phases have the relatively high δ18O values (ranges between2to7‰;SMOW), and have the higher87Sr/86Sr ratios than the ratios of coeval seawater. Fromthe earlier Changxing Formation to the later Leikoupo Formation, the differencesbetween strontium isotope ratios of dolomites and of coeval seawater decreasedgradually. The precipitating fluids of dolomites were getting closer and closer tocoeval seawater. The homogenization temperatures of fluid inclusions in dolomitesare high (ranges from85.85to142.24℃). And the salinities of fluid inclusions indolomites are double as much as the salinity of seawater (ranges from3.01to12.61%NaCl). Thus, the dolomitizing fluid is a kind of marine-derived fluid, andoriginated from downward-migrated refluxing evaporated and concentrated seawaterof Jialingjiangian. The dolomitization occurred in a closed diagenetic system duringdeep burial, and was the product of brine infiltration during deep burial.
前人对四川盆地基础地质工作的研究，诸如构造、沉积相、岩相古地理、成岩作用等方面的研究是我们的工作得以深入的基础。通过具体的室内外工作，从野外剖面实测、岩心观察、采样、磨样、薄片鉴定、阴极发光分析、电子探针分析、扫描电镜分析、能谱测试、碳氧同位素分析、X衍射分析、包裹体均一温度测试这些方法来获得栖霞组白云岩的岩石学及地球化学特征，并由此科学地反演白云化流体的性质及白云岩成因机制。
栖霞组白云岩类型单一，只有一种结晶白云岩，缺乏代表原始沉积的泥晶—微晶白云岩和膏盐沉积。白云岩的微量元素Mn、Fe、Sr含量的变化，相对于先驱灰岩来说表现为Mn、Fe含量增加，Sr含量降低。白云岩的Mn含量28.4~117ppm，Fe含量199.4~381.4ppm，Sr含量35.9~110.5ppm。除宏观的地表剖面和岩心常见的黄铁矿、沥青之外，借助薄片鉴定、扫描电镜、能谱测试等方法和手段，观察到栖霞组白云岩中存在较多的热液矿物，石英、萤石、伊利石、重晶石、磷灰石充填于白云石溶蚀的孔、洞中，还可见在过度白云化使岩石致密后，鞍形白云石溶蚀、破碎，又在其中沉淀方解石。栖霞组白云岩具有典型的晶面弯曲的鞍形白云石，在正交偏光下呈波状消光。且具有溶蚀、垮塌角砾化等特征，这些特征总与热液相伴。
栖霞组白云岩及伴生灰岩的δ13C（PDB）值分布在-0.66~3.84‰，白云岩的δ18O值介于-3.42~9.16‰，反映白云化的流体是海源流体。白云石基质包裹体均一温度67~243℃，鞍形白云石包裹体均一温度91~223℃，方解石包裹体均一温度54~215℃，从包裹体均一温度来看，白云石沉淀的温度至少比方解石沉淀高出10℃以上。包裹体均一温度高达243℃，远不是仅埋藏条件能够达到的温度。
据氧同位素和包裹体均一温度反演白云化流体与方解石沉淀的流体，白云石基质、孔洞白云石及鞍形白云石胶结物对应的流体的氧同位素主要在0~12‰（SMOW），少数的几个样品对应的流体氧同位素在-4~0‰（SMOW）区间，有2个样品（1个为白云石基质，另1个为鞍形白云石胶结物）投点在12~13.5%之间。对方解石的氧同位素及其包裹体均一温度投点，与白云石投点结果相似，流体的氧同位素主要投在-4~0‰（SMOW），0~8‰（SMOW），12~14.5‰（SMOW）之间，记录了50~100℃，100~170℃，190~250℃这几个沉淀期次。从反演的流体氧同位素来看，流体的盐度高于甚至远远高于同期海水。二叠纪同期海水87Sr/86Sr比值介于0.7085~0.7067之间，白云岩的87Sr/86Sr比值介于0.7076~0.7069之间，接近而略低于同期海水。热史演化记录了中、晚二叠世这一异常的热事件，在中二叠世末、晚二叠世初，大约在259Ma，古热流值达到极值,晚二叠世后热流值持续降低。白云化流体是受异常热事件“烘烤”的高温、高盐度的近同期海源流体。
结晶白云岩是川东北地区下三叠统飞仙关组的主要白云岩类型，也存在一些原始结构保存的粒屑白云岩和微晶白云岩。川东北地区白云岩具有低Mn（平均63.47ppm）、Fe含量（平均1019.67ppm），较高Sr含量（132.38ppm）。结晶白云岩具有较高的Sr含量，尤其是与其伴生的方解石胶结物具有很高的Sr含量；碳同位素接近同期海水的δ13C值；流体的氧同位素值δ18O值较高2~7‰（SMOW）；87Sr/86Sr比值高于相应的同期海水，从长兴组、飞仙关组、嘉陵江组和雷口坡组，白云岩的锶同位素比值与同期海水的锶同位素比值的差值越来越小，白云化流体逐渐趋向于完全同期的海水；包裹体均一温度较高介于85.85~142.24℃）；包裹体盐度较高（3.01~12.61%NaCl，大致是海水盐度的2倍以上）。因此，飞仙关组白云化流体是一种海源流体，来源于蒸发浓缩向下渗透回流的嘉陵江期海水，白云化时间出现在相对深埋藏条件下相对封闭的成岩系统中，是深埋藏条件下盐水的渗透机制。
Dolomite reservoir in Qixia Formation, Middle Permian, Western Sichuan Basinhas well exploration potential, cause depositional setting is marine transgression,lacking of evaporate rocks deposition, evaporation dolomitization is not applicable,while mixed water dolomitization are being questioned for the past few years. So it isnecessary to research the dolomitization mechanism and mode in this area, based onthe geological background and dolomite character. Researchers had done lots ofdetailed work about dolomite genesis and mechanism of Feixianguan Formation inNortheastern Sichuan Basin, which is approximate to technically maturation andtheoretically perfect. That’s why using dolomite of Qixia Formation contrast toFeixianguan Formation, incluing the following aspects: rock fabric, geochemicalcharacteristic, fluid inclusion homogenization temperature and salinity, dolomitegenesis and dolomitization mode, to make further explanation of dolomite genesis ofQixia Formation.
On the basis of our predecessors’ work on basic geology, such as tectonic,sedimentary facies, lithofacies paleogeography, diagenesis, etc. We gainedtremendous depth and insight form all of those work and influenced us to achievedgreat results. Using a series of methods to gain rock fabric and geochemicalcharacteristic, included field section measurement, core observation, sampling,ground sample, thin section examination, cathodoluminescence analysis, electronmicroprobe analysis, scanning electron microscopy analysis, energy spectrum analysis,carbon and oxygen isotopic analysis, x-ray diffraction analysis, fluid inclusionhomogenization temperature test, to invert dolomitization fluid and dolomite genesis.
The category of Qixia Formation dolomite is very mono, there is only one singlecrystalline dolomite, lack of micrite dolomite, and also lack of gypsum deposition.Trace element of dolomite changed contrast to pioneer limestone, showing the contentof Manganese (28.4~117ppm) and Ferrum (199.4~381.4ppm) increase, Sr(35.9~110.5ppm) decrease. Cause Pyrite and bitumen can often be seen at outcrop andcore, with the benefit of thin section examination, scanning electron microscopyanalysis, energy spectrum analysis, etc., there also have many hydrothermal mineralsdeposited in dolomite of Qixia Formation. These hydrothermal minerals includingquartz, fluorite, illite, barite and apatite filled in the corroded pores and vugs.Over-dolomitization means that the dolomite precipitated in the pores and vugs andthus made the rock more compact. After that the saddle dolomite dissolution, calciteprecipitate in the pores and vugs formed by dolomite dissolution. Dolomite of QixiaFormation has typical saddle crystal morphology and curved crystal faces, and appearwavy extinction in thin section under crossed-polarized light, also has dissolution,brecciation, all these features are associated with hydrothermal fluid.
The δ13C(PDB) of dolomite and limestone of Qixia Formation lie in the range of-0.66~3.84‰, the δ18O(PDB) of dolomite lie in the range of-3.42~9.16‰，reflectingthe fluid comes from marine. Homogenization temperature of matrix dolomite fluidinclusions show a range of67~243℃, homogenization temperature of saddle dolomitein a range of91~223℃, and the homogenization temperature of calcite in a range of54~215℃, demonstrating that the temperature dolomite precipitated higher more than10℃than calcite precipitated. And the homogenization temperature reach up to243℃,which is not only the burial condition can be reached.
Adopting oxygen isotope of minerals and the homogenization temperature offulid inclusions to invert the oxygen isotope of fluid. The δ18O of fluid correspondingwith matrix dolomite, void-filling dolomite and saddle dolomite lie in the range of0~12‰(SMOW), the δ18O of few samples’ corresponding fluid lie in the range of-4~0‰(SMOW), and there are2samples’(one is matrix dolomite, the other is saddledolomite) δ18O of fluid lie in the range of12~13.5%(SMOW). The δ18O of fulid thatcalcite precipitate lie in the range of-4~0‰(SMOW),0~8‰(SMOW),12~14.5‰(SMOW), and recorded the multi-periods of50~100℃,100~170℃,190~250℃, and the salinity of fulid is higher or much higher than the coeval seawater.The87Sr/86Sr ratios of coeval sewater in Permian lies in0.7085~0.7067, while the87Sr/86Sr ratios of dolomite of Qixia Formation lies in0.7076~0.7069and is lowerthan the coeval seawater. Thermal history recorded the temperature anomaly between Middle and Late Permian, the maximum paleo-heat flow reached in the early stage ofLate Permian at approximately259Ma, after that the paleo-heat flow decreased topresent. Meaning the dolomitization fluid mainly derived from the coeval seawaterwhich influenced by the abnormal heat.
The crystalline dolomites are the mainstream dolomite phases in FeixianguanFormation of Lower Triassic, Northeastern Sichuan Basin. And there also exist somefabric-retentive dolomitic grainstones and micritic dolomites. The dolomites inNortheastern Sichuan Basin have low manganese contents (average of63.47ppm),low Ferrum contents (average of1019.67ppm) and high strontium contents (averageof132.39ppm). The crystalline dolomite phases have high strontium contents, and theassociated calcite cements have extreme high strontium contents. The δ13C values areclose to the compositions of coeval seawater. The precipitating fluids of thesedolomite phases have the relatively high δ18O values (ranges between2to7‰;SMOW), and have the higher87Sr/86Sr ratios than the ratios of coeval seawater. Fromthe earlier Changxing Formation to the later Leikoupo Formation, the differencesbetween strontium isotope ratios of dolomites and of coeval seawater decreasedgradually. The precipitating fluids of dolomites were getting closer and closer tocoeval seawater. The homogenization temperatures of fluid inclusions in dolomitesare high (ranges from85.85to142.24℃). And the salinities of fluid inclusions indolomites are double as much as the salinity of seawater (ranges from3.01to12.61%NaCl). Thus, the dolomitizing fluid is a kind of marine-derived fluid, andoriginated from downward-migrated refluxing evaporated and concentrated seawaterof Jialingjiangian. The dolomitization occurred in a closed diagenetic system duringdeep burial, and was the product of brine infiltration during deep burial.
引文
[1] Adams J F, Rhodes M L. Dolomitization by seepage refluxion[J]. AAPG Bulletin,1960,44:1912-1920.
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