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随着常规油气藏勘探的程度越来越高,“深地”“深时”和“深海”的油气勘探在未来油气勘探中变得愈发重要。早期对于生命演化的研究认为,寒武纪之前的生物无论在丰度还是种类上都不足以形成大规模的烃源岩,导致对前寒武系的烃源岩研究长期被忽视[1⁃3]。但是近些年来的古生物研究表明,真核生物如疑源类,最早出现于古太古代,但其丰度和种类较低,至中元古代逐渐开始成为重要的有机质来源[4⁃6]。此外大量研究也证实中元古代存在大气增氧阶段,促使至少在中元古代1.59~1.56 Ga、1.44~1.43 Ga和1.40~1.36 Ga三个时期的大气氧含量达到现今水平的4%以上[7],而已有研究表明当大气的氧含量达到现今水平的0.5%~1.0%,就能够满足后生动物演化和发育的需要[8⁃9]。同时由于存在海洋硫化分层及缺氧条件,也有利于有机质的埋藏,中元古代具备优质烃源岩发育和保存条件[10⁃11]。
近些年在古老地层中取得的一系列勘探突破,也证实了前寒武系也可以发育规模性富含有机质的烃源岩（图1）[12⁃14]。例如,在俄罗斯奥涅加湖地区发现距今20亿年前（古元古代）的硬沥青,这些硬沥青来自于遭受了变质作用的油页岩和古油苗,有可能是世界上最古老的规模性烃源岩[15⁃16]。此外在俄罗斯的东西伯利亚盆地中上元古界里菲系和上元古界震旦系、文德系发现由海相泥页岩和泥灰岩组成厚层烃源岩,平均TOC含量为0.5%,局部可达12.9%,是东西伯利亚盆地油气田群的主力烃源岩之一[17]。澳大利亚北部的McArthur盆地的Barney Creek组（16.4亿年,地质年代与我国华北串岭沟组相当）页岩气区的地质储量达4 000多亿立方米[18],中元古代Middle Velkerra组（14.0亿年,地质年代与我国华北下马岭组相当）页岩气区的地质储量超百亿吨油气当量[19]。此外在印度—巴基斯坦、西非Taoudeni盆地,北美和巴西São Francisco等也发现大量前寒武系优质烃源岩（图1）[3,12⁃13,20]。我国四川盆地安岳气田震旦系取得了海相碳酸盐岩气田突破,证实了中国新元古界震旦系的油气潜力[21]。然而,目前对于华北地台发育的燕辽裂陷槽中新元古界尚无商业化油气突破。因此,本文重点聚焦于燕辽裂陷槽东北段,即现今辽西拗陷部分的中元古界蓟县系—待建系沉积环境和有利生烃条件的研究。
如上所述,目前在国外已发现大量的前寒武系优质烃源岩,其中部分已经形成规模性油气藏商业化的勘探突破。尤其是澳大利亚北部McArthur盆地发育两套中元古代优质烃源岩,油气潜力巨大,这与我国华北串岭沟组、洪水庄组和下马岭组地质年代相近,可能对我国华北地区的油气勘探具有借鉴意义。
华北燕辽裂陷槽地区的中新元古界油气勘探始于20世纪50—60年代,目前已于冀北—辽西拗陷发现上百个油苗点及多个古油藏（如双洞、龙潭沟、卢家庄等）的存在,证实中—新元古界存在过油气的生成、运移和破坏,是中国油气勘探值得关注的一个具有广阔远景的能源领域[22⁃28]。目前在辽西拗陷发现86处油气显示,辽河油田部署的韩1井、杨1井和兴隆1井在中新元古界均有油气显示[29]。中国地质调查局沈阳中心于辽西坳陷凌源盆地部署的辽凌地3井（图2）钻遇优质洪水庄组（TOC平均为3.6%；S1+S2平均为8.20 mg/g；Ro平均为0.95%；有效烃源厚度大于30 m）和下马岭组烃源岩,证实辽西坳陷中新元古界油气存在规模性油气藏的潜力[30]。
图 2 研究区概况图
Figure 2. Geographic figure of the study area showing outcrops and drilling wells used in this work
目前对于燕辽裂陷槽的研究多集中于冀北地区,前人已对此开展了大量的层序地层格架、沉积环境、微生物岩、油气生烃潜力、烃源岩分布等研究[11,23,27,31⁃40],但在辽西地区只有基于少量野外剖面,如凌源—宁城盆地小庄户剖面[41],和几口钻井的油气资源潜力评价[42⁃43]。显然,对于辽西凹陷中元古界蓟县系的沉积环境和生烃条件的认识还处于初级阶段,这制约了该地区的岩相古地理研究和油气勘探前景。因此,本文聚焦辽西地区,结合大量的野外露头和收集的仅有钻井资料,对辽西地区开展系统的沉积环境分析和生烃条件评价。
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在地理范围上,辽西坳陷位于辽宁省西部朝阳、建昌、喀左、凌源四县及其周边中元古界地表露头区,面积约30 000 km2,处于119°00′~122°00′ E,40°20′~42°00′ N之间。在区域构造上,辽西坳陷隶属于华北克拉通北缘,燕辽裂陷带的东段,西侧接连冀北坳陷,东端倾伏于新生代辽河裂谷盆地之下,北为内蒙古地轴,南有山海关隆起（图2a）。
燕辽地区位于我国华北地区的中北部,基底为太古宙迁西群麻粒岩—片麻岩,燕辽裂陷槽形成于18~8亿年,对应于全球Columbia超大陆裂解到Rodina超大陆汇聚—裂解构造背景[44⁃48]。燕辽裂陷槽先后经历了早期长城系大陆裂谷阶段,中期蓟县系被动陆缘阶段,中晚期待建系活动陆缘—陆块碰撞阶段、末期青白口系大陆伸展裂陷阶段[44]（图3）。随后由于构造抬升,导致部分青白口系景儿峪组及之后地层被剥蚀或无沉积,伴随着燕山地区在古生代再次沉降,形成大规模的以海相碳酸盐岩为主的沉积序列。
虽然燕辽裂陷槽形成和发育阶段伴随着全球性Columbia超大陆裂解到Rodina超大陆汇聚—裂解的多次构造和火山运动,但是研究区整体以稳定升降运动为主,形成了以碳酸盐岩为主的巨厚的海相地层,部分地区例如天津蓟县标准剖面总厚度可达9 000 m[49]。燕山地区中新元古界根据构造演化的阶段不同和岩性组合差异,自下而上可以划分为4个系和12个组,依次为长城系（常州沟组、串岭沟组、团山子组、大红峪组）,蓟县系（高于庄组、杨庄组、雾迷山组、洪水庄组、铁岭组）、待建系（下马岭组）和青白口系（长龙山组、景儿峪组）（图3）。
辽西拗陷的地层发育情况与燕辽裂陷槽其他区域类似,长城系—青白口系发育完整。前人的调查研究表明研究区存在串岭沟组、高于庄组、洪水庄组、铁岭组和下马岭组5套烃源岩层系,本次研究聚焦于洪水庄组、铁岭组和下马岭组这三套烃源岩层系的沉积环境和生烃潜力。其中洪水庄组与铁岭组为整合接触关系,铁岭组沉积之后受到芹裕运动影响导致铁岭组顶部遭受剥蚀,因此铁岭组与其上覆下马岭组呈平行不整合接触关系[50⁃52]。多数研究认为下马岭组与其上覆龙山组为不整合接触关系,但是基于地层学、碎屑锆石测年、锂同位素和主微量元素的最新研究中指出,下马岭组与龙山组并未存在大型不整合面[53]。
本研究基于辽西坳陷35个野外露头,6口钻井资料（图2b）,通过野外露头和岩心观察、镜下薄片鉴定、有机地化参数对研究区烃源岩沉积环境和生烃潜力开展系统研究。
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燕辽裂陷带蓟县系洪水庄组岩性主要为一套黑色页岩夹白云岩,厚度为100~170 m,沉积中心位于蓟县、兴隆、宽城一带[54]。前人研究认为洪水庄组整体为浅海环境,沉积中心为海湾—潟湖沉积,沉积边缘为碳酸盐岩潮坪相沉积[33,55⁃56]。其他学者对冀北地区洪水庄组黑色页岩分析也指出,黑色页岩大部分沉积于缺氧或静海环境,其沉积时期古生产力水平达到中等—高水平,部分钻井岩心中可见固体沥青及渗出的油苗[25,57⁃58],认为洪水庄组页岩沉积于滞留和水体交换循环弱的环境中,对有机质的保存非常有利。可见前人认为冀北地区洪水庄组整体环境是一个较为浅水但封闭的环境。
前人的研究多聚焦于冀北地区,目前对于辽西坳陷尚无系统的沉积环境分析。本次对辽西地区洪水庄组的研究表明,水深可能要比前人认识得更深,例如在辽西凌源市孟家窝铺剖面、辽宁省朝阳市朝阳县瓦房子镇尹杖子村、曲家沟村和杨树底下剖面都揭示了约80 m的洪水庄组黑色页岩（图4,5；露头位置请见图2b）,该套页岩页理极为发育,未见厚层白云岩,只在顶部见薄层白云岩、底部见薄层的钙质粉砂岩和白云岩,指示其处于稳定的沉积环境和较为停滞的水体环境。此外如喀左县平房子镇北洞村连续出露近90 m洪水庄组黑色页岩（图4d；露头位置请见图2b）,只在顶部发育薄层的白云岩和石英砂岩。由于野外露头的长期风化,洪水庄组页岩页理非常发育,但其内部细微沉积特征难以辨认。辽凌地2井和辽凌地3井的钻井岩心同样揭示了连续的暗色泥岩（图5,6）,部分岩心中可以观察到层状黄铁矿,指示还原的水体环境（图6b,c）。辽凌地3井黑色页岩的薄片观察可见条带状的黑色有机质,指示了强还原的沉积环境和较好的生烃潜力（图6d,e）。此外洪水庄组在研究区分布范围广,地层厚度稳定,可以全区追踪对比,且未见到明显的相带变化,反映了研究区中西部均为稳定的还原环境（图5）。
图 4 洪水庄组野外露头特征
Figure 4. The depositional features of the outcrops of the Hongshuizhuang Formation
图 5 辽西坳陷洪水庄组和铁岭组地层对比图（剖面位置请见图2b）
Figure 5. The stratigraphic correlation between wells and outcrops in the Western Liaoning Depression (please find the cross⁃section location on Fig.2b)
图 6 洪水庄组钻井、岩心和薄片特征（辽凌地3井）
Figure 6. The core, well log and thin section features of the Hongshuizhuang Formation (well Liaolingdi 3)
在喀左县姜杖子村剖面上洪水庄组顶部可见薄层的暗色泥岩夹透镜状的白云岩,白云岩与暗色泥岩呈冲刷切割关系（图7a,b）,部分白云岩透镜体可见丘状交错层理,指示其原始的形成环境为风暴沉积背景,但由于后期受到重力作用而滑塌进入暗色泥岩。该重力流滑塌特征还可见于辽宁省朝阳市朝阳县瓦房子镇曲家沟村剖面,白云岩与下伏洪水庄组暗色泥岩呈不规则状切割关系（图7c）。白云岩内部呈角砾状混杂堆积,为碳酸盐岩台地前缘斜坡滑塌进入深水海槽（图7d）。这种呈杂乱排列的角砾状灰岩代表了斜坡的重力流沉积过程[59]。
图 7 研究区洪水庄组顶部滑塌体野外特征
Figure 7. The sedimentary features of the slump deposits on the uppermost part of Hongshuizhuang Formation on outcrops
综合辽西坳陷洪水庄组特征：（1）岩性以黑色页岩为主；（2）分布广泛；（3）风暴岩或角砾状白云岩滑塌体侵蚀暗色泥岩；（4）黄铁矿发育等现象,可以判断辽西坳陷洪水庄组为一套临近台地边缘相的深水海槽沉积,顶部逐渐过渡到台地斜坡相,相较于前人认为冀北等地区的局限海或潟湖沉积,水体更深。无独有偶,澳大利亚McArthur盆地中元古Velkerri组,主要由灰黑色富含有机质的纹层状泥岩与粉细砂岩互层组成,前人研究分析认为其沉积环境是厌氧的水深相对较浅的深海盆地[58]。
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铁岭组主要由一套白云岩、含锰白云岩、锰质页岩、叠层石白云岩以及白云质灰岩组成,与洪水庄组整合接触。铁岭组沉积之后,受芹裕运动的影响,铁岭组与其上的下马岭组为不整合接触。辽西坳陷铁岭组根据岩性特征可以分为三段,铁岭组底部（铁一段）以白云岩、含锰白云岩为主,铁岭组中部（铁二段）以灰色、灰绿色泥岩为主,部分地区,如朝阳市瓦房镇以含锰白云岩和含锰页岩为主,而铁岭组顶部（铁三段）以叠层石白云岩,白云岩和泥岩薄互层为特点。研究区铁岭组厚度一般介于100~350 m之间,向研究区东部逐渐减薄（图5）,可能与芹裕运动抬升有关。根据野外的露头观察和部分样品镜下微观特征,研究区铁岭组可识别出台地边缘颗粒滩相（铁岭组底部）、局限台地潟湖相（铁岭组中部）和潮坪相（铁岭组顶部）。
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台地边缘颗粒滩多发育在水深几米到几十米之间,通常位于正常浪基面之上,是频繁受到风浪改造的高能相带,因此颗粒滩多由磨圆、分选良好的鲕粒及球粒组成,可以成为良好的油气储层[59]。辽西坳陷多个剖面的铁岭组底部可见颗粒白云岩,风化面呈黄色,新鲜面为灰色（图8）。颗粒白云岩镜下可见圆形或椭圆形碳酸盐颗粒,分选磨圆好,粒径介于0.5~1 mm,反映了强水动力条件下波浪的反复淘洗（图8c,d）。
图 8 铁岭组底部野外露头和微观镜下特征
Figure 8. Outcrop and microscopic features of the basal part of the Tieling Formation
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局限台地（潟湖）相位于台地礁—滩内侧,与开阔海的连通受到限制。其水深在几米到几十米之间,由于受到障壁阻挡,波浪作用相对较弱,主要受到潮汐作用的影响,主要的岩性多为灰泥,受到陆源输入影响也常含灰色泥岩和粉砂岩。辽西坳陷大部分区域的铁岭组中部（铁二段）以暗色泥岩为主,夹薄层白云岩,厚度多为30~70 m（图5、图9a,b）,单个剖面（喀左县玉皇庙剖面）最大累计厚度可达120 m（露头位置见图2b）,为局限台地（潟湖）相,在相带上与下伏的铁岭组底部颗粒灰岩相邻,反映沉积相带的向陆方向迁移。
图 9 铁岭组中部和顶部野外露头特征
Figure 9. Outcrop features of the middle and upper parts of the Tieling Formation
此外在辽西朝阳市瓦房子镇地区铁岭组中部广泛发育含锰白云岩和黑色页岩（图9c,d）,是华北地区主要的锰矿发育区。前人基于海水分层模式将全球各大沉积型锰矿成矿模式总结为极端气候事件（如冰期—间冰期）、闭塞盆地、最小含氧带扩张[60⁃63]。瓦房子镇含锰白云岩及其黑色页岩围岩,结合辽西地区广泛发育的黑色页岩沉积,可以推断瓦房子镇的含锰白云岩的形成环境为闭塞盆地,这与区域上认为辽西地区铁岭组中部为局限台地潟湖沉积环境相一致。
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潮坪相主要发育在铁岭组顶部,主要为叠层石白云岩、薄层白云岩和薄层泥岩互层（图9e,f）,其中薄层白云岩和薄层泥岩在垂向上频繁互层,旋回性明显,可能受到气候旋回的控制。该相带（铁岭组顶部）分布范围不如洪水庄组—铁岭组中部（图5）,这是由于后期芹裕运动造成的构造抬升,导致辽西坳陷东部（例如瓦房镇子镇一带）铁岭组顶部沉积序列被剥蚀,只在辽西坳陷西部地区广泛分布[64]。
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蓟县系下马岭组与其下伏铁岭组为不整合接触（图2、图10a,b）,由于受到芹裕运动影响,下马岭组露头分布范围较为局限,主要分布在辽西坳陷西南一带。与铁岭组以碳酸盐岩沉积为主不同,下马岭组主要为一套硅质碎屑岩,底部岩性以石英砂岩、粉砂岩和粉砂质页岩为主,顶部为厚层的灰黑色页岩夹薄层粉砂岩和白云岩透镜体,在本研究区下马岭组常见辉绿岩脉侵入,在露头多见辉绿岩的球形风化。研究区下马岭组主要发育碎屑滨岸相和浅海—半深海相。
图 10 凌源市沟门子镇小庄户村下马岭组野外沉积特征
Figure 10. Sedimentary features of the Xiamaling Formation outcrop in Xiaozhuanghu village, Goumenzi town, Lingyuan city
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下马岭组底部以一套石英砂岩向上过渡为粉砂岩和粉砂质泥岩为特征。石英砂岩呈块状,见多种类型的交错层理,石英颗粒分选磨圆极好,反映了波浪和潮汐的反复淘洗冲刷,为典型的碎屑滨岸相（图10a~c）。
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下马岭组中部—顶部以暗色泥岩为主,夹含少量的粉砂岩和白云岩透镜体,为浅海相沉积,在水深最大处可能为半深海沉积（图10d~f）。早期前人认为燕辽裂陷槽的北缘被内蒙古地轴所局限,因此多认为下马岭组沉积时期为局限的海湾或潟湖沉积。但后期的研究表明内蒙古地轴为后期古生代隆升[65⁃66],此外有学者根据冀北下花园地区下马岭组的古海洋环境分析此时燕辽裂陷槽与北面广海连通[7,52,67⁃68]。结合山海关在中新元古代长期隆起的背景[64],下马岭组时期华北地台东部山海关—葫芦岛一带为古隆起,向西和西北逐渐过渡为滨浅海相、浅海相和深海相。
高志勇等[52]在河北下花园夏家沟—古城梁剖面的研究中指出下马岭组为浅海陆棚—深水陆棚的泥页岩沉积和风暴—浊流沉积。张水昌等[7]研究指出下马岭组沉积时期,冀北—辽西一带为浅海陆棚—深水海湾沉积,北部和西北部为广海和深海,东南部为古陆。旷红伟等[53]也指出北京西山、河北怀来、河北下花园一带下马岭组中部为浅海陆棚。综合而言,下马岭组时期为无障壁海岸沉积,岸线沿山海关—葫芦岛一带呈北东方向向南北两侧延伸,浅海陆棚—深水盆地向西和西北方向发育。辽西坳陷早期为滨岸相沉积,中晚期以浅海陆棚沉积为主,水深最大时为半深海沉积。
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结合区域地质背景、野外露头、岩心、薄片观察以及前人认识,分别建立了辽西坳陷中元古界蓟县系洪水庄组、铁岭组和下马岭组沉积模式。其中洪水庄组为深水海槽—台地边缘—潮坪环境,研究区主要发育深水海槽和台地边缘相,而浅水潮坪相在研究区的东部和山海关古陆之间发育,但目前缺乏露头和钻井资料进一步限定其发育范围（图11a）。铁岭组为台地边缘—潟湖—潮坪沉积环境（图11b）,下马岭组为碎屑滨岸—浅海陆棚沉积环境（图11c）。
图 11 辽西坳陷中元古蓟县系洪水庄组（a）、铁岭组（b）和下马岭组（c）沉积模式图
Figure 11. Depositional model of the Mesoproterozoic Hongshuizhuang Formation (a), Tieling Formation(b) and Xiamaling Formation(c) in the Western Liaoning Depression
洪水庄组沉积时期水体较深,主要由暗色泥岩夹薄层白云岩组成。洪水庄组顶部出现白云岩的滑塌沉积,反映水体逐渐向上变浅的序列,并从海槽沉积环境过渡为台地斜坡环境。铁岭组底部发育高能碳酸盐岩台地边缘颗粒滩沉积,向中部逐渐过渡为潟湖相灰色泥岩,局部地区由于水体循环闭塞形成含锰白云岩和含锰页岩,顶部为潮坪相叠层石白云岩、白云岩和泥岩的频繁互层。因此,洪水庄组和铁岭组分别构成了两个水体整体向上变浅的沉积序列（图11a,b）。下马岭组为无障壁碎屑海岸—浅海陆棚沉积,底部为滨海石英砂岩、粉砂岩沉积为主,向上逐渐过渡为浅海陆棚,岩性以灰色页岩和粉砂质页岩为主,海侵最大时水深可达半深海（图11c）。
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本次研究收集和整理了176份辽西坳陷洪水庄组（115份）、铁岭组（23份）和下马岭组（38份）烃源岩的地球化学数据。总有机碳（TOC）是烃源岩评价的重要指标,统计分析表明洪水庄组TOC介于0.2%~3.9%,平均值为1.8%,属于好烃源岩的标准（图12）。洪水庄组的生烃潜量（S1+S2）分布范围为0.02~33.17 mg/g,平均值为2.58 mg/g,为较好烃源岩。前人分析冀北地区洪水庄组烃源岩地球化学指标后指出TOC平均值为2.4%,S1+S2平均值为2.58 mg/g[27],略好于本次研究区的相关指标,但两者的差距并不明显,可能是冀北地区更处于当时的沉积中心,导致冀北地区洪水庄组黑色页岩的指标略好于辽西坳陷。总体而言,综合TOC和S1+S2数据认为辽西坳陷洪水庄组整体为较好—好烃源岩。
图 12 辽西坳陷洪水庄组、铁岭组和下马岭组烃源岩有机地化参数分布图
Figure 12. Distribution of organic geochemical parameters of source rocks from the Hongshuizhuang Formation, Tieling Formation, and Xiamling Formation in the Western Liaoning Depression
相较于洪水庄组,铁岭组的TOC介于0.1%~1.2%,平均值只有0.3%,属于较差的烃源岩,但是对测试样品的岩性进行分析,只有部分样品属于黑色页岩,大部分样品为白云岩或粉砂质泥岩。如对辽西轱辘井剖面的黑色页岩进行单独统计,其TOC介于0.6%~1.2%,平均值为0.9%,属于中等烃源岩。铁岭组整体S1+S2介于0.10~2.20 mg/g,平均值为0.30 mg/g,属于非烃源岩；但对铁岭组黑色页岩单独统计发现,其S1+S2介于0.40~2.20 mg/g,平均值为1.00 mg/mg,属于差烃源岩。总体而言,铁岭组黑色页岩品质不如洪水庄组,属于差—中等烃源岩。这可能与铁岭组黑色页岩沉积时期虽然为潟湖沉积,但水体相对较浅,容易受到陆源物质输入和表层大气的影响,导致烃源岩品质不如洪水庄组。
下马岭组黑色页岩的有机地球化学结果显示了优质烃源岩品质,TOC介于0.1%~12.6%,平均值为2.3%,属于好烃源岩。S1+S2测试结果介于0.10~66.00 mg/g,平均值为8.40 mg/g,同样属于好烃源岩的标准。这比前人总结的冀北地区下马岭组平均TOC为2.1%,平均S1+S2为3.90 mg/g要高[27],显示了良好的烃源岩品质和生油潜力。下马岭相对洪水庄组和铁岭组具有更高的总有机碳含量和生烃潜量,可能与下马岭组沉积时期更为丰富活跃的藻类微生物[40],以及适宜生物勃发的较高氧气含量有关[7]。
此外对辽西坳陷的烃源岩Tmax参数统计发现,这三套古老烃源岩的热演化并没有达到过成熟的阶段,反而相当一部分的洪水庄组—下马岭组烃源岩处于低成熟阶段（图12）。处于成熟阶段（Tmax为435 ℃~445 ℃）约占18%~32%,高成熟阶段（445 ℃~480 ℃）约占23%~33%,过成熟的烃源岩占比很小。综合Tmax数据可得,洪水庄组—下马岭组烃源岩大多处于产油和产气的成熟—高成熟早期阶段,前人总结冀北地区的洪水庄组—下马岭组的平均Ro介于1.09%~1.14%,其热演化程度略高于本次研究统计的Tmax参数,可能与冀北地区为当时的沉降中心埋藏更深有关,但两者的热演化程度均表明这三套烃源岩均处于成熟—高成熟早期阶段,适宜于油气的生成。
史晓颖等[24]认为中元古代海洋海底普遍缺氧,有利于有机质的保存,因此中元古代的有机质具有较高的埋藏率。王浩等[27]估算中新元古界烃源岩的总生烃量约为1 227.01×108 t。可见中新元古界的烃源岩层系不仅具有高的生烃潜力和适宜的热演化程度,其资源潜力也非常可观。
评价辽西坳陷的油气潜力同时也需考虑生储盖组合,大量的研究表明蓟县系雾迷山组和铁岭组白云岩经过成岩作用及后期改造,可以形成大量的溶蚀孔洞,同时受构造应力作用影响形成了大量的裂缝,是燕山地区的优质储层[75⁃76]。下马岭组底部发育一套滨海相的石英砂岩,是研究区另一套优质的储集体。而洪水庄组和下马岭组的页岩X衍射测试表明脆性矿物含量平均值为66.8%,有利于后期的压裂改造,是优质的非常规油气储层,同时也是优质的盖层[40]。因此,蓟县系雾迷山组顶部白云岩、洪水庄组黑色页岩、铁岭组白云岩、待建系下马岭组底部石英砂岩和中上部黑色页岩,组成了多套的生储盖组合,利于油气的生成、储集和封盖。由于本文聚焦于烃源岩的沉积环境和生烃潜力评价,故对含油气系统不再展开分析。
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（1） 研究发现洪水庄组主要为一套富含有机质的黑色页岩,黄铁矿非常发育,指示深水海槽沉积。多个露头点在洪水庄组顶部见白云岩滑塌沉积,表明水深向上变浅,逐渐过渡为碳酸盐岩台地斜坡沉积环境。
（2） 铁岭组底部广泛发育高能颗粒白云岩沉积,中部以灰色页岩为主,局部地区灰色页岩与含锰白云岩交互沉积,顶部为叠层石白云岩和泥岩互层,反映碳酸盐岩台地边缘—潟湖—潮坪沉积环境,并同洪水庄组组成了两个整体水深向上变浅的沉积旋回。
（3） 待建系下马岭组为底部石英砂岩、中上部则以灰色页岩沉积为主,为无障壁碎屑滨岸—浅海陆棚沉积。
（4） 有机地化测试数据表明洪水庄组和下马岭组黑色页岩是中—优质烃源岩,铁岭组次之。烃源岩热演化程度多处于成熟—高成熟早期阶段,有利于油气的生成。
The Depositional Environment and Hydrocarbon Potential of the Mesoproterozoic Black Shale in the Western Liaoning Depression of the Yanliao Rift Zone
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摘要: 目的 前人对中元古代生命演化、氧气含量、古海洋条件等研究均表明中元古代存在适宜优质烃源岩生成和保存的环境。加之近年来元古宇油气资源的相继发现,使得我国中元古界黑色页岩沉积环境和生烃潜力的认识亟需加强。华北地台燕辽裂陷槽沉积了巨厚的中新元古代地层,发育串岭沟组、高于庄组、洪水庄组、铁岭组和下马岭组5套烃源岩层系,前人在冀北地区对这些烃源岩层系已开展了大量研究,但是目前对辽西坳陷研究还处于初级阶段。 方法 基于大量的野外露头、钻井、薄片和有机地球化学数据对辽西坳陷洪水庄组、铁岭组和下马岭组这三套烃源岩层系开展了沉积环境和生烃潜力分析。 结果 洪水庄组主要为一套富含有机质的黑色页岩,黄铁矿非常发育,指示海槽深水沉积。多个露头点在洪水庄组顶部见白云岩滑塌沉积,表明水深向上变浅,逐渐过渡为碳酸盐岩台地斜坡沉积环境。铁岭组底部广泛发育高能颗粒白云岩沉积,中部以灰色页岩为主,局部地区灰色页岩与含锰白云岩交互沉积,顶部为叠层石白云岩和泥岩互层,反映碳酸盐岩台地边缘—潟湖—潮坪沉积环境,并同洪水庄组组成了两个整体水深向上变浅的沉积旋回。待建系下马岭组底部发育石英砂岩、中上部则以灰色页岩沉积为主,为无障壁碎屑海岸—浅海陆棚沉积。有机地球化学数据表明多数黑色页岩TOC含量大于1.0%,为中到优质烃源岩,Tmax介于435 ℃~480 ℃,指示烃源岩处于成熟阶段,有利于油气的生成。 结论 中元古界黑色页岩沉积环境和生烃潜力综合分析表明,辽西坳陷具有良好的油气勘探潜力。Abstract: Objective Recent years' research advance on the life evolution, oxygen content, and paleo oceanic conditions of the Mesoproterozoic all indicate that during the Mesoproterozoic era there were suitable environments for the formation and preservation of high-quality hydrocarbon source rocks. The discoveries of the Proterozoic oil and gas resources in recent years, also suggests a need to enhance our understanding of the China's Mesoproterozoic black organic shale depositional environment and its potential for generating hydrocarbons. The YanLiao rift belt in the North China Craton has deposited thick Proterozoic strata, developing five sets of source rock systems： Chuanlinggou Formation, Gaoyuzhuang Formation, Hongshuizhuang Formation, Tieling Formation, and Xiamaling Formation. Previous studies have conducted extensive research on these source rock systems in the northern Hebei region but current research on the Western Liaoning Depression is still at an early stage. Methods This study is based on field outcrops investigation, drilling core observation, thin sections analysis and geochemical data to reveal the sedimentary environment and hydrocarbon potential for the Proterozoic Hongshuizhuang, Tieling, and Xiamaling Formation in the Western Liaoning Depression. Results and Discussions The study found that the Hongshuizhuang Formation mainly consists of organic-rich black shales with abundant pyrite indicating a deep- marine trough depositional setting. Multiple outcrop sections show carbonate debris flow deposits at the top of the Hongshuizhuang Formation, suggesting a gradually decreased water depth and depositional environment transition into a carbonate platform slope setting. The Tieling Formation consists of the grain dolostone formed under high energy at the bottom, gray shale and locally developed manganese-bearing dolostone in the middle, and interbedded stromatolite dolomite and thin mudstone at the top, suggesting a carbonate platform margin-lagoon- tidal flat depositional environment. The Xiamaling Formation is dominated by quartz sandstone at the bottom and grey shale in the middle-upper part indicating a clastic coast - shallow marine shelf depositional environment. Organic geochemical test data shows that most black shales have TOC content >1.0%, which are medium to high-quality source rocks. The majority of the Tmax ranges from 435°-480°, indicating that the source rock is mature and favorable for oil and gas generation. Conclusions Given the widely development of the black shale, favorite depositional environment, along with the high shale TOC and suitable thermal evolution degree, we believe the Proterozoic black shales in the Western Liaoning Depression have great hydrocarbon potential.
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图 2 研究区概况图
（a）冀北辽西地区中新元古界分布图,红框范围为燕辽裂陷带辽西坳陷部分,即本次研究区；（b）研究区野外露头和钻井资料分布图；红色线为野外露头和钻井对比剖面
Figure 2. Geographic figure of the study area showing outcrops and drilling wells used in this work
(a) distribution of the Mesoproterozoic strata in the northern Hebei and western Liaoning regions. The area within the red box represents the Western Liaoning Depression of the Yan⁃Liao rift belt, which is the focus of this study; (b) distribution map of outcrops and drilling wells used in the study area; The red line marks the stratigraphic correlation section based on outcrops and wells
图 3 华北地区燕辽裂陷槽地层和构造演化综合柱状图（据文献[40,44])修改）
1.灰岩；2.泥质灰岩；3.白云岩；4.灰质白云岩；5.白云质灰岩；6.粉砂质白云岩；7.页岩；8.粉砂质页岩；9.砂岩；10.砾岩；11.火山岩；12.花岗岩；13.片麻岩；14.沥青质；15.叠层石；16.燧石条带
Figure 3. Comprehensive stratigraphic and tectonic evolution history diagram of the Yan⁃Liao rift belt in the North China Craton (modified from references [40,44])
1. limestone; 2. marlite; 3. dolomite; 4. limy dolomite; 5. dolomitic limestone; 6. silty dolomite; 7. shale; 8. silty shale; 9. sandstone; 10. conglomerate; 11. volcanic rock; 12. granite; 13. gneiss; 14. asphaltene contents; 15. stromatolite; 16. chert band
图 4 洪水庄组野外露头特征
（a）洪水庄组黑色页岩,风化严重,新鲜面为灰色,辽西凌源市孟家窝铺剖面；（b）洪水庄组黑色页岩,向上过渡为铁岭组白云岩,朝阳市瓦房子镇尹杖子村剖面；（c）洪水庄组页岩,注意新鲜面为黑色,风化面为黄色,朝阳市瓦房子镇曲家沟西梁；（d）洪水庄组页岩,页理发育,喀左县平房子镇北洞村剖面
Figure 4. The depositional features of the outcrops of the Hongshuizhuang Formation
(a) the black shale of the Hongshuizhuang Formation, Mengjiawopu section, Lingyuan city; (b) the black shale of the Hongshuizhuang Formation, Yinzhangzi village, Wafangzi town, Chaoyang city; (c) black shale of the Hongshuizhuang Formation, note the fresh surface is black and the weathered surface is yellow, western ridge of Qujiagou village, Wafangzi town, Chaoyang city; (d) black shale of the Hongshuizhuang Formation with well⁃developed lamination, Beidong village, Pingfangzi town, Kazuo county
图 5 辽西坳陷洪水庄组和铁岭组地层对比图（剖面位置请见图2b）
Figure 5. The stratigraphic correlation between wells and outcrops in the Western Liaoning Depression (please find the cross⁃section location on Fig.2b)
Fig.5
图 6 洪水庄组钻井、岩心和薄片特征（辽凌地3井）
（a）洪水庄组岩性和测井柱状图；（b）黑色页岩,黄铁矿发育,410.1 m；（c）黑色页岩,黄铁矿发育,464.6 m；（d,e）洪水庄组黑色页岩镜下特征,黑色条带为有机质,正交光,比例尺见右下角,410.1 m
Figure 6. The core, well log and thin section features of the Hongshuizhuang Formation (well Liaolingdi 3)
(a) the lithology and GR logging feature; (b) black shale with well developed pyrite, 410.1 m; (d) black shale with well developed pyrite, 464.6 m; (d, e) Microscopic feature of the black shale under thin section, cross-polarized light. Please note the black color band are organic rich and the scale bare is located at the lower right corner, 3, 410.1 m
图 7 研究区洪水庄组顶部滑塌体野外特征
（a）洪水庄组顶部页岩,夹透镜状白云岩,白云岩透镜体内部见丘状交错层理,凌源市姜杖子村剖面；（b）洪水庄组顶部页岩被白云岩滑塌体切割,凌源市姜杖子村剖面；（c）洪水庄组顶部页岩被白云岩滑塌体侵蚀,朝阳市瓦房子镇曲家沟西梁；（d）白云岩滑塌体内部见白云岩角砾,朝阳市瓦房子镇曲家沟西梁
Figure 7. The sedimentary features of the slump deposits on the uppermost part of Hongshuizhuang Formation on outcrops
(a) top shale of the Hongshuizhuang Formation interbedded with lens⁃shaped dolomite, with hummocky cross⁃stratification observed inside the dolomite lens, Jiangzhangzi village, Lingyuan city; (b) top shale of the Hongshuizhuang Formation cut by dolomite debris flow, Jiangzhangzi village, Lingyuan city; (c) top shale of the Hongshuizhuang Formation eroded by dolomite debris flow, western ridge of Qujiagou village, Wafangzi town, Chaoyang city; (d) dolomite breccia observed inside the dolomite debris flow, western ridge of Qujiagou village, Wafangzi town, Chaoyang city
图 8 铁岭组底部野外露头和微观镜下特征
（a,b）铁岭组底部颗粒白云岩,辽西喀左县姜杖子村剖面；（c,d）铁岭组底部颗粒白云岩镜下微观特征,薄片取自图b中岩石；（e）铁岭组底部颗粒白云岩；辽西凌源市孟家窝铺剖面；（f）铁岭组底部颗粒灰岩,为图5e的局部放大；辽西凌源市孟家窝铺剖面
Figure 8. Outcrop and microscopic features of the basal part of the Tieling Formation
(a, b) grain dolostone at the base of the Tieling Formation, Jiangzhangzi village, Kazuo county, western Liaoning; (c, d) microscopic features of grain dolostone at the base of the Tieling Formation, thin sections taken from the rock in Fig.5b; (e) grain dolostone at the base of the Tieling Formation, Mengjiawopu village, Lingyuan city, western Liaoning; (f) grain dolostone at the base of the Tieling Formation, a magnified section of Fig.5e, Mengjiawopu village, Lingyuan city, western Liaoning
图 9 铁岭组中部和顶部野外露头特征
（a）铁岭组中部灰色页岩,辽西喀左县姜杖子村剖面；（b）铁岭组中部灰色页岩,凌源市孟家窝铺剖面；（c）铁岭组中部含锰白云岩和含锰页岩,朝阳市瓦房子镇曲家沟剖面；（d）铁岭组中部含锰白云岩和含锰页岩,朝阳市瓦房子镇曲家沟剖面；（e）铁岭组顶部薄层白云岩与泥岩互层,凌源市小庄户剖面；（f）铁岭组顶部叠层石白云岩,喀左县姜杖子村剖面
Figure 9. Outcrop features of the middle and upper parts of the Tieling Formation
(a) gray shale in the middle part of the Tieling Formation, Jiangzhangzi village, Kazuo county, western Liaoning; (b) gray shale in the middle part of the Tieling Formation, Mengjiawopu village, Lingyuan city; (c, d) Manganese⁃bearing dolostone and manganese⁃bearing shale in the middle part of the Tieling Formation, Qujiagou village, Wafangzi town, Chaoyang city; (e) thin⁃layered dolostone interbedded with mudstone at the top of the Tieling Formation, Xiaozhuanghu village, Lingyuan city; (f) stromatolite dolostone at the top of the Tieling Formation, Jiangzhangzi village, Kazuo county
图 10 凌源市沟门子镇小庄户村下马岭组野外沉积特征
（a,b）铁岭组与下马岭组不整合接触,底下为白云岩,顶部为石英砂岩；（c）下马岭组石英砂岩,可见槽状交错层理；（d）厚层石英砂岩向上过渡为薄层灰色页岩；（e）灰色粉砂质页岩,风化面发黄,新鲜面为灰色；（f）灰色页岩夹薄层粉砂质条带
Figure 10. Sedimentary features of the Xiamaling Formation outcrop in Xiaozhuanghu village, Goumenzi town, Lingyuan city
(a, b) unconformity between the Tieling Formation and the Xiamaling Formation, with dolomite below and quartz sandstone above; (c) quartz sandstone of the Xiamaling Formation showing trough cross⁃bedding; (d) the brownish quartz sandstone gradually changes upward to gray silty shale; (e) gray silty shale, note the yellow color is caused by weathering and the fresh surface is gray; (f) gray shale with very thin silty lamination
图 11 辽西坳陷中元古蓟县系洪水庄组（a）、铁岭组（b）和下马岭组（c）沉积模式图
Figure 11. Depositional model of the Mesoproterozoic Hongshuizhuang Formation (a), Tieling Formation(b) and Xiamaling Formation(c) in the Western Liaoning Depression
Fig.11
图 12 辽西坳陷洪水庄组、铁岭组和下马岭组烃源岩有机地化参数分布图
（a）烃源岩TOC和S1+S2分布图,数据据文献[69⁃74]；（b）烃源岩Tmax分布图,数据据文献[70⁃74]
Figure 12. Distribution of organic geochemical parameters of source rocks from the Hongshuizhuang Formation, Tieling Formation, and Xiamling Formation in the Western Liaoning Depression
(a) distribution map of TOC and S1+S2 of source rocks, data based on references[69⁃74]; (b) distribution map of Tmax in source rocks, data based on based on references[70⁃74]
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