岩性油气藏 ›› 2026, Vol. 38 ›› Issue (3): 120–131.doi: 10.12108/yxyqc.20260310

• 地质勘探 • 上一篇    下一篇

四川盆地威远地区奥陶系天然气地球化学特征及富集规律

苟哲培1(), 魏倩倩1, 严雪齐1, 隆辉2, 卢嘉勋2, 高儇博1,3(), 唐银海4, 谭先锋1,3   

  1. 1 重庆科技大学 石油与天然气工程学院， 重庆 401331
    2 中国石油西南油气田公司 蜀南气矿， 四川 泸州 646001
    3 复杂油气田勘探开发重庆市重点实验室， 重庆 401331
    4 重庆市地质矿产勘查开发集团 检验检测有限公司， 重庆 400700
  • 收稿日期:2025-12-01 修回日期:2025-12-25 出版日期:2026-05-01 发布日期:2026-02-06
  • 第一作者:苟哲培（1999—），男，重庆科技大学在读硕士研究生，研究方向为油气成藏。地址：（401331）重庆市沙坪坝区大学城东路20号重庆科技大学。Email:gouzhepei@qq.com。
  • 通信作者: 高儇博（1987—），博士，副教授，主要从事油气地球化学和油气成藏研究。Email:gaoxuanbo@cqust.edu.cn。
  • 基金资助:
    国家自然科学基金“挤压高陡褶皱区湖相富有机质页岩差异成岩过程及油气富集机理”(42572138);“挤压构造动力影响下富有机质页岩有机-无机成岩效应及孔隙改造机理”(42202122);重庆科技大学校级科技创新项目“伴生凝析油在气-源对比研究中的应用—以川东凉高山组为例”(YKJCX2420108)

Geochemical characteristics and enrichment rule of natural gas in Ordovician of Weiyuan area, Sichuan Basin

GOU Zhepei1(), WEI Qianqian1, YAN Xueqi1, LONG Hui2, LU Jiaxun2, GAO Xuanbo1,3(), TANG Yinhai4, TAN Xianfeng1,3   

  1. 1 School of Petroleum Engineering, Chongqing University of Science and Technology, Chongqing 401331, China
    2 Shunan Gas Mine, PetroChina Southwest Oil & Gasfield Company, Luzhou 646001, Sichuan, China
    3 Chongqing Key Laboratory of Complex Oil & Gas Exploration and Development, Chongqing 401331, China
    4 Chongqing Geology and Mineral Exploration and Development Group Inspection and Test Co., Ltd., Chongqing 400700, China
  • Received:2025-12-01 Revised:2025-12-25 Online:2026-05-01 Published:2026-02-06

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摘要：

近年来，四川盆地威远地区奥陶系红花园组与宝塔组海相碳酸盐岩中持续获得天然气发现，展现出良好的勘探潜力。通过对天然气组分、碳同位素特征、烃源岩特征、流体包裹体特征以及埋藏-热演化史进行分析，明确了研究区天然气来源和油气充注期次，探讨了其天然气成藏模式及主控因素。研究结果表明：①威远地区奥陶系红花园组和宝塔组天然气干燥系数高，平均为0.995 8，属于过成熟油型气，为干酪根裂解和原油裂解成因的同源不同期混合气，热化学硫酸盐还原反应（TSR）和过高成熟度是导致天然气碳同位素倒转的主要原因；筇竹寺组烃源岩是红花园组和宝塔组天然气的主要供烃层位，烃源岩品质中等—好，总有机碳（TOC）含量平均值为1.90%，生烃潜量（S1 + S2）平均值为 0.27 mg/g，有机质类型为Ⅰ型，处于过成熟阶段，Ro为2.74%~3.28%；岩石热解峰温（Tmax）为397~499 ℃。②研究区奥陶系红花园组和宝塔组在晚二叠世与早白垩世分别形成了古油藏和古气藏，喜山期后气藏发生调整，形成了受大型背斜与走滑断层系统控制的构造-地层-岩性复合气藏，上部红花园组和宝塔组发育以白云岩为主的储层，下部筇竹寺组为其供烃，形成了“下生上储”的成藏模式。③奥陶系红花园组和宝塔组油气成藏主要受控于白云岩储层质量和走滑断层及逆断层的输导能力，背斜圈闭高部位和裂陷槽边缘断层的叠合区是天然气富集“甜点”区。

关键词: 油型气, 碳同位素, 走滑断层, 裂陷槽, 筇竹寺组, 红花园组, 宝塔组, 奥陶系, 威远地区, 四川盆地

Abstract:

In recent years, natural gas resources have been successively discovered in marine carbonate rocks of Ordovician Honghuayuan Formation (O1h) and Baota Formation (O2b) in Weiyuan area of Sichuan Basin, which shows favorable exploration potential. Based on integrated analyses of composition and carbon isotopes of natural gas, source rock features, fluid inclusion characteristics and burial-thermal evolution, the origin of natural gas and hydrocarbon charging episodes in the study area were determined, and hydrocarbon accumulation models along with its controlling factors for Ordovician natural gas were explored. The results show that： （1） Ordovician O1h and O2b natural gases in Weiyuan area exhibit high dryness coefficient, with an average value of 0.995 8，and belong to over-mature oil-type gas, they are mixed gases derived from both kerogen cracking and crude oil cracking, formed at different stages but from the same source. The carbon isotope reversal in the natural gas primarily results from thermochemical sulfate reduction (TSR) and over-mature background. Hydrocarbon source rocks of Є1q serve as the main hydrocarbon supply layers for the natural gas in O1h and O2b. Є1q source rocks have medium-good quality, with an average total organic carbon (TOC) of 1.90% and a mean hydrocarbon generation potential (S1 + S2) of 0.27 mg/g. The organic matter type is Type I, indicating over-maturity, with Ro of 2.74%-3.28% and Tmax of 397-499 ℃. （2） In the study area, O1h and O2b formed paleo-oil reservoirs and paleo-gas reservoirs during Late Permian and Early Cretaceous, respectively. After the Himalayan orogeny, gas reservoirs underwent structural adjustment, forming structural-stratigraphic-lithological composite reservoirs controlled by large-scale anticline and strike-slip fault system. Reservoir rocks developed in upper O1h and O2b predominantly composed of dolomite, while the lower Є1q supplied hydrocarbons, forming a hydrocarbon accumulation model of “lower-generation and upper-storage”. （3） Hydrocarbon accumulations of Ordovician O1h and O2b are mainly controlled by the quality of dolomite reservoirs, and the migration capacity of strike-slips and reverse faults. The “sweet spots” for natural gas enrichment are overlapping zones of high parts of anticlinal traps and the faults along the aulacogen margin.

Key words: oil-type gas, carbon isotope, strike-slip fault, aulacogen, Qiongzhusi Formation, Honghuayuan Formation, Baota Formation, Ordovician, Weiyuan area, Sichuan Basin

中图分类号: 

  • TE122

图1

四川盆地威远地区奥陶系宝塔组顶面构造位置（a）与下古生界岩性地层综合柱状图（b）（据文献[20]修改）"

表1

四川盆地威远地区下古生界天然气组分"

井名 层位 ϕ(组分)/% 干燥系数 ln（C1/C2） ln（C2/C3）
CH4 C2H6 C3H8 CO2 N2 H2S
威201 志留系龙马溪组 97.91 0.59 0.021 0.88 0.62 — 0.993 8 5.11 3.34
威201 志留系龙马溪组 97.85 0.66 0.029 0.97 0.59 — 0.993 0 5.00 3.12
威201 志留系龙马溪组 97.59 0.52 0.022 1.06 0.61 — 0.994 5 5.23 3.16
威201 志留系龙马溪组 98.51 0.51 0.021 0.45 0.67 — 0.994 6 5.26 3.19
威201 志留系龙马溪组 96.89 0.68 0.023 0.57 2.14 — 0.992 8 4.96 3.39
威201 志留系龙马溪组 99.14 0.46 — 0.42 — — 0.995 4 — —
威201 志留系龙马溪组 98.64 0.42 0.016 0.38 0.64 — 0.995 6 5.46 3.27
威201 志留系龙马溪组 97.43 0.49 0.021 0.49 1.51 — 0.994 8 5.29 3.15
威寒1 奥陶系宝塔组 96.56 0.52 — 1.68 — 0.68 0.994 6 5.22 —
威97 奥陶系宝塔组 96.21 0.57 — 1.58 — 0.50 0.994 1 5.13 —
威93 奥陶系宝塔组 97.45 0.47 — 1.58 — 0.46 0.995 2 5.33 —
威93 奥陶系宝塔组 92.95 0.36 0.003 3.69 — 0.73 0.996 1 5.55 4.67
威93 奥陶系宝塔组 91.12 0.41 0.006 1.43 — 2.59 0.995 5 5.40 4.23
威探1H 奥陶系红花园组 90.23 0.22 0.002 0.08 — 1.07 0.997 5 6.01 4.97
威探1H 奥陶系红花园组 91.24 0.25 0.002 0.07 — 1.22 0.997 2 5.90 5.10
威201 寒武系筇竹寺组 96.19 0.34 — 1.04 2.25 — 0.996 5 5.65 —
威201 寒武系筇竹寺组 96.61 0.36 — 1.13 1.79 — 0.996 3 5.59 —
威201 寒武系筇竹寺组 96.29 0.32 — 1.26 1.96 — 0.996 7 5.71 —
威201 寒武系筇竹寺组 96.52 0.33 — 1.21 1.82 — 0.996 6 5.68 —
威201 寒武系筇竹寺组 96.39 0.36 — 1.09 2.08 — 0.996 3 5.59 —
威201 寒武系筇竹寺组 96.62 0.35 — 1.13 1.82 — 0.996 4 5.62 —
威201 寒武系筇竹寺组 96.55 0.32 — 1.31 1.79 — 0.996 7 5.71 —

表2

四川盆地威远地区下古生界天然气碳同位素组成"

井名 层位 δ13C/‰
C1 C2 C3
威201 志留系龙马溪组 -37.55 -37.78 —
威201 志留系龙马溪组 -36.65 -37.73 -33.26
威201 志留系龙马溪组 -36.69 -37.67 —
威201 志留系龙马溪组 -35.94 -40.67 -41.86
威201 志留系龙马溪组 -36.71 -40.95 -42.56
威201 志留系龙马溪组 -36.78 -42.75 —
威201 志留系龙马溪组 -35.88 -40.06 —
威201 志留系龙马溪组 -36.12 -36.60 -35.20
威寒1 奥陶系宝塔组 -33.22 -37.67 —
威97 奥陶系宝塔组 -31.61 -36.41 —
威93 奥陶系宝塔组 -31.78 -34.29 —
威93 奥陶系宝塔组 -32.26 -33.45 —
威93 奥陶系宝塔组 -31.41 -33.57 —
威93 奥陶系宝塔组 -32.14 -34.29 —
威93 奥陶系宝塔组 -32.52 -36.76 —
威探1H 奥陶系红花园组 -33.54 -34.82 —
威探1H 奥陶系红花园组 -32.78 -35.69 —
威201 寒武系筇竹寺组 -34.91 -35.68 —
威201 寒武系筇竹寺组 -35.41 -36.89 —
威201 寒武系筇竹寺组 -34.43 -38.54 —
威201 寒武系筇竹寺组 -34.51 -39.45 —
威201 寒武系筇竹寺组 -33.57 -39.11 —
威201 寒武系筇竹寺组 -33.74 -37.46 —
威201 寒武系筇竹寺组 -34.58 -38.02 —

图2

四川盆地威远地区下古生界天然气δ13C2与δ13C1交会图（据文献[32]修改） 注：Ⅰa. 成熟油型气；Ⅰb. 成熟油型气-煤成气混合气；Ⅰc. 成熟煤成气；Ⅱa. 高成熟油型气；Ⅱb. 高成熟油型气-煤成气混合气；Ⅱc. 高成熟煤成气；Ⅲa. 过成熟油型气；Ⅲb. 过成熟油型气-煤成气混合气；Ⅲc. 过成熟煤成气。"

图3

四川盆地威远地区下古生界天然气干酪根与原油裂解气成因判识（据文献[31]修改）"

图4

四川盆地威远地区下古生界天然气碳同位素组成"

图5

四川盆地威远地区下古生界天然气甲烷、乙烷和丙烷碳同位素组成及成因判识（据文献[26]修改） 注：Ⅰ. 煤成气区；Ⅱ. 油型气区；Ⅲ. 碳同位素系列倒转混合区； Ⅳ. 煤成气和（或）油型气区；Ⅴ. 生物气和亚生物气区。"

图6

四川盆地威远地区下古生界天然气碳同位素组成及气源判识"

图7

四川盆地威远地区寒武系筇竹寺组烃源岩有机质丰度与生烃潜量交会图"

图8

四川盆地威远地区寒武系筇竹寺组烃源岩成熟度"

图9

四川盆地威远地区奥陶系储层薄片和岩心照片 （a） 溶蚀作用发育，可见微裂缝和粒内溶孔，砂质鲕粒白云岩，红花园组，威寒1井，2 072.38 m；（b） 可见粒内溶孔，砂质鲕粒生屑白云岩，红花园组，威探1H井，1 800.49~1 800.75 m；（c） 发育粒内溶孔、晶间孔，砂质泥粉晶云岩，红花园组，威探1H井，1 802.40~1 802.58 m；（d） 发育溶蚀缝，残余生屑白云岩，宝塔组，威寒105井，1 810.00 m；（e） 发育晶间孔，存在沥青充填，粉—细晶白云岩，宝塔组，威寒101井，1 750.00 m；（f） 发育构造缝，含白云质生屑灰岩，宝塔组，威探1H井，1 527.04~1 527.22 m。"

图10

四川盆地威远地区威寒102井奥陶系储层盐水包裹体照片 （a） 石英颗粒内盐水包裹体带状分布，共生的气烃包裹体荧光无显示，2 199 m;（b） a图样品的荧光照片图;（c） 石英颗粒内盐水包裹体成群分布，共生的沥青包裹体荧光显示为黄白色，2 199 m;（d） c图样品的荧光照片图。"

图11

四川盆地威远地区奥陶系储层均一温度分布特征"

图12

四川盆地威远地区寒武系筇竹寺组—奥陶系埋藏-热演化史（a）和Ro模拟曲线（b）"

图13

四川盆地威远地区奥陶系成藏模式"

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