岩性油气藏 ›› 2026, Vol. 38 ›› Issue (2): 12–31.doi: 10.12108/yxyqc.20260202

• 地质勘探 • 上一篇    下一篇

中国陆上中小盆地群发育特征与油气勘探方向

杨占龙1,2(), 郝彬1,2, 谭开俊1,2, 张晶1,2, 张丽萍1,2, 廖建波1,2, 李在光1,2, 史江龙1,2   

  1. 1 中国石油勘探开发研究院 西北分院， 兰州 730020
    2 中国石油集团油藏描述重点实验室， 兰州 730020
  • 收稿日期:2025-02-20 修回日期:2025-09-01 出版日期:2026-03-01 发布日期:2026-01-27
  • 第一作者:杨占龙（1970—），男，博士，教授级高级工程师，主要从事陆相湖盆油气地质综合评价与岩性油气藏勘探技术方面的研究工作。地址：（730020）甘肃省兰州市城关区雁儿湾路535号。Email:yang_zl@petrochina.com.cn。
  • 基金资助:
    中国石油天然气股份有限公司油气与新能源分公司项目“含油气盆地整体研究与战略选区评价”(2025YQXN202)

Geological features and hydrocarbon exploration directions of medium to small-scale basin group, onshore China

YANG Zhanlong1,2(), HAO Bin1,2, TAN Kaijun1,2, ZHANG Jing1,2, ZHANG Liping1,2, LIAO Jianbo1,2, LI Zaiguang1,2, SHI Jianglong1,2   

  1. 1 Research Institute of Petroleum Exploration & Development-Northwest （NWGI）, PetroChina， Lanzhou 730020, China
    2 Key Laboratory of Reservoir Description, CNPC, Lanzhou 730020, China
  • Received:2025-02-20 Revised:2025-09-01 Online:2026-03-01 Published:2026-01-27

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摘要：

中国陆上中小盆地总体认识程度低、勘探程度不高，油气资源潜力与勘探方向不明确，但部分盆地已取得大规模油气发现。通过将全国中小盆地纳入同一盆地类型进行整体对比研究，探讨了中小盆地油气富集的关键控制因素，进而进行中小盆地勘探战略选区与有利盆地优选，以明确中小盆地勘探方向。研究结果表明：①构造域背景及构造活动过程是影响中小盆地以盆地群特征发育的关键控制因素，在较大稳定构造域周缘以发育快速沉降形成的原生型沉积盆地群为主，在活动带内部及其周缘主要发育改造残留型沉积盆地群，在多期次构造活动区域多发育叠置型沉积盆地群。②原生型盆地主要发育中—新生界湖-沼相煤系地层和湖相泥质烃源岩系，以Ⅱ—Ⅲ型有机质为主，部分盆地有机质丰度达0.5%以上，但不同盆地、不同层系及相同层系不同部位成熟度变化大；部分改造残留型盆地发育古生界海相或海陆过渡相碳酸盐岩、泥质烃源岩系，以Ⅰ—Ⅱ型有机质为主，部分盆地有机质丰度达到0.3%以上，成熟度较高，处于成熟—过成熟阶段；中下组合是叠置型盆地烃源岩发育的主要层系。③决定部分中小盆地富集油气的主要因素包括：原生型盆地经历了完整的湖盆填充演化过程，改造残留型盆地遭受的抬升和剥蚀作用没有破坏成盆期优质烃源岩的主体部分，叠置型盆地往往具备优质烃源岩成熟与保存的后期改造过程，均经历了后期的深埋作用；盆地区具有以高地温梯度为特征的深部热背景，有利于烃源岩成熟、油气规模运移和生成烃类的有效保存。④中国陆上环鄂尔多斯盆地周缘部分原生型盆地、泛河西地区部分改造残留型盆地、沿郯庐断裂带发育的部分走滑-拉分盆地、南方部分后期改造程度低的古生界残留盆地和新生代发育的原生型盆地、西部较稳定区域发育的部分叠置型盆地中下组合均具备良好的油气勘探潜力。近源勘探或顺流体运移优势路径开展探索是中小盆地油气勘探必须把握的关键，中小盆地已构成中国陆上油气勘探战略选区的重要接替领域。

关键词: 中小盆地群, 构造活动, 湖-沼相煤系地层, 原生型盆地, 改造残留型盆地, 叠置型盆地, 环鄂尔多斯盆地, 泛河西地区, 郯庐断裂带, 南方扬子区

Abstract:

The overall understanding of medium to small-scale basins onshore China is low, with not high degree exploration, and hydrocarbon potential and exploration direction remain unclear, but some basins have achieved large-scale oil and gas discoveries. By incorporating medium to small-scale basins across the country into a same basin type for overall systematic comparison, key geological factors for hydrocarbon accumulation in medium to small-scale basins were explored, and then strategic selection and favorable basin optimization for exploration in medium to small-scale basins were carried out to clarify the exploration direction. The results show that: （1） Tectonic domain and their activity process are key controlling factors that determine geological features of medium to small-scale basins in group. Primary basin groups are mainly developed in periphery of the relative large and stable tectonic domain, transformed remnant basins are mainly developed within the tectonically active zones and superimposed basins are mostly developed in areas experienced multi-phase tectonic activity. （2） Primary basins mainly develop Meso-Cenozoic lake-marsh coal measure strata and lacustrine mudstone source rocks, mainly with Ⅱ-Ⅲ type organic matter, and the abundance in some of basins are more than 0.5%, but the maturity in different basins, different strata and different parts of the same strata varies greatly. Partial transformed remnant basins develop source rock of Paleozoic marine or marine-terrestrial transitional carbonate and mudstone, mainly with Ⅰ-Ⅱ type organic matter, and the abundance in some of basins are more than 0.3%, and the overall maturity is high and in maturity to over-maturity phase. Source rocks in superimposed basins mainly develop within middle to lower assemblages. （3） Main factors that determine the enrichment of hydrocarbon in some medium to small-scale basins include: The primary basin has undergone a complete lake-basin infilling evolution, the uplift and erosion to the transformed remnant basin did not destroy the main part of high-quality source rocks, the late transformation of superimposed basin are favorable for the maturing and preserving of high-quality source rock. Which have undergone deep burial in late period. The basin region has deep thermal background, characterized by high geothermal gradients, which are conducive to the maturing of source rocks, large-scale migration of hydrocarbon and effective preservation of generated hydrocarbons. （4） Primary basins surrounding Ordos Basin, some transformed remnant basins in Pan-Hexi region, some strike-slip and pull apart basins along Tan-Lu fault zone, some Paleozoic remnant basins with lower degree of late modification and Cenozoic primary basins in the South, and middle to lower assemblages of some superimposed basins in stable areas of West are favorable for hydrocarbon exploration onshore China. The near-source exploration or along dominant paths of fluid migration is the key to hydrocarbon exploration in medium to small-scale basins, medium to small-scale basins have become an important replacement domain for onshore hydrocarbon exploration strategic selection of China.

Key words: medium to small-scale basin group, tectonic activity, lake-marsh coal measure strata, primary basins, transformed remnant basins, superimposed basins, periphery of Ordos Basin, Pan-Hexi region, Tan-Lu fault zone, southern Yangtze region

中图分类号: 

  • TE121.13

图1

中国陆上古生代板块构造域划分与现代沉积盆地分布（构造域界线据文献[2]修改）"

表1

中国陆上主要中小盆地主力烃源岩发育特征统计表"

盆地 坳陷/
凹陷/
次凹		 面积/
km2		 源岩
时代		 现今地
温梯度/
（°C·100 m-1）		 古地温梯度
（°C·100 m-1）		 岩性 累计厚度/m 平均
TOC/%		 氯仿“A”/
%		 总烃量/10-6 生烃门限
深度/m		 有机质
类型		 Ro/% （S1 + S2）/
（mg·g-1）		 参考文献
酒西 青南次凹 170 K1 2.80 3.75~4.50 泥岩、泥灰岩 2 600.00~3 000.00 1.68 1.253~1.332 772.00~890.00 3 000~4 000 Ⅱ 0.60~1.50 5.87 文献[17]
酒东 营尔 8 400 K1 3.00 3.75~4.20 泥岩、泥灰岩 800.00 0.82 0.052 — — Ⅱ，Ⅲ 0.70~1.20 2.22 文献[18]
雅布赖 小胡子 2 525 J2 2.76 2.80~3.40 泥岩 60.00~582.00 1.25~1.50 0.037~0.425 — — Ⅰ，Ⅱ 0.77~1.50 6.00 文献[19]
潮水 金昌 2 340 J2 2.00~2.80 — 泥岩 5.00~55.00 2.99 0.255 1 373.00 1 200~2 000 Ⅰ，Ⅱ1 0.50~0.70 15.96 文献[20]
民和 巴州 11 200 J2 3.50 2.50~5.10 泥岩、煤 800.00 3.69 0.212 — — Ⅰ，Ⅲ 0.59~0.79 0.69~16.81 文献[21]
二连 乌里雅斯 2 000 K1 3.00~3.80 — 泥岩 1 500.00 1.40~2.92 0.050~0.100 — 1 900~2 000 Ⅰ，Ⅱ 0.50~1.20 2.49~15.56 文献[22]
银额 天草 1 900 K1 2.00~3.00 — 泥岩 300.00 1.10 0.150 — 1 500 Ⅱ1，Ⅱ2 0.60~1.30 3.25 文献[23]
中口子 5 300 J1-2、K 3.00~4.00 — 泥岩 1 157.67 0.75~4.03 0.120~0.905 368.00~2 123.00 — Ⅰ，Ⅱ2 0.60~1.20 4.92~6.22 文献[24-26]
六盘山 7 000 K1 3.50~4.50 5.10~6.00 泥岩、泥灰岩 100.00~1 167.50 0.41~3.91 0.140 — — Ⅰ，Ⅱ 0.56~0.75 0.14~20.32 文献[27-28]
J 泥岩 600.00 0.77~5.19 0.106 — — Ⅱ，Ⅲ 0.79~1.38 0.12~35.00
河套 临河 22 400 K1g 2.70~2.90 2.70~2.90 泥岩 250.00 1.29 0.004~1.315 103.00~15.99 3 000~3 400 Ⅱ2，Ⅰ 1.00~1.25 0.73~0.79 文献[12,29]
E3 泥岩 650.00 0.76 0.005~1.847 8.49~4 079.60 3 400~3 600 Ⅱ2，Ⅰ 0.80 —
三门峡 灵宝 1 647 E 2.90~3.80 3.79 泥岩、泥页岩 240.00 1.00~3.00 — — — Ⅰ，Ⅱ 0.50~1.30 0.20~5.10 文献[30]
三塘湖 马朗 20 000 C 2.40 4.40 泥岩 50.00 4.72 0.550 — — Ⅰ，Ⅱ 1.00~1.70 11.79 文献[18]
P 2.40 5.20 泥岩、煤 700.00 7.22 0.410 — — Ⅱ，Ⅲ 0.60~0.80 45.22
J 2.40 3.16~3.93 泥岩、煤 450.00 2.53 0.090 — — Ⅱ 0.50~0.80 3.97
焉耆 13 000 J 2.60~4.00 4.00 泥岩、煤 1 500.00 2.88 1.970 656.00 — Ⅲ 0.70~1.20 6.23 文献[7]
敦煌 40 000 J1-2 1.50~2.00 — 泥岩、煤 50.00~140.00 1.00~3.00 0.125 — — Ⅱ，Ⅲ 0.60~1.20 2.19 文献[8]
伊犁 28 500 P 1.80~2.50 — 炭质泥岩 600.00~700.00 2.83 1.000 — — Ⅱ1，Ⅲ 0.60~1.40 0.02~17.35 文献[31]
库木库里 梯子梁 4 800 E 4.50~6.50 — 泥岩 140.00 0.40~1.32 0.001~0.006 — — Ⅲ 0.47~0.70 0.81 文献[32]
突泉 2 360 J、P 3.60~4.30 — 泥岩 66.00 1.37~3.70 0.006 7.73~37.58 — Ⅱ1 1.19~7.85 0.11~5.39 文献[33-34]
扎鲁特 5 098 P — — 泥岩 — 0.40~1.14 0.030~0.073 — — Ⅲ 1.38~2.80 0.03~0.75 文献[35]
乌兰盖 3 100 J — — 泥岩 — 0.59~4.92 0.078~0.443 — — Ⅱ1 0.60~1.79 0.05~61.03 文献[36]
伊通 岔路河 1 350 E 3.36 4.68 泥岩 1 200.00 0.80~1.50 0.090 1 950.00 1 600 Ⅱ2，Ⅲ 0.60~1.50 19.28
鹿乡 310 E 3.62 4.45 泥岩 1 134.00 0.80~1.50 0.074 3 380.00 1 750 Ⅱ，Ⅲ 0.50~1.10 2.63
莫里青 540 E 3.52 3.74 泥岩 1 163.00 0.80~1.50 0.120 3 950.00 1 400 Ⅱ，Ⅲ 0.60~1.00 2.90
三江 喜大
林子		 800 K1 3.50~4.00 — 泥岩、煤 — 1.22~9.05 0.018~0.213 121.00~1 336.00 — Ⅱ1，Ⅲ — 0.89~36.08 文献[37]
E — 泥岩 1 464.40 0.84~1.48 0.015~0.028 38.40~81.00 1 900~3 000 Ⅱ2，Ⅲ 0.80~1.00 1.60~8.63
鸡西 3 780 J、K1 2.50~3.50 — 煤、炭质泥岩 — 1.36~22.76 0.022~0.218 385.00~939.00 — Ⅱ2，Ⅲ 0.60~0.80 1.04~43.25 文献[33-34]
通化 1 420 K1 3.00~4.50 — 泥岩 394.00 1.08~1.85 0.064~0.133 334.00~869.00 — Ⅱ1，Ⅲ 0.97~1.39 2.57~42.00
虎林 9 510 K1 — — 煤、炭质泥岩 — 1.97~14.50 0.009 — — Ⅲ 0.50~0.70 3.29~44.85
勃利 9 202 K1 — — 泥岩 463.00 0.48~1.12 0.010~0.091 625.00~1 135.00 — Ⅲ 1.20~1.75 0.18~1.45
宁安 2 900 K1 — — 煤、炭质泥岩 — 1.63~14.87 — — — — — 5.34~41.47
延吉 980 K1 — — 泥岩、煤 — 1.57~4.62 0.030~0.390 357.00~444.00 — Ⅱ，Ⅲ > 0.50 2.38~16.13
南襄 泌阳 1 000 E2 4.10 4.10 泥岩 1 900.00 1.77 0.220 1 219.00 1 700~1 900 Ⅰ，Ⅱ 0.50~1.80 — 文献[18]
南阳 3 600 E2 3.78 — 泥岩 1 100.00 0.76 0.150 1 240.00 2 000~2 200 Ⅱ 0.50~1.00 —
枣阳 2 950 E 3.55 — 泥岩 788.00 0.71 0.070 200.00 2 000~2 500 Ⅰ，Ⅱ 0.20~0.40 —
三水 3 400 E1 3.13 6.00 泥岩 500.00 1.25 0.100 1 578.00 800~1 200 Ⅱ 0.80~1.80 —
百色 830 E 3.74 3.90~4.70 泥岩 1 000.00 1.01~1.58 0.090 775.00 1 650~2 000 Ⅱ，Ⅲ 0.55~1.04 11.00
保山 135 E2 7.00~8.00 — 泥岩 1 000.00 1.59 — — — Ⅱ 0.31~0.45 25.78
陆良 325 E2 3.47~4.27 — 泥岩 800.00 1.04 0.049 — — Ⅲ 0.27~0.94 —
曲靖 213 E2 3.00~3.20 — 泥岩、煤 1 000.00 3.58 0.020~0.120 — — Ⅱ 0.28~0.60 —
伦坡拉 3 800 E2 4.60~6.60 5.50~6.00 泥岩 1 000.00~1 300.00 0.91 0.189 548.00 884 Ⅰ 0.74~1.14 —

图2

中国陆上部分中小型盆地烃源岩厚度（a）与成熟度（b）直方图"

表2

不同湖盆填充类型有机质发育影响因素与烃源岩特征"

湖盆类型 生成作用 破坏作用 稀释作用 烃源岩特征
过填
充湖盆		 + 养分输入增加
- 淡水输入稀释养分
- 总产量随湖盆体积增大而下降		 - 底部的氧气供应增加
- 均匀的水体使风的混合更有效
- 冷的底流
- 浊流的发育		 - 丰富的碎屑岩
± 丰富的陆源碎屑对流		 ①中等—差的油/气
②油气混合
③横向变化大（泥岩TOC < 1%~7%，煤TOC < 80%；OMT为藻类/陆源，Ⅰ—Ⅱ型；HI为50~600 mgHC/g；厚度大，小于数十米）
平衡
填充湖盆		 + 明显的养分输入
+ 养分由于间歇性干旱而浓缩
+ 大部分湖盆水体位于透光带		 + 封闭湖盆和间歇性干旱使水体密度分层
+ 大量的生产消耗水体底部的氧气		 + 变化很大，碎屑相对少
+ 对流的陆源有机质含量低
- 间歇性洪水或泄洪可能带来大量陆源碎屑		 ①中等—好的油
②以生油为主，个别情况下生气
③横向变化小（TOC为1%~30%；OMT以藻类为主，Ⅰ型，偶有陆源，为Ⅱ型；HI为500~700 mgHC/g；厚度较小，为1~10 m）
欠填
充湖盆		 ± 养分输入变化大
+ 养分由于间歇性干旱而浓缩
- 过度的浓缩破坏有机质
- 仅部分演化阶段水体适合有机质生成		 - 间歇性干旱氧化有机质
- 间歇性的水体输入导致氧化，消耗有机质		 - 半干旱气候产生大量碎屑输入
+ 陆源有机质输入少
+ 矿物沉淀产生大量填充物		 ①差—好的油
②以油为主
③横向变化弱（TOC < 0.5%~20.0%；OMT为藻类，Ⅰ型；HI为650~1 150 mgHC/g；厚度小，为米级）

图3

雅布赖盆地侏罗系—古近系湖盆填充演化阶段划分地震剖面示意图"

表3

中国陆上地温梯度分布特征"

区域 地温梯度分布特征
东部地区 高地温梯度区主要分布于松辽盆地、华北及东南沿海区域，多为4.00~5.00 ℃/100 m，最高达7.00~8.00 ℃/100 m，多呈条带状NE向延伸。其中松辽盆地地温梯度为3.50~4.00 ℃/100 m，最高达6.00 ℃/100 m以上，以NNE和NEE向延伸为主；华北地区为3.20~3.50 ℃/100 m，最高达7.00 ℃/100 m以上，呈NNE向低—高—低条带状分布；东南沿海为2.50~3.50 ℃/100 m，温州、广州一线以东多为3.00 ℃/100 m以上分布区，局部地热异常区达6.00~7.00 ℃/100 m，而雷州半岛、北部湾等可达3.30 ℃/100 m，等值线延伸方向与海岸线基本一致；鄱阳盆地、洞庭盆地、南阳盆地及三水盆地等地温梯度均偏高，一般为3.00 ℃/100 m以上，最高达4.00 ℃/100m以上。
中部地区 海拉尔盆地、二连盆地、四川盆地及其以南滇、黔、桂地区地温梯度多为2.50 ℃/100 m左右；银根—额济纳旗盆地、鄂尔多斯盆地及周缘地区达3.00 ℃/100 m以上；滇东地区一般为3.00~3.50 ℃/100 m；南盘江盆地、百色盆地和南宁盆地等区域地温梯度偏高。
西部地区 地温梯度南高北低。西藏南部及云南西部沿雅鲁藏布江向东延至腾冲—景谷一带是西南部一条较高的地温梯度陡变带，最高可达5.00~7.00 ℃/100 m以上，一般为2.50~3.00 ℃/100 m，其中陆良盆地、玉溪盆地、景谷盆地和保山盆地等区域偏高。山区通常低于1.50 ℃/100 m，藏北高原中—新生代沉积盆地比周围高1.00~1.50 ℃/100 m；柴达木盆地及河西走廊地区地温梯度为2.50~3.00 ℃/100 m；共和盆地大于5.10~7.25 ℃/100 m[50]；兰州—西宁地区为2.00~3.00 ℃/100 m；新疆塔里木、准噶尔盆地偏低，多为1.50~2.50 ℃/100 m，仅伊犁、霍尔果斯局部地区偏高。

图4

中国陆上大地热流分布图(据文献[51]修改)"

图5

酒泉盆地青南次凹柳9井（a）、青深1井（b）下白垩统烃源岩与河套盆地临河坳陷古近系临河组（c） 埋藏演化与生烃史（图b据文献[17]修改，图c据文献[12]修改）"

图6

环鄂尔多斯周缘中小盆地群平面分布"

图7

鄂尔多斯盆地及周缘测点地温梯度分布图（据文献[54]修改）"

图8

河西走廊地区南北向区域地质剖面"

图9

河西走廊及周缘地区侏罗系烃源岩厚度图"

图10

中国南方晚二叠世孤峰组岩相古地理平面图（据文献[55]修改）"

图11

渭河—鄂尔多斯—河套盆地区域地质横剖面"

图12

渭河盆地南北向地震剖面"

图13

渭河盆地地温梯度平面分布（据文献[58-59]修改）"

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