Thermal Regime and Paleogeothermal Gradient Evolution of Mesozoic-Cenozoic Sedimentary Basins in the Tibetan Plateau, China
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摘要: 尽管前人对青藏高原隆升机制、地块拼合和陆内俯冲、中-下地壳流动以及岩浆活动等过程做了大量研究, 但对工区发育众多的中-新生代沉积盆地热体制和古地温梯度演化很少涉及, 而这些对中生代海相烃源岩油气生成过程以及已生成的油气命运具有重要影响.在总结前人有关青藏高原温度场背景和盆地类型演化成果基础之上, 运用流体包裹体均一温度测定数据, 综合建立了高原腹部中生代海相盆地古地温梯度演化曲线, 认为在中生代至古近纪的被动陆缘-弧后盆地-前陆盆地演化过程中, 中生代海相盆地处于相对低的地温梯度条件下(＜3.0 ℃/100 m)有利于成熟油的生成; 在新近纪至第四纪的青藏高原隆升阶段, 这些中生代海相盆地不仅演化成残留盆地, 而且还伴随着新的热事件使得盆地地温梯度不均匀急剧上升(~6.5 ℃/100 m), 同时会导致大部分中生代海相烃源岩生成的油再度裂解成气和存在二次生烃(气)的可能性.因此, 古地温梯度演化决定了在"冷盆"区域可能还存在找油潜力, 但在大部分的"热盆"区域只能以找气为主.Abstract: Although many scholars have done a lot of research on the uplift mechanism of Tibet plateau, intercontinental subduction, mid-low crust flowing and magmatic activities, the thermal regime and paleogeothermal gradient evolution in the Mesozoic-Cenozoic sedimentary basins have rarely been studied. But the thermal regime and evolution of paleogeothermal gradient have great significance for the hydrocarbon generation processes and hydrocarbon preservation of the Mesozoic marine source rocks. On the basis of achievements of the previous research on the temperature field of Tibet plateau and evolution of basin types, using the fluid inclusion homogenous temperature, the paleogeothermal gradient evolution curves of the Mesozoic marine basins in Tibet plateau are formed in this paper. And it suggests that the Mesozoic marine basins in the low paleogeothermal gradient (< 3.0 ℃/100 m) when they were in the evolution process from continental margin rift basins to back-arc basins and then to foreland basins during Mesozoic to Eocene, which were beneficial for the generation of mature oil. After that these basins evolved into residual basins and the paleogeothermal gradient rising sharply (~6.5 ℃/100 m) because of continuous and periodic uplifts of the Tibet plateau during Neogene to Quaternary, which resulted in the possibility of that the oil reservoir was cracked into natural gas and secondary hydrocarbon generation of the Mesozoic marine source rocks. Therefore, the paleogeothermal gradient evolution determines the exploration potential for oil in the cooling basin and the exploration potential for gas in the heating basin.
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图 1 青藏高原构造分区和沉积盆地分布
Fig. 1. Tectonic division and distribution of sedimentary basin in the Tibetan plateau
图 2 青藏地区各地块低速低阻体分布及管状流流动方向(据Klemperer, 2006修改)
Fig. 2. Distribution of low-speed and conductor block and direction of channel flow in the Tibetan plateau
图 3 青藏地区各地块大地热流值分布(据付孝悦, 2004修改)
Fig. 3. Distribution of geothermal data of different blocks in the Tibetan plateau
图 4 运用流体包裹体均一温度求取古地温梯度方法
Fig. 4. Obtain paleogeothermal gradient using homogenous temperature of fluid inclusion
图 5 青藏高原中-新生代盆地烃类包裹体观察结果
a.措勤盆地洞错-措勤AA'剖面, 丁青湖组(E3d)含砾粗砂岩石英颗粒内裂纹和石英次生加大边中分别发育浅黄色和蓝白色荧光油包裹体, 指示成熟和高成熟两期油充注；b.措勤盆地洞错-措勤AA'剖面, 丁青湖组(E3d)含砾粗砂岩石英颗粒内裂纹和穿石英颗粒裂纹中分别发育浅黄色和蓝白色荧光油包裹体, 指示成熟和高成熟两期油充注；c.措勤盆地洞错-措勤AA'剖面, 下拉组(P2x), 重结晶灰岩中方解石脉裂纹中见发弱蓝白色荧光凝析油和纯气相包裹体；d.昌都盆地肯通(T3bg)地层剖面, 巴贡组(T3bg)灰色细砂岩.穿石英颗粒裂纹中见不发荧光纯气相包裹体
Fig. 5. Hydrocarbon fluid inclusion in the Mesozoic-Cenozoic sedimentary basins of Tibetan plateau
表 1 青藏高原地温梯度结果统计
Table 1. Geothermal gradient data statistics in the Tibetan plateau
地区 今地温梯度
(℃/100 m)古地温梯度
(℃/100 m)方法 资料来源 岗巴地区 6.5 3.0(＞40 Ma) TTI法 曾华盛和王津义, 2003 藏南普莫雍湖 13.83~32.43 实测 沈显杰, 1989 藏南羊卓雍湖 13.83~32.43 实测 沈显杰, 1989 冈底斯弧后逆掩带和
前陆盆地3.5~4.5
(早侏罗世, 195.9±3 Ma)206Pb/238U法 Pullen et al., 2008 拉萨河谷 3.8 实测 李廷栋, 1995 羊八井热田 1.94~5.88
(810~1 580 m)ZK308孔实测 徐纪人等, 2005 拉多岗地热区 6.53~12.48
(20~200 m)ZK203孔实测 徐纪人等, 2005 羊应乡热田 16~53
(40~230 m)ZK201和CHK2孔实测 Francheteau et al., 1984 当雄-南木林断裂带 4.0 实测 潘作枢, 1984 5.0~7.0 Ro-Tmax模型法 付孝悦, 2004 伦坡拉盆地 4.5~6.0 实测 付孝悦, 2004 6.0~7.2 7.0~9.0(渐新世) Ro-Tmax模型法 袁彩萍和徐思煌, 2000 5.0~6.3 7.0~8.5(始新世) Ro-Tmax模型法 袁彩萍和徐思煌, 2000 羌塘盆地拉雄错、董怀桑、隆鄂尼、野牛沟及安多及雀莫错等地区 1.5 T~J: 2.63~2.65
3.0(＞1.6 Ma)
1.5(＜1.6 Ma)Ro-Tmax模型法
Ro-Tmax模型法
Ro-Tmax模型法王剑等, 2004
王剑等, 2004
王剑等, 2004北羌塘坳陷东部雀莫错剖面 2.7 1.72~1.86(51~38 Ma)
2.7(＜3.5 Ma)Ro模拟、流体包裹体和
裂变径迹法许怀先和秦建中, 2004 南羌塘坳陷东部 1.58~1.66(＞81 Ma)
1.72(51~38 Ma)Ro模拟、流体包裹体和
裂变径迹法秦建中, 2006 羌塘盆地 2.73 2.73(中-新生代) Ro-Tmax模型法 王纪祥等, 2003 1.5~1.8(中生代) 流体包裹体法 王纪祥等, 2003 羌塘盆地赤布张错多 2.76(侏罗纪) 流体包裹体法 王成善等, 2001 尔索洞错 2.72(侏罗纪) 王成善等, 2001 依仓玛剖面 4.0~4.5(侏罗纪) 磷灰石裂变径迹技术和
包裹体法王成善等, 2001 乌兰乌拉湖地区 3.7~5.4(白垩纪) 王成善等, 2001 依仓玛-毛毛山剖面 2.45~5.20 Ro-Tmax模型法 王成善等, 2001 全区热模拟值 2.54~2.82 综合方法 王成善等, 2001 全区平均值 2.47~2.49 王成善等, 2001 3.0 3.0(中-新生代) 类比方法 吴孔友等, 1999 K: 2.73 流体包裹体法 高瑞祺和赵政璋, 2001 措勤盆地 3.4~4.0 K1d: 2.28~2.66
(96.4~88.9 Ma)
K1d: 2.07~2.25
(80.4~63.1 Ma)流体包裹体法
流体包裹体法本文
本文K1d: 3.08 流体包裹体法 本文 比如盆地 3.5~4.5 J2-3l: 3.15 流体包裹体法 本文 (128.2~113.0 Ma) T: 2.22~2.39 流体包裹体法 本文 (188.6~181.8 Ma) T: 2.54 流体包裹体法 本文 (174.0~156.9 Ma) 昌都盆地 5.0~6.0 T: 2.02~2.39 流体包裹体法 本文 (149~135 Ma) T: 1.86~2.07 流体包裹体法 本文 (127.1~115.9 Ma) 松潘-阿坝地区 2.7 6.0~7.0(晚三叠世) Ro-Tmax模型法 赵永庆, 2008 柴达木盆地 2.0~3.3 实测 Qiu et al., 2003 
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表 2 措勤盆地盐湖-捷嘎剖面多尼组(K1d)古地温数据
Table 2. Paleogeothermal data of Duoni Formation (K1d) in the Yanhu-Jiega Section in Cuoqin basin
样品编号 层位 古埋深(m) 第二期盐水包裹体 第三期盐水包裹体 Thmin(℃) Thmax(℃) Thmin(℃) Thmax(℃) XZ-4-3 K1d 1 980 115.6 142.0 164.0 170.0 QZ-8 K1d 2 400 118.9 126.9 177.5 181.1 XZ-4-2 K1d 3 200 136.1 156.9 193.3 198.7 XZ-4-4 K1d 3 200 139.7 - - 198.9 XZ-4-1 K1d 3 800 156.9 163.3 206.1 208.0 XZ-5-1 K1d 3 800 - - - 212.2
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表 3 比如盆地拉孜剖面多尼组(K1d)和央青剖面拉贡塘组(J2-3l)古地温数据
Table 3. Paleogeothermal data of Duoni Formation (K1d) in the Lazi Section in Biru basin
样品编号 层位 古埋深(m) 第一期盐水包裹体 第一期古地温梯度(℃/100 m) Thmin(℃) Thmax(℃) QZ-64 K1d 1 200 90.8 107.6 3.08 QZ-65 J2-3l 1 600 103.1 120.2 3.15
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表 4 昌都盆地侏罗系剖面(J1ch)、肯通剖面(T3bg)、都兰多剖面(T3b)和妥坝剖面(T3j)古地温数据
Table 4. Paleogeothermal data of Jurassic Section (J1ch), Kentong Section (T3bg), Duolanduo Section (T3b) and Tuoba Section (T3j) in Changdu basin
样品编号 层位 古埋深(m) 第一期盐水包裹体 第二期盐水包裹体 第三期盐水包裹体 第四期盐水包裹体 Thmin(℃) Thmax(℃) Thmin(℃) Thmax(℃) Thmin(℃) Thmax(℃) Thmin(℃) Thmax(℃) QZ-52 J1ch 3 900 - - - - 112.1 122.8 141.4 156.2 QZ-47 T3bg 4 800 - - - - 130.4 144.4 153.3 167.9 QZ-48 T3bg 4 800 - - - - - - 157.7 168.8 QZ-51 T3bg 5 180 - - - - 137.9 153.4 170.2 182.3 QZ-37 T3b 5 440 92.0 105.2 112.1 - - - - - QZ-44 T3j 5 900 103.0 115.4 123.8 - - - - -
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