唐山及邻区下奥陶统碳酸盐岩微相分析、白云石化特征和碳氧同位素研究
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摘要
南堡凹陷及其周边地区下古生界碳酸盐岩储层是渤海湾盆地重要的油气勘探热点。通过对研究区各种资料全面认识,选取唐山地区赵各庄下奥陶系冶里～亮甲山组典型剖面为主要研究对象,以潮控碳酸盐岩缓坡的微相分析为主线,对剖面所处下古生界的沉积相、沉积体系和沉积环境时间演化和空间展布的研究。识别出冶里组～亮甲山组主要的微相类型和沉积相特征之后,分别建立了对应的潮控碳酸盐岩缓坡体系在唐山地区的相序演化综合图。在此基础上对相关相带以白云岩化为主的成岩作用进行分析。
以典型样品的显微薄片观察、环境扫描电镜形态成分分析和碳氧稳定同位素分析为手段,对不同相带的白云岩化特征进行对比和归纳,建立合适的白云岩化模式以利于探索相关相带中有利储层的配置。通过碳氧稳定同位素分析,对微相分析结论中的碳酸盐岩沉积环境、海平面升降作了对比研究,探索研究稳定同位素分布与碳酸盐地层旋回、白云岩化和古温度古环境的关系。取得一些进展如下：
1根据基质、颗粒和组构等关键特征,借鉴Flugle关于碳酸盐岩缓坡微相鉴定标志,识别出7种微相类型。其中新增RMF31磨圆的竹叶状砾屑灰岩,RMF32磨圆的内碎屑-生屑颗粒/泥粒灰岩。其余分别是RMF7含棘皮生物碎屑和内碎屑的泥粒灰岩,RMF8:具生物潜穴的和多种颗粒的粒泥灰岩,MF9-BI具坡源生屑/内碎屑的粒泥/泥粒灰岩,RMF9-F：坡源的磨圆内碎屑为主的漂砾,RMF9-L含磨圆岩屑的粒泥灰岩,RMF9-A磨圆藻屑粒泥/泥粒灰岩,RMF14含多种生屑的泥粒/粒泥灰岩,RMF18含介形虫的粒泥灰岩。
2唐山地区冶里～亮甲山组沉积相是上寒武统的延续,为由泄湖、颗粒滩、局限台地亚相构成的潮控碳酸盐岩体系的内坡相。
3下奥陶统冶里组经历了一个完整三级层序在台地边缘带演化序列,即：由低位域的内坡局限台地岩相开始,经海侵体系域下部的开阔台地海亚相,至海侵体系域上部变为中缓坡相。以外缓坡相出现为标志的最大海泛层之上,转化为中缓坡为标志的高位体系域。亮家山组充分表现出内坡局限台地岩相占主导的沉积构成特征。
4按照晶体形态、赋存方式以及矿物成分将本区的白云石分为4类,分别为①白云岩化强烈,粗晶,自形,具环带,晶体边界轮廓清晰,粒内和粒间发育收缩孔隙；②白云石含量低,细晶,半自形-它形,边界模糊;③白云石含量低,细晶,半自形-它形,边界模糊,伴生石膏和石盐晶型完好；④白云岩化强烈,粗晶,自形,具环带,晶体边界轮廓清晰,粒内和粒间孔隙不发育,偶尔伴生石膏和石盐。
5根据微相分析的沉积环境特征,结合不同沉积相上白云岩化特征,归纳出研究区在冶里～甲山期的两种白云岩化模式。分别为成岩期毛细管泵汲—蒸发白云岩化模式和同沉积～同生期过蒸发—海水浓缩白云岩化模式。前者主要发生在潮缘相和局限台地相,后者发生在泄湖相和颗粒滩相。
6全岩碳酸盐氧碳同位素分析表明冶里组白云岩的δ13C值为-7.119‰～76‰,均值-2.98‰,δ18O值为-9.09‰～4.65‰,均值为-6.12‰(PDB),亮甲山组δ13C值-115‰-0.3‰,均值-0.57‰，δ18O值为-8.76‰～7.48‰，均值-8.06‰(PDB)。冶里组较小的碳值说明形成于正常海水,而亮甲山组碳值较高,属于咸化介质。氧同位素分析表明亮甲山组高负值可能来自暴露后大气淡水的加入或深埋藏环境中高温的影响。
7研究区碳同位素分布特征与沉积相类型存在着较强的对应关系,表现为极大值出现在RMF31磨圆竹叶状砾屑灰岩,沉积相类型为内坡颗粒滩相/局限台地相,极小值出现在RMF18含介形虫生屑砾泥灰岩沉积相类型为内缓坡/开阔台地相。
8冶里期经历完整的三级沉积系列变化,δ13C值从较高到较低的变化主要与海平面的降低有关,变化趋势与全球同时期低纬度碳同位素—致。亮甲山组下部随着海侵海平面的升高δ13C值上升,而中上部分属高位体系域占优势,内缓坡颗粒滩相和泄湖相为主,使得δ13C值围绕0‰波动,没有明显的漂移。
9在6次海进海退事件对比中,研究区具有与其它剖面更低δ13C值,通过对剖面的岩石特征、沉积体系以及微区分析等手段,认为营养海/饥饿海模式和海底有机质氧化机制是导致较低δ13C值的主要因素,而δ13C的最低负值则与硫酸盐还原作用有关。
10同位素计算古温度表明：冶里组下段古温度在15℃～25℃，冶里组上段-亮甲山组上段温度在较高位置波动30℃-45℃，而亮甲山组中-上段温度最低,波动范围10℃-15℃。较高温度出现的沉积相是局限台地相-开阔台地相,较低温度则出现在颗粒滩相-泄湖相。较高温度段中出现马鞍状白云石,有铁氧化圈是否指示经历过埋藏作用有待进一步研究。
Lower Paleozoic carbonate rock reservoir of Nanpu sag and adjacent aera is one of the hot spot in oil/gas exploration of Bohai bay. Based on the the materials of study area, selected the Zhaogezhuang profile to analyse the characters of microfacies, sediment enviroment and their spatial distrubution. After indentified the main facies types and sediment features of Yeli-Liangjiashan Formation, estabished the facise-order evolution integrate map of tide-conctrol carbonate slop system of Tanshan aera. Then, anlysised the the correlative facies-zone's diagenesis which dominant by the dolomitizaton.
By the means of the thin section observation of all rock sampes, the analyse of microscopy shape and elemental component in typical rock under environmental scanning electron microscope, and the analyse of Carbon Oxygen stable isotope of the representative sampling, established the appropriate dolomitization models to the correlative facies-zones.
Contrasted and concluted the results between the carbon stable isotope analysis, the sediment enviroment and the changes of global sea-level. Discussed the reservior unit compartmentalize and reservior capability of Yeli-Liangjiashan formation by the analysis of sediment microfacies, sediment facies, diagenesis, post-diagenesis and stable isotope analysis.
Acquired some coclution as follow:
1、According to the key charecters of matrix,gain and rock fabric, and use Flugle's microfacies identify class about carbonate slop,7microfacies type was recorgnized. In this paper, two newly facies, namely, RMF31and RMF32was recorgnised and added into the type of cabonate ramp facies. Respectively, RMF7:aboundant echinoderms bioclastic packstone and intra-bioclasts mudstone. RMF8:packstone with arillaceous and multi-grians RMF9-BI with ramp-derived ioclastic/intra-packstone/mudstone. RMF9-F:floatstone dominated by ramp-derived rounding intra-clasts. RMF9-A:rounding alga-clasts wackestone/packstone. RMF14:multi-bioclastic packstone/wackestone. RMF18:bioclastic wackestone with ostracods. RMF31:rounding Spatulate float rudite limestone, RMF32:rounding intraclastic-bioclastic grain/wackestone.
2、The sediment feature of Tangshan Yeling-Liangjiashan formation continues from the Upper Cambrian, it is belongs to the tide control cabonate rock system of inner slop facies which was made up by lagoon/grain-shoal/restrict plateform sub-facies.
3、The evolution serial of Yeli formation is a intergrity third class sequence plateform. Namly, it is begains at at the inner restrict plateform facies of LST, then changed to the open-plateform sub-facies of lower TST, and to the mid-slop facies of the upper HST. Ovber the surfaces of maximum flooding, it changed to HST which marked by middle slop. On the other hand, the Liangjiashang formation shows the character of dominated by the inner slop restrict platform facies.
4、Fur types of dolomaite was distinguished in the study area.①intensity dolomitization, coarse crystal, euhedral, ring-zone, clear crystal boundary ouline, with well growth shrink hole between inner and space of grain.②few dolimite, fine crystal, ubhedral to anhedral.③blur edge few dolimite, fine crystal, subhedral to anhedral, adjoint with fine crystal of gypsum and halite.④intensity dolomitization, coarse crystal, euhedral, ring-zone, clear crystal boundary outline, few of growth shrink hole between inner and space of grain, sporadic with fine crystal of gypsum and halite.
5-Cncluded two dolomitization models refers tothe resuults of sediment facies and dolomitization character. One is the diagenetic capillary punp draw to evaporation dolomitization model, it mainly occurred in the tide-edge facies and restrict platform facies, and the other is the syngenetic over-evaporation-sea-water condense solomitization model, the former, taken placed in the lagoon facies and grain-shoal facies.
6、Whole rock carbonate rock isotope analysis shows that the813C value of Yeli formation dolomite is-7.11‰～0.769‰(PDB), means-2.98‰,δ18O is-9.09‰～-4.65‰, means-6.12‰, and the813C of Liangjiashang formation dolomite is-1.15‰～0.3‰, means-0.57‰,δ18O-8.76‰～7.48‰, means-8.06‰(PDB). The lighter carbon value of Yeli formation indicated that it was forming with normal water, but the higher value of Liangjiashang formation showed the environment of salted medium. Oxygen isotope analysis demonstrated that, the higher negative value of Liangjiashang formation maybe come from the join of meteoric fresh-water after exposure or was affected by the high-temperature during the deep burial enviroment.
7、There is a tight relation between the carbon isotope distribution and sediment facies. The maximum carbon value appearenced at RMF31, rounding Spatulate calcirudite, with sediment facies of the inner grain-shoal/restric platform, the minimum value at RMF18, related with the inner slop/open-plateform facies.
8、As the result of a integrated3-rd sequence evolution to the Yeli formation went through, the changes of813C value was tightly related with globe sea level eustacy, and the trends of carbon isotope was accordanced to the lower latitude in same period. The813C value of bottom Liangjiashan Formation was rise, but in the middle-uuper parts which dominated by HST, the main facies was inner ramp lagoon and grain-shoal, it rotate around0‰, and without obvious dtift.
9、The δ13C value in study area was lighter than other profiles. With the analysis of rock character, sediment system and micro-area when compaired the6events of transgression and regression. It's convinced that the main reason to the lighter δ13C value should be related with the model of over-nutrition/starvation sea and the organic oxidation mechanism in seafloor. and the lowest neagtive value was explained by the sulphate reduction.
10、Paleo-temperature caculated by carbon isotope in the lower Yeli formation was ranged from15℃～25℃. The upper Yeli formation to Liangjiashang formation has the more higher value range of30℃～45℃, and the mid-upper Liangjiashang formation has the lowest range of10℃～15℃. The higher temperature occured at the restrict platform facies to open platform facies, however, the lowest temperature at grain-shoal facies to lagoon facies. Therefor, further study was needed to estimate whether or not the higher temperature of upper Yeli formation to Liangjiashang formation undergo burial diagenesis, which has saddle dolomite and the iron content of dolomite.
以典型样品的显微薄片观察、环境扫描电镜形态成分分析和碳氧稳定同位素分析为手段,对不同相带的白云岩化特征进行对比和归纳,建立合适的白云岩化模式以利于探索相关相带中有利储层的配置。通过碳氧稳定同位素分析,对微相分析结论中的碳酸盐岩沉积环境、海平面升降作了对比研究,探索研究稳定同位素分布与碳酸盐地层旋回、白云岩化和古温度古环境的关系。取得一些进展如下：
1根据基质、颗粒和组构等关键特征,借鉴Flugle关于碳酸盐岩缓坡微相鉴定标志,识别出7种微相类型。其中新增RMF31磨圆的竹叶状砾屑灰岩,RMF32磨圆的内碎屑-生屑颗粒/泥粒灰岩。其余分别是RMF7含棘皮生物碎屑和内碎屑的泥粒灰岩,RMF8:具生物潜穴的和多种颗粒的粒泥灰岩,MF9-BI具坡源生屑/内碎屑的粒泥/泥粒灰岩,RMF9-F：坡源的磨圆内碎屑为主的漂砾,RMF9-L含磨圆岩屑的粒泥灰岩,RMF9-A磨圆藻屑粒泥/泥粒灰岩,RMF14含多种生屑的泥粒/粒泥灰岩,RMF18含介形虫的粒泥灰岩。
2唐山地区冶里～亮甲山组沉积相是上寒武统的延续,为由泄湖、颗粒滩、局限台地亚相构成的潮控碳酸盐岩体系的内坡相。
3下奥陶统冶里组经历了一个完整三级层序在台地边缘带演化序列,即：由低位域的内坡局限台地岩相开始,经海侵体系域下部的开阔台地海亚相,至海侵体系域上部变为中缓坡相。以外缓坡相出现为标志的最大海泛层之上,转化为中缓坡为标志的高位体系域。亮家山组充分表现出内坡局限台地岩相占主导的沉积构成特征。
4按照晶体形态、赋存方式以及矿物成分将本区的白云石分为4类,分别为①白云岩化强烈,粗晶,自形,具环带,晶体边界轮廓清晰,粒内和粒间发育收缩孔隙；②白云石含量低,细晶,半自形-它形,边界模糊;③白云石含量低,细晶,半自形-它形,边界模糊,伴生石膏和石盐晶型完好；④白云岩化强烈,粗晶,自形,具环带,晶体边界轮廓清晰,粒内和粒间孔隙不发育,偶尔伴生石膏和石盐。
5根据微相分析的沉积环境特征,结合不同沉积相上白云岩化特征,归纳出研究区在冶里～甲山期的两种白云岩化模式。分别为成岩期毛细管泵汲—蒸发白云岩化模式和同沉积～同生期过蒸发—海水浓缩白云岩化模式。前者主要发生在潮缘相和局限台地相,后者发生在泄湖相和颗粒滩相。
6全岩碳酸盐氧碳同位素分析表明冶里组白云岩的δ13C值为-7.119‰～76‰,均值-2.98‰,δ18O值为-9.09‰～4.65‰,均值为-6.12‰(PDB),亮甲山组δ13C值-115‰-0.3‰,均值-0.57‰，δ18O值为-8.76‰～7.48‰，均值-8.06‰(PDB)。冶里组较小的碳值说明形成于正常海水,而亮甲山组碳值较高,属于咸化介质。氧同位素分析表明亮甲山组高负值可能来自暴露后大气淡水的加入或深埋藏环境中高温的影响。
7研究区碳同位素分布特征与沉积相类型存在着较强的对应关系,表现为极大值出现在RMF31磨圆竹叶状砾屑灰岩,沉积相类型为内坡颗粒滩相/局限台地相,极小值出现在RMF18含介形虫生屑砾泥灰岩沉积相类型为内缓坡/开阔台地相。
8冶里期经历完整的三级沉积系列变化,δ13C值从较高到较低的变化主要与海平面的降低有关,变化趋势与全球同时期低纬度碳同位素—致。亮甲山组下部随着海侵海平面的升高δ13C值上升,而中上部分属高位体系域占优势,内缓坡颗粒滩相和泄湖相为主,使得δ13C值围绕0‰波动,没有明显的漂移。
9在6次海进海退事件对比中,研究区具有与其它剖面更低δ13C值,通过对剖面的岩石特征、沉积体系以及微区分析等手段,认为营养海/饥饿海模式和海底有机质氧化机制是导致较低δ13C值的主要因素,而δ13C的最低负值则与硫酸盐还原作用有关。
10同位素计算古温度表明：冶里组下段古温度在15℃～25℃，冶里组上段-亮甲山组上段温度在较高位置波动30℃-45℃，而亮甲山组中-上段温度最低,波动范围10℃-15℃。较高温度出现的沉积相是局限台地相-开阔台地相,较低温度则出现在颗粒滩相-泄湖相。较高温度段中出现马鞍状白云石,有铁氧化圈是否指示经历过埋藏作用有待进一步研究。
Lower Paleozoic carbonate rock reservoir of Nanpu sag and adjacent aera is one of the hot spot in oil/gas exploration of Bohai bay. Based on the the materials of study area, selected the Zhaogezhuang profile to analyse the characters of microfacies, sediment enviroment and their spatial distrubution. After indentified the main facies types and sediment features of Yeli-Liangjiashan Formation, estabished the facise-order evolution integrate map of tide-conctrol carbonate slop system of Tanshan aera. Then, anlysised the the correlative facies-zone's diagenesis which dominant by the dolomitizaton.
By the means of the thin section observation of all rock sampes, the analyse of microscopy shape and elemental component in typical rock under environmental scanning electron microscope, and the analyse of Carbon Oxygen stable isotope of the representative sampling, established the appropriate dolomitization models to the correlative facies-zones.
Contrasted and concluted the results between the carbon stable isotope analysis, the sediment enviroment and the changes of global sea-level. Discussed the reservior unit compartmentalize and reservior capability of Yeli-Liangjiashan formation by the analysis of sediment microfacies, sediment facies, diagenesis, post-diagenesis and stable isotope analysis.
Acquired some coclution as follow:
1、According to the key charecters of matrix,gain and rock fabric, and use Flugle's microfacies identify class about carbonate slop,7microfacies type was recorgnized. In this paper, two newly facies, namely, RMF31and RMF32was recorgnised and added into the type of cabonate ramp facies. Respectively, RMF7:aboundant echinoderms bioclastic packstone and intra-bioclasts mudstone. RMF8:packstone with arillaceous and multi-grians RMF9-BI with ramp-derived ioclastic/intra-packstone/mudstone. RMF9-F:floatstone dominated by ramp-derived rounding intra-clasts. RMF9-A:rounding alga-clasts wackestone/packstone. RMF14:multi-bioclastic packstone/wackestone. RMF18:bioclastic wackestone with ostracods. RMF31:rounding Spatulate float rudite limestone, RMF32:rounding intraclastic-bioclastic grain/wackestone.
2、The sediment feature of Tangshan Yeling-Liangjiashan formation continues from the Upper Cambrian, it is belongs to the tide control cabonate rock system of inner slop facies which was made up by lagoon/grain-shoal/restrict plateform sub-facies.
3、The evolution serial of Yeli formation is a intergrity third class sequence plateform. Namly, it is begains at at the inner restrict plateform facies of LST, then changed to the open-plateform sub-facies of lower TST, and to the mid-slop facies of the upper HST. Ovber the surfaces of maximum flooding, it changed to HST which marked by middle slop. On the other hand, the Liangjiashang formation shows the character of dominated by the inner slop restrict platform facies.
4、Fur types of dolomaite was distinguished in the study area.①intensity dolomitization, coarse crystal, euhedral, ring-zone, clear crystal boundary ouline, with well growth shrink hole between inner and space of grain.②few dolimite, fine crystal, ubhedral to anhedral.③blur edge few dolimite, fine crystal, subhedral to anhedral, adjoint with fine crystal of gypsum and halite.④intensity dolomitization, coarse crystal, euhedral, ring-zone, clear crystal boundary outline, few of growth shrink hole between inner and space of grain, sporadic with fine crystal of gypsum and halite.
5-Cncluded two dolomitization models refers tothe resuults of sediment facies and dolomitization character. One is the diagenetic capillary punp draw to evaporation dolomitization model, it mainly occurred in the tide-edge facies and restrict platform facies, and the other is the syngenetic over-evaporation-sea-water condense solomitization model, the former, taken placed in the lagoon facies and grain-shoal facies.
6、Whole rock carbonate rock isotope analysis shows that the813C value of Yeli formation dolomite is-7.11‰～0.769‰(PDB), means-2.98‰,δ18O is-9.09‰～-4.65‰, means-6.12‰, and the813C of Liangjiashang formation dolomite is-1.15‰～0.3‰, means-0.57‰,δ18O-8.76‰～7.48‰, means-8.06‰(PDB). The lighter carbon value of Yeli formation indicated that it was forming with normal water, but the higher value of Liangjiashang formation showed the environment of salted medium. Oxygen isotope analysis demonstrated that, the higher negative value of Liangjiashang formation maybe come from the join of meteoric fresh-water after exposure or was affected by the high-temperature during the deep burial enviroment.
7、There is a tight relation between the carbon isotope distribution and sediment facies. The maximum carbon value appearenced at RMF31, rounding Spatulate calcirudite, with sediment facies of the inner grain-shoal/restric platform, the minimum value at RMF18, related with the inner slop/open-plateform facies.
8、As the result of a integrated3-rd sequence evolution to the Yeli formation went through, the changes of813C value was tightly related with globe sea level eustacy, and the trends of carbon isotope was accordanced to the lower latitude in same period. The813C value of bottom Liangjiashan Formation was rise, but in the middle-uuper parts which dominated by HST, the main facies was inner ramp lagoon and grain-shoal, it rotate around0‰, and without obvious dtift.
9、The δ13C value in study area was lighter than other profiles. With the analysis of rock character, sediment system and micro-area when compaired the6events of transgression and regression. It's convinced that the main reason to the lighter δ13C value should be related with the model of over-nutrition/starvation sea and the organic oxidation mechanism in seafloor. and the lowest neagtive value was explained by the sulphate reduction.
10、Paleo-temperature caculated by carbon isotope in the lower Yeli formation was ranged from15℃～25℃. The upper Yeli formation to Liangjiashang formation has the more higher value range of30℃～45℃, and the mid-upper Liangjiashang formation has the lowest range of10℃～15℃. The higher temperature occured at the restrict platform facies to open platform facies, however, the lowest temperature at grain-shoal facies to lagoon facies. Therefor, further study was needed to estimate whether or not the higher temperature of upper Yeli formation to Liangjiashang formation undergo burial diagenesis, which has saddle dolomite and the iron content of dolomite.
引文
[1]安太庠,张放,向维达.华北及邻区牙形石.北京：科学出版社,1983.1-195.
[2]包洪平,杨承运,碳酸盐岩微相分析及其在岩相古地理研究中的意义,岩相古地理,1999,19(6)：60-63.
[3]曹守连.南堡凹陷断裂带构造演化及成藏条件分析.断块油气田,1997,4(2)：13-16.
[4]陈恭洋,何鲜,陶自强,等.千米桥潜山碳酸盐岩古岩溶特征及储层评价[J].天然气地球科学,2003,14(5)：3752379.
[5]陈好寿.同位素地球化学研究[M].杭州：浙江大学出版社,1994.
[6]陈锦石,陈文正,碳同位素地质学概论,北京：地质出版社,1983.
[7]陈永武.储集层与油气分布.北京：石油工业出版社,1995.
[8]成永生,渤海湾盆地南堡凹陷周边地区寒武-奥陶系碳酸盐岩储层研究,[学位论文],中南大学,2008.
[9]成永生,陈松岭,南堡凹陷周边寒武-奥陶系碳酸盐岩储层特征及成岩作用[J].地质找矿论丛2008,23(3)231-235.
[10]丛良滋,周海民.南堡凹陷主动裂谷多幕拉张与油气关系.石油与天然气地质,1998,19(4)：296-301.
[11]戴永定,生物矿物学[M],北京：石油工业出版社,1994.
[12邓俊国,王贤.南堡凹陷构造应力场演化史与油气聚集.保定师专学报,1999,12(2)：72-77.
[13]丁梯平.氢氧同位素地球化学[M].北京：地质出版社,1980.
[14]董月霞,夏文臣,周海民.南堡凹陷第三系火山岩演化序列研究.石油勘探与开发,2003,30(2)：24-26.
[15]董月霞,周海民,夏文臣.南堡凹陷第三系层序地层与油气成藏的关系.石油与天然气地质,2003,24(1)：39-41.
[16]董月霞,周海民,夏文臣.南堡凹陷火山活动与裂陷旋回.石油与天然气地质,2000,21(4)：304-307.
[17]窦立荣,王一刚.中国古生界海相碳酸盐岩油气藏的形成与分布.石油实验地质,2003,25(5)：419-425.
[18]方少仙,董兆雄,侯方浩等.层状白云岩储层特征与成因[M].北京：地质出版社.1999,1-115
[19]费宝生,汪建红.中国海相油气田勘探实例(之三)：渤海湾盆地任丘古潜山大油田的发现与勘探.海相油气地质,2005,10(3)：43-50.
[20]冯洪真,刘家润,施贵军.2000.湖北宜昌地区寒武系-下奥陶统的碳氧同位素记录.高校地质学报,6(1)：106-115.
[21]冯增昭,沉积岩石学(第二版,上、下册)[M].石油工业出版社2004.
[22]冯增昭,单因素分析多因素综合作图-定量岩相古地理重建[J],古地理学 报,2004,6(1),3-19
[23]冯增昭,华北早奥陶世岩相古地理新探[J],地质科学,1979,6(4),302-313.
[24]冯增昭,碳酸盐岩岩相古地理学[M]北京：石油工业出版社,1989.
[25]冯增昭等,鄂尔多斯地区奥陶纪地层岩相古地理[M]北京：地质出版社,1998.
[26]冯增昭等,华北地台早古生代岩相古地理[M],北京：地质出版社,1990.
[27]冯增昭等,下扬子地区中下三叠统青龙群岩相古地理[M],北京：地质出版社,1988.
[28]冯增昭等,中下扬子地区二叠纪岩相古地理[M]北京：地质出版社,1991.
[29]冯增昭等华北地台早古生代岩相古地理[M]北京：地质出版社,1991.
[30]傅学斌,刘蕴华,曹中宏,等.冀东探区潜山油藏形成条件及分布规律研究[J].地质科技情报,2004,23(3)：66-70.
[31]顾家裕,朱筱敏,贾进华等.塔里木盆地沉积与储层[M1.北京：石油工业出版社.2003.1--400.
[32]顾家裕.塔里木盆地下奥陶统白云岩特征及成因(J].新疆石油地质,2000,21(2)：120-122
[33]郭绪杰,焦贵浩.华北古生界石油地质.北京：地质出版社,2002.
[34]韩宝平,陈锁忠,冯启言.任丘油田古潜山储集孔隙特征研究[J].中国矿业大学学报,1997,26(2)：46-51.
[35]韩宝平,刘仁达,罗承建,等.岩溶作用对任丘古潜山碳酸盐岩油藏赋存的控制作用[J]中国岩溶,1998,17(1)：75-80.
[36]韩晋阳,肖军,郭齐军,等.渤海湾盆地南堡凹陷沉降过程、岩浆活动、温压场演化与油气成藏的综合分析[J].石油实验地质,2003,25(3)：257-263.
[37]何自新,杨奕华.鄂尔多斯盆地奥陶系储层图册[MI.北京：石油工业出版社.2004.1-24.4
[38]黄思静,Qing,Hairuo,胡作维等,四川盆地东北部三叠系飞仙关组硫酸盐还原作用对碳酸盐成岩作用的影响[J].沉积学报,2007,25(6)：815-824.
[39]黄思静,裴锡古,谢庆邦.陕甘宁盆地中部奥陶系碳酸盐风化壳中的地开石及其与储层的关系[J].成都理工学院学报,1995,22(3)：43-51.
[40]黄思静,王春梅等,碳酸盐岩成岩作用的研究前沿和值得思考的问题[J],成都理工大学学报(自然科学版),2008,35(1)1-10.
[41]嵇少丞,王茜,许志琴,华北克拉通破坏与岩石圈减薄[J].地质学报,2008.82(2)：174-193.
[42]姜平,王建华.大港地区千米桥潜山奥陶系古岩溶研究[J].成都理工大学学报(自然科学版),2005,32(1)：50-53.
[43]卢鸿,王铁冠,徐新德,等.南堡凹陷原油的有机地球化学特征[J].江汉石油学院学报,1995,20(3)：28-35.
[44]金振奎,邹元荣,等黄骅坳陷奥陶系碳酸盐岩岩溶储层分布规律及其控制因素[J].沉积学报,2001，19(4)530-535.
[45]金振奎.华北地台东部下古生界白云岩的类型及储集性[J].沉积学报,1993,11(2)：11-19.
[46]金之钧.中国海相碳酸盐岩层系油气勘探特殊性问题[J].地学前缘,2005,12(3)：15-22.
[47]李江海,侯贵廷,黄雄南,张志强,钱祥麟,华北克拉通对前寒武纪超大陆旋回的基本制约[J].岩石学报,2001.17(2)：177-186.
[48]李江海,钱祥麟,黄雄南,刘树文,华北陆块基底构造格局及早期大陆克拉通化过程[J].岩 石学报,2000.16(1)：1-10.
[49]李心清,万国江.碳酸盐岩氧、碳稳定同位素地球化学研究目前面临的几个问题[J].地球科学进展,1999.14(3)：262-268.
[50]李振宏,杨永恒等,鄂尔多斯盆地天环北段白云岩体成因及储集性能,海相油气地质[J],2005,10(3)：19-24.
[51]刘波,钱祥麟,王英华,华北板块早古生代构造-沉积演化[J].地质科学,1999.4(3)：347-356.
[52]刘蕴华,周海民,熊保贤等.南堡凹陷的含油气系统分析.石油与天然气地质[J].2000,21(4)：364-365.
[53]卢焕章等.包裹体地球化学[M].北京：地质出版社,1990.
[54]卢武长.稳定同位素地球化学[M].成都：成都地质学院,1986.5.
[55]罗宾巴瑟斯特,碳酸盐沉积物及其成岩作用[M],科学出版社,1980.
[56]吕宝凤,夏斌.关于中国海相碳酸盐岩含油气系统的几点思考[J].天然气地球科学,2005,16(2)：175-177.
[57]吕宝凤,夏斌.中国海相碳酸盐岩地区油气成藏基本特征及勘探系统初探[J].油气地质与采收率,2005,12(s)：21-23.
[58]吕修祥,金之钧.碳酸盐岩油气田分布规律[J].石油学报,2000,21(2)：8-12.
[59]马永生,郭旭升,郭彤楼,等.四川盆地普光大型气田的发现与勘探启示[J].地质论评,2005,51(4)：477-480.
[60]马永生,田海芹.碳酸盐岩油气勘探[M].山东：石油大学出版社,1999.
[61]马永生.中国海相油气田勘探实例之六-四川盆地普光大气田的发现与勘探[J].海相油气地质,2006,11(2)：35-40.
[61]梅博文译.储层地球化学(译文集)[M].西安：西北大学出版社,1992.
[62]梅冥相,华北地台北缘奥陶系亮甲山组的碳酸盐复合海平面变化旋回层序[J],岩相古地理1995，15(5)33-42.
[63]梅冥相,马永生,梅仕龙等.华北寒武系层序地层格架及碳酸盐台地演化[J].现代地质,1997,11(3)：275-252.
[62]牟保磊.元素地球化学[M].北京：清华大学出版社,1999.206-210.
[63]彭澎,翟明国,华北陆块前寒武纪两次重大地质事件的特征和性质[J].地球科学进展,2002.17(6)：818-825.
[64]钱凯,李本亮,许惠中.从全球海相古生界油气地质共性看四川盆地海相地层天然气勘探方向[J].天然气地球科学,2003,14(3)：167-171.
[65]钱峥,黄先雄,碳酸盐岩成岩作用及储层-以中国四川东部石炭系为例[M].北京：石油工业出版社.2000.1-119.
[66]强子同.碳酸盐岩储层地质学[M].东营：石油大学出版社.1998.1-470.
[67]邵济安,牟保磊,张履桥,华北东部中生代构造格局转换过程中的深部作用与浅部响应[J].地质论评,2000.46(1)：32-40.
[68]邵龙义,碳酸盐岩氧、碳同位素与古温度等的关系[J],中国矿业大学学报,1994,23(1)：39-45.
[69]石振荣,葛云龙,秦风启.南堡凹陷北部断裂特征动力学分析[J].断块油气田,2000,7(4)：1-4.
[70]苏立萍,罗平,胡社荣等.苏桥潜山带奥陶系碳酸盐岩储集层研究[J].石油勘探与开发,2003,30(6)：54-57.
[71]谭丽娟,田世澄.南堡凹陷油气运移特征及成藏动力学系统划分[J].石油勘探与开发,2000,27(5)：16-18.
[72]谭丽娟,田世澄.南堡凹陷油气运移特征及成藏动力学系统划分[J].石油勘探与开发,2000,27(5)：16-18.
[73]汤朝阳等.白云石化作用及白云岩问题研究述评[J].东华理工学院学报,2006.9,205-211.
[74]田景春,陈洪德,侯明才等.右江盆地晚古生代白云岩与层序地层的关系及其储集性[J].成都理工大学学报,2004,31(1)：34-39.
[75]汪啸风,陈旭,陈孝红等.中国地层典：奥陶系[M].北京：地质出版社,1996.1-126.
[76]王大锐,白志强.广西中-上泥盆统界线附近的化学地层学特征[J].地层学杂志,2002a.26(1)：50-54.
[77]王大锐,渤海湾地区下古生界碳、氧同位素地球化学研究[J].地质学报2002,3(8)400-408
[78]王刚,窦立荣,文应初等.四川盆地东北部三叠系飞仙关组高含硫气藏H2S成因研究[J].地球化学,2002,31(6)：517-524.
[79]王家豪,王华,王根发.南堡凹陷厚层泥岩的封-盖作用及期与油气的关系石油实验地质,2001,23(4)：418-423.
[80]王家豪,王华,周海民等.断陷湖盆基底非线性沉降与H型层序的形成-以冀东油田南堡凹陷为例[J].石油与天然气地质,2001,22(3)：203-206.
[81]王杰,陈践发.海相碳酸盐岩烃源岩的研究进展[J].天然气工业,2004,24(8)：21-23.
[82]王涛,郑亚东,张进江,华北克拉通中生代伸展构造研究的几个问题及其在岩石圈减薄研究中的意义[J].地质通报,2007.26(9)：1154-1166.
[83]王英华等,化石岩石学[M],北京：中国矿业大学出版社,1990.
[84]威尔逊J L著,冯增昭等译.地质历史中的碳酸盐岩相[M].北京：地质出版社,1981.
[85]魏中文等.南堡凹陷深层石油地质特征及有利勘探目标评价[M].唐山：中石油冀东油田勘探开发研究院,2001.
[86]吴昌华,华北克拉通的变质沉积岩及其克拉通的构造划分[J].高校地质学报,2007.13(3)：442-457.
[87]夏日元,唐健生.黄骤坳陷奥陶系古岩溶发育演化模式[J].石油勘探与开发2004,31(1)：51-53.
[88]项礼文,李善姬,南润善等中国地层(4)[M].中国的寒武系北京地质出版社.1981
[89]许化政,周新科,高金慧,华北盆地中南部早古生代沉积特征及油气成藏条件[J].石油学报,2005.26(5)：10-16.
[90]杨承运,卡罗兹A V,碳酸盐岩实用分类及微相分析[M],北京：北京大学出版社,1988.
[91]杨池银,武站国.千米桥潜山奥陶系碳酸盐岩储层成岩作用与孔隙演化[J].石油与天然气地质,2004,25(3).
[92]永生永平,杨池银,王喜双.渤海湾盆地北部奥陶系潜山油气藏成藏组合及勘探技术.石油勘探与开发,2000,27(5)：1-4.
[93]于学敏,苏俊青,王振升.千米桥潜山油气藏基本地质特征[J].石油勘探与开发.1999,26(6)：7-9.
[94]余家仁,陶洪兴,樊哲仁.华北潜山油藏碳酸盐岩储集层研究[M].北京：石油工业出版社,1993.
[95]翟明国,樊棋诚,华北克拉通中生代下地壳置换：非造山过程的壳慢交换[J].岩石学报,2002.18(1)：1-8.
[96]翟明国,彭澎,华北克拉通古元古代构造事件[J].岩石学报,2007.23(11)：2665-2682.
[97]张锦泉.鄂尔多斯盆地奥陶系沉积、古岩溶及储集特征[M].成都：成都科技大学出版社,1992.
[98]张立平,王东坡,克拉通盆地形成机制及沉积特征[J].世界地质,1994.13(3)：26-31.
[99]张小青,羌塘盆地双湖地区侏罗系自云岩成因及储集性研究[D].成都理工大学,2005.
[100]张小青,伊海生,朱迎堂.羌塘盆地双湖地区白云岩储集层特征研究闭[J].西南石油学院学报,2005,27(5)：10-13.
[101]张振英,邵龙义,柳广第.南堡凹陷无井探区烃源岩评价研究[J].石油勘探与开发,2004,31(4)：64-67.
[102]赵太平,翟明国,夏斌等,熊耳群火山岩锆石SHRIMP年代学研究：对华北克拉通盖层发育初始时间的制约[J].科学通报,2004.49(22)：2342-2349.
[103]赵文智,张光亚,何海清等.中国海相石油地质与叠合含油气盆地[M].北京：地质出版社,2002.
[104]赵宗举,范国章等.中国海相碳酸盐岩的储层类型、勘探领域及勘探战略[J].海相油气地质,2007,12(1)：1-11.
[105]中国科学院地质所主编,化石岩石学图版[S],1981.
[106]钟大康、朱筱敏等,南襄盆地泌阳凹陷溶孔溶洞型白云岩储层特征与分布规律[J],地质论评,2004,50(2)：162-169.
[107]钟长汀,邓晋福,万渝生,毛德宝,李惠民.华北克拉通北缘中段古元古代造山作用的岩浆S型花岗岩地球化学特征及锆石SHRIMP年龄[J].地球化学,2007,36(6)：633-637.
[108]周海民,董尽霞,刘蕴蕴华等.小型断陷盆地油气勘探理论与时间-以渤海湾盆地南堡凹陷为例[M].东营：石油大学出版社,2001.
[109]周海民,董月霞,刘蕴华,等.冀东南堡凹陷精细勘探实践与效果[J].中国石油勘探,2003,8(1)：11-15.
[110]周海民,范文科.高成熟探区深化勘探的潜力与措施-以冀东油田南堡凹陷陆地为例[J].中国石油勘探,2001,6(3)：63-70.
[111]周海民,魏忠文,曹中宏,等.南堡凹陷的形成演化与油气的关系[J].石油与天然气地质,2000,21(4)：345-349.
[112]周海民,张玮,谢占安等.断陷盆地大面积三维叠前时间偏移连片处理的地质意义及关键技术[J].石油地球物理勘探,2005,40(6)：693-699.
[113]周新源,王招明,杨海军,等.中国海相油气田勘探实例之五：塔中奥陶系大型凝析气田的勘探和发现[J].海相油气地质,2006,n(1)：45-51.
[117]周志毅,陈均远,林尧坤等.唐山地区奥陶系的新观察.地层学杂志,1983,7(1)：19-31.
[118]朱光有,张水昌,梁英波等.TSR对深部碳酸盐岩储层的溶蚀改造四川盆地深部碳酸盐岩优质储层形成的重要方式[J].岩石学报,2006,22(8)：2182-2194.
[119]朱夏.论中国含油气盆地构造[M].北京：石油工业出版社,1986.
[120]邹元荣,金振奎,由伟丰,黄骅坳陷奥陶纪岩相古地理[M],古地理学报2002,3(4)：35-44.
[121]Prokoph, G.A. Shields, J. Veizer, Compilation and time-series analysis of a marine carbonateδ18O,δ13C, "Sr/86Sr and δ34S database through Earth history[J], Earth-Science Reviews 87 (2008) 113-133.
[122]Braithwaitec.J.R, Rizzig, Dark.G., The geometry and petrogenesis of dolomite hydrocarbon reservoirs [M]. Geological Society (London) SpecialPublication,2004,235:1-413.
[123]CAI Chunfang, XIE Zengye, Worden.R.H, et al, Methane dominated thermochemical sulphate reduction in the Triassic Feixianguan Formation East Sichuan Basin, China: towards prediction of fatal H2S concent rations [J]. Marine and PetroleumGeology,2004, 21:1265-1279.
[124]Chen Ling, Wang Tao, et.al,2008. Distinct lateral variation of lithospheric thickness in the Northeastern North China Craton. Earth and Planetary Science Letters 267:56-68.
[125]Chend, Qingh, Lir, The Late Devonian Frasnian Famennian (F/F) biotic crisis:Insight of rom δ13 C carb,δ13 Corg and 87 Sr/86 Sr isotopic systematics [J]. Earth and Planetary Science Letters,2005,235:151-166.
[126]DaviesAVIES.G.R, Smith.J.L.B, Structurally cont rolled hydrothermal dolomite reservoir facies:An overview[J]. AAPG Bulletin,2006,90 (11):1641-1690.
[127]Deny L A, BrasierM D, Corfield R M, RozanovA Y,& ZhuravlevA Yu.1994. Sr and C isotopic in Lower Cambrian carbonates from the Siberian Craton:a paleoenvironmental record during the Cambrian explosion[J]. Earth and Planetary Science Letters,128: 671-681.
[128]Derry L A, Kaufaman A J,& Jacobsen S B.1992. Sedimentary cycling and environmental chang in the Late Proeterozoic:evidence form stable and radiogenic isotopes[J]. Geochimica et Cosmochimica Acta,56:1317-1329.
[129]FlugleL著,曾允孚译.石灰岩微相[M].北京：地质出版社,1989.
[130]Flugle著,马永生主译,碳酸盐岩微相-分析、解释及应用北京：地质出版社2006，
[131]Gilliskm, Cooganlat, Pedersen.R, Strontium isotope constraints on fluid flow in the upper oceanic crust at the East Pacific Rise [J]. Earth and Planetary Science Letters,2005, 232:83-94.
[132]Hayton,S., Nelson,S.D. (1995):A skeletal assemblage classification system for non-tropical carbonate depositesbased on New Zealand Cenozoic limestones[J]. Sedimentary Geology,100,123-141.
[133]Horowitz.A.S, Potter.P.E, Introductory petrography of fossils[M]. New York, Springer-Verlag,1971.
[134]FlugleL, Microfacies of carbonate rocks:Analysis, Interpretation and Application [M], New York Inc:Springer 2004.
[135]Feng Zengzhao, Jin Zhenkui. Types and origin of dolostones in the Lower Palaeozoic of the North China Platform[J]. Sedimentary Geology,1994 (93):279-290.
[136]Enos, P. Samankassou.E(1998):Lofer cyclothems reservited (Late Triassic. Northern Alps.Austria).Facies.38.207-228.
[137]Feng Zengzhao, Jin Zhenkui:Types and origin of dolostones of Lower Palaeozoic in the North China Platform[J], Sedimentary Geology,1994,Vol93, Nos.3-4,P.279-290.
[138]James,N.P(1997), The cool-water carbonate depositional realm, In:James,N.P, Clarke, A.D(eds):coole-water carbonates:SEPM special Publictions,56,1-20.
[139]Jean-Jacques.C, Jean-Paul.S.M and Conesa.G et al. Geometry, palaeoenvironments and relative sea-level(accommodation space) changes in the Messinian Murdjtdjo carbonate platform (Orau, western Algeria):consequences[J]. Sedimentary Geology, 1994,89:143-158.
[140]KATZ D A, EBERL I G P, SWART P K, et al.Tectonic-hydrothermal brecciation associated with calcite precipitation and permeability dest ruction in Mississippian carbonate reservoirs, Montana and Wyoming [J]. AAPGBulletin,2006,90.
[141]Kaufman A J & Kno 11 A H.1995. Neoproterozoic variations in the C-isotope composition of seawater:stratigraph ic and biogeochemical implications[J]. Precambrian Research,73: 27-49.
[142]Kaufman A J, Konll A H,& N arbonne G M.1997. Isotopes, iceages and terminal Proterozoic earth history[J]. Preceedings of the National Academy of Sciences,95: 6600-6605.
[143]Lasemi, palaeoenvironments and sequences[J]. Sedimentology,1995,99:151-164.
[144]Lasemi.Y, Platform carbonates of the Upper Jurassic Mozduran Formation in the Kopef Dagh Basin, NE Iran:facies.
[145]Lees.A, Buller.A.T(1972):Modern temperate-water and warm water shelf carbonate sediments contrasted.-Marine Geology,13,M67-M73.
[146]Lonnee.J, Machel.H.G, Pervasive dolomitization with subsequent hydrothermal alteration in he Clarke Lake gas field, Middle Devonian Slave Point Formation, British Columbia, Canada [J]. AAPGBulletin,2006,90 (11):173-1761.
[147]Luczaj.J.A, Harrison.W.B,Wiliams.N.S. Fractured hydrothermal dolomite reservoirs in the Devonian Dundee Formation of the cent ral Michigan Basin [J]. AAPG Bulletin,2006, 90(11):1787-1801.
[148]Luczajj.A, Evidence against the Dorag (mixing zone) model for dolomitization along the Wisconsin arch A case for hydrothermal diagenesis [J].AAPG Bulletin,2006,90 (11): 1719-1738.
[149]LuoYan, Sun Min, Zhao Guochun et al.,2004. LA-ICP-MS U-Pb zircon ages of the Liaohe Group in the Eastern Block of the North China Craton:constraints on the evolution of the Jiao-Liao-Ji Belt[J]. Precambrian Research 134:349-371.
[150]Malivar.G, Dickson.A.D, Microfacies and diagenetic controls of porosity in Cretaceous/Tertiary chalks, Eldfisk Field, Norwegian North Sea[J]. AAPG Bulletin, 1992,76(11):1825-1838.
[151]Matanof, Barboerim, Nocerasd, et al, Stratigraphy and strontium geochemist ry of Messinian evaporite bearing successions of the southern Apennines foredeep, Italy: implications for the Mediterranean"salinity crisis" and region.
[152]Meilezhikva, Kuzetsovab, Fallickaf, et al, Depositional environments and an apparent age for the Gecimeta limestones:Constraints on the geological history of Northern Mozambique [J]. Precambrian Research,2006,148:19.
[153]Melezhikva, Robertaad, Fallickbae, et al, Geochemical preservation potential of high grade calcite marble versus dolomite marble:implication for isotope chemost ratigraphy [J]. Chemical Geology,2005,216:203-224.
[154]MELIMLA, WESTPHALH, SWARTP.K, et al.Questioning carbonate diagenetic paradigms:evidence from the Neogene of the Bahamas[J]. Marine Geology,2002, 185:27-53.
[155]Meng X H, Ge M, Tucker E. Sequence stratigraphy, sea?_level changes and depositional systems in the Cambro_Ordovician of the North China carbonate platform. Sediment Geol, 1997,114:189-222.
[156]Osleger, D, Read,J.F(1991):Relation of enstasy to stacking patterns of meter-scale carbonate cycles.Later Cambrian[J] U.S.A.-Journal of Sedimentary Petrology,61,1225-1252.
[157]Pricegd.G.R, Ckedr, Strontium isotope stratigraphy and oxygen and carbon isotope variation during the Middle Jurassic Early Cretaceous of the Falkland Plateau,South Atlantic [J]. Palaeogeography Palaeoclimatology Palaeoecology.
[158]Qing Hairuo, Veizer, Oxygen and carbon isotopic composition of Ordovician brachiopods: Implications for coeval seawater[J]. Geochimica et Cosmochimica Acta,1994,58(20) 4429-4442.
[159]Schwarzacher. W(2000):Reptitions and cyclic stratigraphy:Earth-Science Reviews, 50,51-75
[160]Sharma, G.D.1979, The Alakan shelf hydrographic, sedimentary and geochemical enviroment[J], Springer-Verlag New York Inc.
[161]Shields, J. Veizer, et al,2003, Sr, C, and O isotope geochemistry of Ordovician brachiopods: A major isotopic event around the Middle-Late Ordovician transition [J]. Geochimica et Cosmochimica Acta, Vol.67, No.11,pp.2005-2025.
[162]Smith.J.L.B, Davies.G.R. Structurally controlled hydrothermal alteration of carbonate reservoirs:Introduction [J].AAPG Bulletin,2006,90 (11):1635-1640.
[163]Smith.J.L.B. Origin and reservoir characteristics of Upper Ordovician Trenton2Black River hydrothermal dolomite reservoirs in New York [J]. AAPG Bulletin,2006,90 (11):1691-1718.
[164]Steinm, Starinsky.A, Agnon.A, et al. The impact of brine2rock interaction during marine evaporite formation on the isotopic Sr record in the oceans:Evidence f rom Mt Sedom, Israel [J].Geochimica et Cosmochimica Acta,2000,6.
[165]Tuker.M.E. Carbonate diagenesis and sequence stratigraphy[J]. Sedimentology Review, 1993,1993:57-721.
[166]Vahren, Kampvc, Swartpk, New distribution coefficient for the incorporation of st rontium into dolomite and it s implication for the formation of ancient dolomites [J]. Geology, 1990,18:387-391.
[167]Veizer J.1983.Chemical diagenesis of carbonates:theory and application. In:ArthurM A,A anderson T F, Kaplan IR, et al.eds. Stable isotopes in sedimentary geo logy[J]. SEPM Sthort Course,10:3-100.
[168]Veizer.J, Weller.J. M, Strontium as a tool for facies analysis[J]. Journal of sedimentary Petrology,1974,44:93-115.
[169]Wan Yusheng, Song Biao, Liu Dunyi et al,2006. SHRIMP U-Pb zircon geochronology of Palaeoproterozoic metasedimentary rocks in the North China Craton:Evidence for a major Late Palaeoproterozoic tectonothermal even[J]. Precambrian Research 149:249-271.
[170]Wei Wenbo, Ye Gaofeng, Jin Sheng et al.,2008. Geoelectric Structure of Lithosphere Beneath Eastern North China:Features of Thinned Lithosphere from Magnetotelluric Soundings. Earth Science Frontiers 15(4):204-216.
[171]Wiezerbrickir, Daarvis.J, et al, Burial dolomitization and dissolution of Upper J urassic Abenaki platform carbonates, Deep Panuke reservoir, NovaScotia, Canada [J]. AAPG Bulletin,2006,90 (11):1843-1861.
[172]Williams D F.1988. Isotope chronostratigraphy:theory and methods. California:Academic Press.39-68.
[173]Wilson, J.L(1975):Carbonate facies in geologic history.-471., Belin(Springer).
[174]Wrightdt,Waceyd.Sedimentary dolomite:A reality check [C] The Geometry and Pet rogenesis of Dolomite Hydrocarbon Reservoirs[J]. London:Geological Society Special Publication,2004,235:65-74.
[175]Zhao Guochun, When did plate tectonics begin on the North China craton., insights form metamorphism[J]. Earth Science Frontiers,2007.14(1):19-31.
[2]包洪平,杨承运,碳酸盐岩微相分析及其在岩相古地理研究中的意义,岩相古地理,1999,19(6)：60-63.
[3]曹守连.南堡凹陷断裂带构造演化及成藏条件分析.断块油气田,1997,4(2)：13-16.
[4]陈恭洋,何鲜,陶自强,等.千米桥潜山碳酸盐岩古岩溶特征及储层评价[J].天然气地球科学,2003,14(5)：3752379.
[5]陈好寿.同位素地球化学研究[M].杭州：浙江大学出版社,1994.
[6]陈锦石,陈文正,碳同位素地质学概论,北京：地质出版社,1983.
[7]陈永武.储集层与油气分布.北京：石油工业出版社,1995.
[8]成永生,渤海湾盆地南堡凹陷周边地区寒武-奥陶系碳酸盐岩储层研究,[学位论文],中南大学,2008.
[9]成永生,陈松岭,南堡凹陷周边寒武-奥陶系碳酸盐岩储层特征及成岩作用[J].地质找矿论丛2008,23(3)231-235.
[10]丛良滋,周海民.南堡凹陷主动裂谷多幕拉张与油气关系.石油与天然气地质,1998,19(4)：296-301.
[11]戴永定,生物矿物学[M],北京：石油工业出版社,1994.
[12邓俊国,王贤.南堡凹陷构造应力场演化史与油气聚集.保定师专学报,1999,12(2)：72-77.
[13]丁梯平.氢氧同位素地球化学[M].北京：地质出版社,1980.
[14]董月霞,夏文臣,周海民.南堡凹陷第三系火山岩演化序列研究.石油勘探与开发,2003,30(2)：24-26.
[15]董月霞,周海民,夏文臣.南堡凹陷第三系层序地层与油气成藏的关系.石油与天然气地质,2003,24(1)：39-41.
[16]董月霞,周海民,夏文臣.南堡凹陷火山活动与裂陷旋回.石油与天然气地质,2000,21(4)：304-307.
[17]窦立荣,王一刚.中国古生界海相碳酸盐岩油气藏的形成与分布.石油实验地质,2003,25(5)：419-425.
[18]方少仙,董兆雄,侯方浩等.层状白云岩储层特征与成因[M].北京：地质出版社.1999,1-115
[19]费宝生,汪建红.中国海相油气田勘探实例(之三)：渤海湾盆地任丘古潜山大油田的发现与勘探.海相油气地质,2005,10(3)：43-50.
[20]冯洪真,刘家润,施贵军.2000.湖北宜昌地区寒武系-下奥陶统的碳氧同位素记录.高校地质学报,6(1)：106-115.
[21]冯增昭,沉积岩石学(第二版,上、下册)[M].石油工业出版社2004.
[22]冯增昭,单因素分析多因素综合作图-定量岩相古地理重建[J],古地理学 报,2004,6(1),3-19
[23]冯增昭,华北早奥陶世岩相古地理新探[J],地质科学,1979,6(4),302-313.
[24]冯增昭,碳酸盐岩岩相古地理学[M]北京：石油工业出版社,1989.
[25]冯增昭等,鄂尔多斯地区奥陶纪地层岩相古地理[M]北京：地质出版社,1998.
[26]冯增昭等,华北地台早古生代岩相古地理[M],北京：地质出版社,1990.
[27]冯增昭等,下扬子地区中下三叠统青龙群岩相古地理[M],北京：地质出版社,1988.
[28]冯增昭等,中下扬子地区二叠纪岩相古地理[M]北京：地质出版社,1991.
[29]冯增昭等华北地台早古生代岩相古地理[M]北京：地质出版社,1991.
[30]傅学斌,刘蕴华,曹中宏,等.冀东探区潜山油藏形成条件及分布规律研究[J].地质科技情报,2004,23(3)：66-70.
[31]顾家裕,朱筱敏,贾进华等.塔里木盆地沉积与储层[M1.北京：石油工业出版社.2003.1--400.
[32]顾家裕.塔里木盆地下奥陶统白云岩特征及成因(J].新疆石油地质,2000,21(2)：120-122
[33]郭绪杰,焦贵浩.华北古生界石油地质.北京：地质出版社,2002.
[34]韩宝平,陈锁忠,冯启言.任丘油田古潜山储集孔隙特征研究[J].中国矿业大学学报,1997,26(2)：46-51.
[35]韩宝平,刘仁达,罗承建,等.岩溶作用对任丘古潜山碳酸盐岩油藏赋存的控制作用[J]中国岩溶,1998,17(1)：75-80.
[36]韩晋阳,肖军,郭齐军,等.渤海湾盆地南堡凹陷沉降过程、岩浆活动、温压场演化与油气成藏的综合分析[J].石油实验地质,2003,25(3)：257-263.
[37]何自新,杨奕华.鄂尔多斯盆地奥陶系储层图册[MI.北京：石油工业出版社.2004.1-24.4
[38]黄思静,Qing,Hairuo,胡作维等,四川盆地东北部三叠系飞仙关组硫酸盐还原作用对碳酸盐成岩作用的影响[J].沉积学报,2007,25(6)：815-824.
[39]黄思静,裴锡古,谢庆邦.陕甘宁盆地中部奥陶系碳酸盐风化壳中的地开石及其与储层的关系[J].成都理工学院学报,1995,22(3)：43-51.
[40]黄思静,王春梅等,碳酸盐岩成岩作用的研究前沿和值得思考的问题[J],成都理工大学学报(自然科学版),2008,35(1)1-10.
[41]嵇少丞,王茜,许志琴,华北克拉通破坏与岩石圈减薄[J].地质学报,2008.82(2)：174-193.
[42]姜平,王建华.大港地区千米桥潜山奥陶系古岩溶研究[J].成都理工大学学报(自然科学版),2005,32(1)：50-53.
[43]卢鸿,王铁冠,徐新德,等.南堡凹陷原油的有机地球化学特征[J].江汉石油学院学报,1995,20(3)：28-35.
[44]金振奎,邹元荣,等黄骅坳陷奥陶系碳酸盐岩岩溶储层分布规律及其控制因素[J].沉积学报,2001，19(4)530-535.
[45]金振奎.华北地台东部下古生界白云岩的类型及储集性[J].沉积学报,1993,11(2)：11-19.
[46]金之钧.中国海相碳酸盐岩层系油气勘探特殊性问题[J].地学前缘,2005,12(3)：15-22.
[47]李江海,侯贵廷,黄雄南,张志强,钱祥麟,华北克拉通对前寒武纪超大陆旋回的基本制约[J].岩石学报,2001.17(2)：177-186.
[48]李江海,钱祥麟,黄雄南,刘树文,华北陆块基底构造格局及早期大陆克拉通化过程[J].岩 石学报,2000.16(1)：1-10.
[49]李心清,万国江.碳酸盐岩氧、碳稳定同位素地球化学研究目前面临的几个问题[J].地球科学进展,1999.14(3)：262-268.
[50]李振宏,杨永恒等,鄂尔多斯盆地天环北段白云岩体成因及储集性能,海相油气地质[J],2005,10(3)：19-24.
[51]刘波,钱祥麟,王英华,华北板块早古生代构造-沉积演化[J].地质科学,1999.4(3)：347-356.
[52]刘蕴华,周海民,熊保贤等.南堡凹陷的含油气系统分析.石油与天然气地质[J].2000,21(4)：364-365.
[53]卢焕章等.包裹体地球化学[M].北京：地质出版社,1990.
[54]卢武长.稳定同位素地球化学[M].成都：成都地质学院,1986.5.
[55]罗宾巴瑟斯特,碳酸盐沉积物及其成岩作用[M],科学出版社,1980.
[56]吕宝凤,夏斌.关于中国海相碳酸盐岩含油气系统的几点思考[J].天然气地球科学,2005,16(2)：175-177.
[57]吕宝凤,夏斌.中国海相碳酸盐岩地区油气成藏基本特征及勘探系统初探[J].油气地质与采收率,2005,12(s)：21-23.
[58]吕修祥,金之钧.碳酸盐岩油气田分布规律[J].石油学报,2000,21(2)：8-12.
[59]马永生,郭旭升,郭彤楼,等.四川盆地普光大型气田的发现与勘探启示[J].地质论评,2005,51(4)：477-480.
[60]马永生,田海芹.碳酸盐岩油气勘探[M].山东：石油大学出版社,1999.
[61]马永生.中国海相油气田勘探实例之六-四川盆地普光大气田的发现与勘探[J].海相油气地质,2006,11(2)：35-40.
[61]梅博文译.储层地球化学(译文集)[M].西安：西北大学出版社,1992.
[62]梅冥相,华北地台北缘奥陶系亮甲山组的碳酸盐复合海平面变化旋回层序[J],岩相古地理1995，15(5)33-42.
[63]梅冥相,马永生,梅仕龙等.华北寒武系层序地层格架及碳酸盐台地演化[J].现代地质,1997,11(3)：275-252.
[62]牟保磊.元素地球化学[M].北京：清华大学出版社,1999.206-210.
[63]彭澎,翟明国,华北陆块前寒武纪两次重大地质事件的特征和性质[J].地球科学进展,2002.17(6)：818-825.
[64]钱凯,李本亮,许惠中.从全球海相古生界油气地质共性看四川盆地海相地层天然气勘探方向[J].天然气地球科学,2003,14(3)：167-171.
[65]钱峥,黄先雄,碳酸盐岩成岩作用及储层-以中国四川东部石炭系为例[M].北京：石油工业出版社.2000.1-119.
[66]强子同.碳酸盐岩储层地质学[M].东营：石油大学出版社.1998.1-470.
[67]邵济安,牟保磊,张履桥,华北东部中生代构造格局转换过程中的深部作用与浅部响应[J].地质论评,2000.46(1)：32-40.
[68]邵龙义,碳酸盐岩氧、碳同位素与古温度等的关系[J],中国矿业大学学报,1994,23(1)：39-45.
[69]石振荣,葛云龙,秦风启.南堡凹陷北部断裂特征动力学分析[J].断块油气田,2000,7(4)：1-4.
[70]苏立萍,罗平,胡社荣等.苏桥潜山带奥陶系碳酸盐岩储集层研究[J].石油勘探与开发,2003,30(6)：54-57.
[71]谭丽娟,田世澄.南堡凹陷油气运移特征及成藏动力学系统划分[J].石油勘探与开发,2000,27(5)：16-18.
[72]谭丽娟,田世澄.南堡凹陷油气运移特征及成藏动力学系统划分[J].石油勘探与开发,2000,27(5)：16-18.
[73]汤朝阳等.白云石化作用及白云岩问题研究述评[J].东华理工学院学报,2006.9,205-211.
[74]田景春,陈洪德,侯明才等.右江盆地晚古生代白云岩与层序地层的关系及其储集性[J].成都理工大学学报,2004,31(1)：34-39.
[75]汪啸风,陈旭,陈孝红等.中国地层典：奥陶系[M].北京：地质出版社,1996.1-126.
[76]王大锐,白志强.广西中-上泥盆统界线附近的化学地层学特征[J].地层学杂志,2002a.26(1)：50-54.
[77]王大锐,渤海湾地区下古生界碳、氧同位素地球化学研究[J].地质学报2002,3(8)400-408
[78]王刚,窦立荣,文应初等.四川盆地东北部三叠系飞仙关组高含硫气藏H2S成因研究[J].地球化学,2002,31(6)：517-524.
[79]王家豪,王华,王根发.南堡凹陷厚层泥岩的封-盖作用及期与油气的关系石油实验地质,2001,23(4)：418-423.
[80]王家豪,王华,周海民等.断陷湖盆基底非线性沉降与H型层序的形成-以冀东油田南堡凹陷为例[J].石油与天然气地质,2001,22(3)：203-206.
[81]王杰,陈践发.海相碳酸盐岩烃源岩的研究进展[J].天然气工业,2004,24(8)：21-23.
[82]王涛,郑亚东,张进江,华北克拉通中生代伸展构造研究的几个问题及其在岩石圈减薄研究中的意义[J].地质通报,2007.26(9)：1154-1166.
[83]王英华等,化石岩石学[M],北京：中国矿业大学出版社,1990.
[84]威尔逊J L著,冯增昭等译.地质历史中的碳酸盐岩相[M].北京：地质出版社,1981.
[85]魏中文等.南堡凹陷深层石油地质特征及有利勘探目标评价[M].唐山：中石油冀东油田勘探开发研究院,2001.
[86]吴昌华,华北克拉通的变质沉积岩及其克拉通的构造划分[J].高校地质学报,2007.13(3)：442-457.
[87]夏日元,唐健生.黄骤坳陷奥陶系古岩溶发育演化模式[J].石油勘探与开发2004,31(1)：51-53.
[88]项礼文,李善姬,南润善等中国地层(4)[M].中国的寒武系北京地质出版社.1981
[89]许化政,周新科,高金慧,华北盆地中南部早古生代沉积特征及油气成藏条件[J].石油学报,2005.26(5)：10-16.
[90]杨承运,卡罗兹A V,碳酸盐岩实用分类及微相分析[M],北京：北京大学出版社,1988.
[91]杨池银,武站国.千米桥潜山奥陶系碳酸盐岩储层成岩作用与孔隙演化[J].石油与天然气地质,2004,25(3).
[92]永生永平,杨池银,王喜双.渤海湾盆地北部奥陶系潜山油气藏成藏组合及勘探技术.石油勘探与开发,2000,27(5)：1-4.
[93]于学敏,苏俊青,王振升.千米桥潜山油气藏基本地质特征[J].石油勘探与开发.1999,26(6)：7-9.
[94]余家仁,陶洪兴,樊哲仁.华北潜山油藏碳酸盐岩储集层研究[M].北京：石油工业出版社,1993.
[95]翟明国,樊棋诚,华北克拉通中生代下地壳置换：非造山过程的壳慢交换[J].岩石学报,2002.18(1)：1-8.
[96]翟明国,彭澎,华北克拉通古元古代构造事件[J].岩石学报,2007.23(11)：2665-2682.
[97]张锦泉.鄂尔多斯盆地奥陶系沉积、古岩溶及储集特征[M].成都：成都科技大学出版社,1992.
[98]张立平,王东坡,克拉通盆地形成机制及沉积特征[J].世界地质,1994.13(3)：26-31.
[99]张小青,羌塘盆地双湖地区侏罗系自云岩成因及储集性研究[D].成都理工大学,2005.
[100]张小青,伊海生,朱迎堂.羌塘盆地双湖地区白云岩储集层特征研究闭[J].西南石油学院学报,2005,27(5)：10-13.
[101]张振英,邵龙义,柳广第.南堡凹陷无井探区烃源岩评价研究[J].石油勘探与开发,2004,31(4)：64-67.
[102]赵太平,翟明国,夏斌等,熊耳群火山岩锆石SHRIMP年代学研究：对华北克拉通盖层发育初始时间的制约[J].科学通报,2004.49(22)：2342-2349.
[103]赵文智,张光亚,何海清等.中国海相石油地质与叠合含油气盆地[M].北京：地质出版社,2002.
[104]赵宗举,范国章等.中国海相碳酸盐岩的储层类型、勘探领域及勘探战略[J].海相油气地质,2007,12(1)：1-11.
[105]中国科学院地质所主编,化石岩石学图版[S],1981.
[106]钟大康、朱筱敏等,南襄盆地泌阳凹陷溶孔溶洞型白云岩储层特征与分布规律[J],地质论评,2004,50(2)：162-169.
[107]钟长汀,邓晋福,万渝生,毛德宝,李惠民.华北克拉通北缘中段古元古代造山作用的岩浆S型花岗岩地球化学特征及锆石SHRIMP年龄[J].地球化学,2007,36(6)：633-637.
[108]周海民,董尽霞,刘蕴蕴华等.小型断陷盆地油气勘探理论与时间-以渤海湾盆地南堡凹陷为例[M].东营：石油大学出版社,2001.
[109]周海民,董月霞,刘蕴华,等.冀东南堡凹陷精细勘探实践与效果[J].中国石油勘探,2003,8(1)：11-15.
[110]周海民,范文科.高成熟探区深化勘探的潜力与措施-以冀东油田南堡凹陷陆地为例[J].中国石油勘探,2001,6(3)：63-70.
[111]周海民,魏忠文,曹中宏,等.南堡凹陷的形成演化与油气的关系[J].石油与天然气地质,2000,21(4)：345-349.
[112]周海民,张玮,谢占安等.断陷盆地大面积三维叠前时间偏移连片处理的地质意义及关键技术[J].石油地球物理勘探,2005,40(6)：693-699.
[113]周新源,王招明,杨海军,等.中国海相油气田勘探实例之五：塔中奥陶系大型凝析气田的勘探和发现[J].海相油气地质,2006,n(1)：45-51.
[117]周志毅,陈均远,林尧坤等.唐山地区奥陶系的新观察.地层学杂志,1983,7(1)：19-31.
[118]朱光有,张水昌,梁英波等.TSR对深部碳酸盐岩储层的溶蚀改造四川盆地深部碳酸盐岩优质储层形成的重要方式[J].岩石学报,2006,22(8)：2182-2194.
[119]朱夏.论中国含油气盆地构造[M].北京：石油工业出版社,1986.
[120]邹元荣,金振奎,由伟丰,黄骅坳陷奥陶纪岩相古地理[M],古地理学报2002,3(4)：35-44.
[121]Prokoph, G.A. Shields, J. Veizer, Compilation and time-series analysis of a marine carbonateδ18O,δ13C, "Sr/86Sr and δ34S database through Earth history[J], Earth-Science Reviews 87 (2008) 113-133.
[122]Braithwaitec.J.R, Rizzig, Dark.G., The geometry and petrogenesis of dolomite hydrocarbon reservoirs [M]. Geological Society (London) SpecialPublication,2004,235:1-413.
[123]CAI Chunfang, XIE Zengye, Worden.R.H, et al, Methane dominated thermochemical sulphate reduction in the Triassic Feixianguan Formation East Sichuan Basin, China: towards prediction of fatal H2S concent rations [J]. Marine and PetroleumGeology,2004, 21:1265-1279.
[124]Chen Ling, Wang Tao, et.al,2008. Distinct lateral variation of lithospheric thickness in the Northeastern North China Craton. Earth and Planetary Science Letters 267:56-68.
[125]Chend, Qingh, Lir, The Late Devonian Frasnian Famennian (F/F) biotic crisis:Insight of rom δ13 C carb,δ13 Corg and 87 Sr/86 Sr isotopic systematics [J]. Earth and Planetary Science Letters,2005,235:151-166.
[126]DaviesAVIES.G.R, Smith.J.L.B, Structurally cont rolled hydrothermal dolomite reservoir facies:An overview[J]. AAPG Bulletin,2006,90 (11):1641-1690.
[127]Deny L A, BrasierM D, Corfield R M, RozanovA Y,& ZhuravlevA Yu.1994. Sr and C isotopic in Lower Cambrian carbonates from the Siberian Craton:a paleoenvironmental record during the Cambrian explosion[J]. Earth and Planetary Science Letters,128: 671-681.
[128]Derry L A, Kaufaman A J,& Jacobsen S B.1992. Sedimentary cycling and environmental chang in the Late Proeterozoic:evidence form stable and radiogenic isotopes[J]. Geochimica et Cosmochimica Acta,56:1317-1329.
[129]FlugleL著,曾允孚译.石灰岩微相[M].北京：地质出版社,1989.
[130]Flugle著,马永生主译,碳酸盐岩微相-分析、解释及应用北京：地质出版社2006，
[131]Gilliskm, Cooganlat, Pedersen.R, Strontium isotope constraints on fluid flow in the upper oceanic crust at the East Pacific Rise [J]. Earth and Planetary Science Letters,2005, 232:83-94.
[132]Hayton,S., Nelson,S.D. (1995):A skeletal assemblage classification system for non-tropical carbonate depositesbased on New Zealand Cenozoic limestones[J]. Sedimentary Geology,100,123-141.
[133]Horowitz.A.S, Potter.P.E, Introductory petrography of fossils[M]. New York, Springer-Verlag,1971.
[134]FlugleL, Microfacies of carbonate rocks:Analysis, Interpretation and Application [M], New York Inc:Springer 2004.
[135]Feng Zengzhao, Jin Zhenkui. Types and origin of dolostones in the Lower Palaeozoic of the North China Platform[J]. Sedimentary Geology,1994 (93):279-290.
[136]Enos, P. Samankassou.E(1998):Lofer cyclothems reservited (Late Triassic. Northern Alps.Austria).Facies.38.207-228.
[137]Feng Zengzhao, Jin Zhenkui:Types and origin of dolostones of Lower Palaeozoic in the North China Platform[J], Sedimentary Geology,1994,Vol93, Nos.3-4,P.279-290.
[138]James,N.P(1997), The cool-water carbonate depositional realm, In:James,N.P, Clarke, A.D(eds):coole-water carbonates:SEPM special Publictions,56,1-20.
[139]Jean-Jacques.C, Jean-Paul.S.M and Conesa.G et al. Geometry, palaeoenvironments and relative sea-level(accommodation space) changes in the Messinian Murdjtdjo carbonate platform (Orau, western Algeria):consequences[J]. Sedimentary Geology, 1994,89:143-158.
[140]KATZ D A, EBERL I G P, SWART P K, et al.Tectonic-hydrothermal brecciation associated with calcite precipitation and permeability dest ruction in Mississippian carbonate reservoirs, Montana and Wyoming [J]. AAPGBulletin,2006,90.
[141]Kaufman A J & Kno 11 A H.1995. Neoproterozoic variations in the C-isotope composition of seawater:stratigraph ic and biogeochemical implications[J]. Precambrian Research,73: 27-49.
[142]Kaufman A J, Konll A H,& N arbonne G M.1997. Isotopes, iceages and terminal Proterozoic earth history[J]. Preceedings of the National Academy of Sciences,95: 6600-6605.
[143]Lasemi, palaeoenvironments and sequences[J]. Sedimentology,1995,99:151-164.
[144]Lasemi.Y, Platform carbonates of the Upper Jurassic Mozduran Formation in the Kopef Dagh Basin, NE Iran:facies.
[145]Lees.A, Buller.A.T(1972):Modern temperate-water and warm water shelf carbonate sediments contrasted.-Marine Geology,13,M67-M73.
[146]Lonnee.J, Machel.H.G, Pervasive dolomitization with subsequent hydrothermal alteration in he Clarke Lake gas field, Middle Devonian Slave Point Formation, British Columbia, Canada [J]. AAPGBulletin,2006,90 (11):173-1761.
[147]Luczaj.J.A, Harrison.W.B,Wiliams.N.S. Fractured hydrothermal dolomite reservoirs in the Devonian Dundee Formation of the cent ral Michigan Basin [J]. AAPG Bulletin,2006, 90(11):1787-1801.
[148]Luczajj.A, Evidence against the Dorag (mixing zone) model for dolomitization along the Wisconsin arch A case for hydrothermal diagenesis [J].AAPG Bulletin,2006,90 (11): 1719-1738.
[149]LuoYan, Sun Min, Zhao Guochun et al.,2004. LA-ICP-MS U-Pb zircon ages of the Liaohe Group in the Eastern Block of the North China Craton:constraints on the evolution of the Jiao-Liao-Ji Belt[J]. Precambrian Research 134:349-371.
[150]Malivar.G, Dickson.A.D, Microfacies and diagenetic controls of porosity in Cretaceous/Tertiary chalks, Eldfisk Field, Norwegian North Sea[J]. AAPG Bulletin, 1992,76(11):1825-1838.
[151]Matanof, Barboerim, Nocerasd, et al, Stratigraphy and strontium geochemist ry of Messinian evaporite bearing successions of the southern Apennines foredeep, Italy: implications for the Mediterranean"salinity crisis" and region.
[152]Meilezhikva, Kuzetsovab, Fallickaf, et al, Depositional environments and an apparent age for the Gecimeta limestones:Constraints on the geological history of Northern Mozambique [J]. Precambrian Research,2006,148:19.
[153]Melezhikva, Robertaad, Fallickbae, et al, Geochemical preservation potential of high grade calcite marble versus dolomite marble:implication for isotope chemost ratigraphy [J]. Chemical Geology,2005,216:203-224.
[154]MELIMLA, WESTPHALH, SWARTP.K, et al.Questioning carbonate diagenetic paradigms:evidence from the Neogene of the Bahamas[J]. Marine Geology,2002, 185:27-53.
[155]Meng X H, Ge M, Tucker E. Sequence stratigraphy, sea?_level changes and depositional systems in the Cambro_Ordovician of the North China carbonate platform. Sediment Geol, 1997,114:189-222.
[156]Osleger, D, Read,J.F(1991):Relation of enstasy to stacking patterns of meter-scale carbonate cycles.Later Cambrian[J] U.S.A.-Journal of Sedimentary Petrology,61,1225-1252.
[157]Pricegd.G.R, Ckedr, Strontium isotope stratigraphy and oxygen and carbon isotope variation during the Middle Jurassic Early Cretaceous of the Falkland Plateau,South Atlantic [J]. Palaeogeography Palaeoclimatology Palaeoecology.
[158]Qing Hairuo, Veizer, Oxygen and carbon isotopic composition of Ordovician brachiopods: Implications for coeval seawater[J]. Geochimica et Cosmochimica Acta,1994,58(20) 4429-4442.
[159]Schwarzacher. W(2000):Reptitions and cyclic stratigraphy:Earth-Science Reviews, 50,51-75
[160]Sharma, G.D.1979, The Alakan shelf hydrographic, sedimentary and geochemical enviroment[J], Springer-Verlag New York Inc.
[161]Shields, J. Veizer, et al,2003, Sr, C, and O isotope geochemistry of Ordovician brachiopods: A major isotopic event around the Middle-Late Ordovician transition [J]. Geochimica et Cosmochimica Acta, Vol.67, No.11,pp.2005-2025.
[162]Smith.J.L.B, Davies.G.R. Structurally controlled hydrothermal alteration of carbonate reservoirs:Introduction [J].AAPG Bulletin,2006,90 (11):1635-1640.
[163]Smith.J.L.B. Origin and reservoir characteristics of Upper Ordovician Trenton2Black River hydrothermal dolomite reservoirs in New York [J]. AAPG Bulletin,2006,90 (11):1691-1718.
[164]Steinm, Starinsky.A, Agnon.A, et al. The impact of brine2rock interaction during marine evaporite formation on the isotopic Sr record in the oceans:Evidence f rom Mt Sedom, Israel [J].Geochimica et Cosmochimica Acta,2000,6.
[165]Tuker.M.E. Carbonate diagenesis and sequence stratigraphy[J]. Sedimentology Review, 1993,1993:57-721.
[166]Vahren, Kampvc, Swartpk, New distribution coefficient for the incorporation of st rontium into dolomite and it s implication for the formation of ancient dolomites [J]. Geology, 1990,18:387-391.
[167]Veizer J.1983.Chemical diagenesis of carbonates:theory and application. In:ArthurM A,A anderson T F, Kaplan IR, et al.eds. Stable isotopes in sedimentary geo logy[J]. SEPM Sthort Course,10:3-100.
[168]Veizer.J, Weller.J. M, Strontium as a tool for facies analysis[J]. Journal of sedimentary Petrology,1974,44:93-115.
[169]Wan Yusheng, Song Biao, Liu Dunyi et al,2006. SHRIMP U-Pb zircon geochronology of Palaeoproterozoic metasedimentary rocks in the North China Craton:Evidence for a major Late Palaeoproterozoic tectonothermal even[J]. Precambrian Research 149:249-271.
[170]Wei Wenbo, Ye Gaofeng, Jin Sheng et al.,2008. Geoelectric Structure of Lithosphere Beneath Eastern North China:Features of Thinned Lithosphere from Magnetotelluric Soundings. Earth Science Frontiers 15(4):204-216.
[171]Wiezerbrickir, Daarvis.J, et al, Burial dolomitization and dissolution of Upper J urassic Abenaki platform carbonates, Deep Panuke reservoir, NovaScotia, Canada [J]. AAPG Bulletin,2006,90 (11):1843-1861.
[172]Williams D F.1988. Isotope chronostratigraphy:theory and methods. California:Academic Press.39-68.
[173]Wilson, J.L(1975):Carbonate facies in geologic history.-471., Belin(Springer).
[174]Wrightdt,Waceyd.Sedimentary dolomite:A reality check [C] The Geometry and Pet rogenesis of Dolomite Hydrocarbon Reservoirs[J]. London:Geological Society Special Publication,2004,235:65-74.
[175]Zhao Guochun, When did plate tectonics begin on the North China craton., insights form metamorphism[J]. Earth Science Frontiers,2007.14(1):19-31.
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