The Age and Potential Provenance Information of Amushan Formation in Wulanaobao Area, Northwestern of Langshan, Inner Mongolia and Its Geological Significance
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摘要: 沉积盆地的研究对于理解造山带的构造演化具有重要意义.内蒙古狼山地区位于中亚造山带中段，构造演化历史复杂，晚古生代沉积盆地的大地构造背景存在争议.在对狼山西北缘乌兰敖包地区出露的"阿木山组"岩性特征、沉积构造及沉积环境的系统研究基础上，将该组分为3个岩性段.一段主要为粗碎屑岩，交错层理发育，沉积环境为辫状河三角洲；二段底部主要为粗碎屑岩，向上沉积物粒度变细，顶部出现生物碎屑灰岩，在岩屑石英砂岩中新发现芦木Calamites sp.，座延羊齿Alethopteris sp.，带科达Cordaites principalis Gein等植物化石，沉积环境由辫状河三角洲向滨海环境过渡；三段主要岩性为结晶灰岩，含生物碎屑，沉积环境为滨-浅海环境."阿木山组"一、二段砂岩碎屑锆石年龄可分为~2.5 Ga、~1.8~1.2 Ga、~826 Ma、461~440 Ma和313~273 Ma五个时间段，其中最小年龄为273 Ma，结合植物化石鉴定结果以及上覆火山岩地层年代，确定"阿木山组"沉积时代为265~273 Ma.研究区内同时代的岩浆岩指示该区在早中二叠世处于古亚洲洋向华北板块俯冲的岩浆弧环境，结合"阿木山组"的沉积特征、沉积时代及所处构造位置，对其地层划分与对比方案提出建议.Abstract: The study of sedimentary basins is important for understanding the tectonic evolution of orogenic belts. The Langshan region of Inner Mongolia is located in the middle central Asian orogenic belt and has a complicated structural evolutionary history. The tectonic setting of Late Paleozoic sedimentary basin is still in controversy. Based on the study of the lithology, sedimentary structure and sedimentary environment of Amushan Formation in Wulanaobao area in the northwestern of Langshan, we divide the Formation into three members. The first member is mainly composed of coarse clastic rocks with cross-bedding developed, and the sedimentary environment is braided river delta. The bottom of the second member is mainly composed of coarse clastic rocks with increasingly finer grain-size in the upper sediments and the bioclastic limestone at the top of second member, and the depositional environment is from braided river delta to littoral circumstances. At the same time, we firstly discovered plant fossils such as Calamites sp., Alethopteris sp., Cordaites principalis Gein from the lithic quartz sandstone of the second member. The third member consists of crystalline limestone and bioclastic limestone, and the sedimentary facies type is littoral-neritic facies. The detrital zircon ages of sandstone from the first and second members of Amushan Formation are divided into five groups of about~2.5 Ga, ~1.8-1.2 Ga, ~826 Ma, 461-440 Ma and 313-273 Ma, respectively. The youngest age of Amushan Formation is 273 Ma. Combining the results of plant fossils and the age of overlying volcanic rocks, the age of "Amushan Formation" is limited between 265 Ma and 273 Ma. The contemporaneous magmatic rocks in the study area were formed in the continental marginal arc. With the research of sedimentary characteristics, sedimentary age and tectonic position of Amushan Formation, we propose the method of stratigraphical divisions and correlation.
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0. 引言
有机储集空间是页岩的重要储集类型，国外已在这方面开展了大量研究工作，结果表明页岩中的有机储集空间的发育和有机质类型及演化程度有关(Jarvie et al., 2007；Curtis et al., 2010, 2012；Schieber, 2010；Sondergeld et al., 2010；Christopher and Scott, 2012；Loucks et al., 2012)，一般有机质类型为Ⅰ、Ⅱ型并且演化程度较高的页岩有机储集空间更为发育.但Kitty et al.(2013)最近对宾夕法尼亚北部的Marcellus页岩有机孔隙的研究发现，与有机质的演化程度相比，有机质含量对有机孔隙发育更为重要，但页岩中的有机质原始氢指数较低，即便有机碳含量较高，仍然不利于有机孔隙的发育.
关于页岩中有机孔隙的发育，近年来我国在页岩油气的勘探中也开展了一些研究工作，邹才能等(2010)在我国四川盆地寒武系和志留系高成熟海相页岩的有机质中发现了有机演化孔隙认为有机孔隙一般在100 nm左右.黄志龙等(2012)在对三塘湖盆地马朗凹陷芦草沟组源岩的研究中也观察到了有机孔隙，该源岩的埋深为2 297.1 m，马朗凹陷现今的地温梯度为2.2~2.4 ℃/100 m，该区有机孔隙发育于演化程度较低的页岩中，Ro%小于0.75%(吴林钢等，2012).
从目前国外对有机孔隙开展的研究工作来看，有机孔隙一般发育于演化程度较高的(Ro大于1.0%)海相地层(Milner et al., 2010；Gareth et al., 2012).由于有机孔隙的发育取决于油气的生成(Jarvie et al., 2007), 其有机孔隙的发育程度随演化程度的增加而增大已被页岩气研究领域广为接受(Ross and Bustin, 2009; 朱日房等, 2012).在演化程度较低的页岩中能否发育有机孔隙，人们一直存在质疑.笔者利用陆相断陷盆地页岩埋深跨度较大的特点，系统采集了同一沉积相带不同演化程度的湖相页岩，探讨湖相页岩有机储集空间发育的特点，并对其成因机制进行了分析.
1. 研究区地质背景
东营凹陷位于渤海湾盆地东南部，是渤海湾中、新生代裂谷盆地中的一个三级负向构造单元，东西长约150 km，南北宽74 km，面积为5 700 km2，受盆地一级断裂活动和中央隆起带抬升影响，东营凹陷分割成利津、民丰、牛庄、博兴4个洼陷(图 1).东营凹陷为中国东部典型富油凹陷，已完成各类探井3 179口，其中有110口井在钻遇古近系Es3x、Es4s泥页岩时有油气显示，有13口井在泥页岩段获工业油气流.
东营凹陷的构造演化可划分为4个不同阶段，即前裂陷期、裂陷期、断陷期和坳陷期，古近系Es3下、Es4上段泥页岩分别发育于盆地的断陷鼎盛期和断陷加速期，该泥页岩是东营凹陷的主要生烃层系(张林晔等, 2003a, 2003b, 2005；Zhang et al., 2009).
沙三下亚段泥页岩以半咸水-淡水湖相泥岩、灰褐色油页岩及页岩沉积为主，夹少量灰色灰岩及白云岩，暗色泥岩厚度一般在300 m以上，最厚可达500 m，页岩厚度150~200 m，埋深为1 500~4 200 m.沙四上亚段泥页岩岩性组合以灰褐色钙质纹层泥页岩为主，夹泥灰岩、白云岩，为咸水-半咸水湖相沉积，暗色泥岩厚度一般为250~350 m，页岩厚度为40~120 m，埋深为1 576~4 800 m(张林晔等, 2012).
2. 样品和实验方法
2.1 样品
样品分别取自东营凹陷的利津、民丰、牛庄、博兴4个洼陷，样品分布见图 1.样品的地球化学和岩石学特征见表 1.样品的岩性均为灰色-深灰色页岩，有机质类型为Ⅰ、Ⅱ1型，样品的有机质丰度较高，有机碳含量平均值为4.45%，粘土矿物含量较低，最高为41%，平均值为25%.碳酸盐含量平均值为35%，石英加长石平均含量为36%.样品埋藏深度为1 982.50~4 046.35 m，Ro为0.32%~1.09%，主要处于生油窗范围内(张林晔等, 2011).
图 1 研究区构造单元及取样点分布图a中虚线表示隆起Fig. 1. Structure units and sample distribution of the study area表 1 实验样品地球化学参数数据Table Supplementary Table Geochemical parameters of experimental samples
2.2 实验方法
样品的地球化学和岩石学基本特征的分析采用如下仪器：有机碳分析使用仪器为CS-600有机碳分析仪，执行的分析标准为GB/T 19145-2003；热解分析使用仪器为ROCK-EVAL6岩石热解仪，执行的分析标准为GB/T 18602-2001；镜质体反射率使用仪器为UMSP-50显微光度计，执行的分析标准为SY/T 5124-2012；全岩矿物组成分析使用的仪器为D/max-2500pc X-射线衍射仪，执行的分析标准为SY/T5163-2010.
样品微观特征的分析采用了氩离子抛光样品制备技术，使用的仪器为IB-09010CP离子截面抛光仪，实验条件为：加工电压6 kV；离子束直径500 μm；加工摆角±30°.
样品制备完成后，分别使用Quanta200扫描电镜及EDAX能谱仪联机和JSM-6700f冷场发射扫描电子显微镜进行样品微观特征观察和岩石组分分析，图像模式为背散电子图像(backscattered electron detector，简称BSED)和二次电子图像(low frequency disturbance，简称LFD).Quanta200扫描电镜及EDAX能谱仪联机实验条件为：加速电压20 kV；束斑3.5，工作距离7~13 mm.JSM-6700f冷场发射扫描电子显微镜实验条件为：加速电压10 kV；束流10 μA；物距7.5~8.3 mm.
样品总孔隙度采用密度法测定总孔隙度的方法, 密度由胜利油田分公司地质科学研究院测试中心测定，将均质岩心上分别取两块岩样，一块测出岩样密度，另一块粉碎80目以下，洗油后测得该粒度级颗粒密度，利用孔隙度(%)=(1-岩样密度/颗粒密度)×100计算岩石总孔隙度.
3. 结果与讨论
图 2 东营凹陷有机质-粘土-碳酸盐混合体电子图像和能谱图a.2号样品富含有机质泥质纹层和富含碳酸盐纹层间充填有机质(LFD)及其能谱图，wang129，Es4s，TOC=3.97%，Ro=0.32%；b.5号有机质(C)、粘土(I/S)、碳酸盐(Cc)混合体中发育的孔隙(BSED)及其能谱图，yong89，Es4s，TOC=2.85%，Ro=0.53%；c.7号黄铁矿、石英、方解石颗粒间孔内充填含有机质粘土碳酸盐混合体(BSED)及其能谱图，fan291，Es3x，TOC=9.20%，Ro=0.62%；d.11号有机质、粘土、碳酸盐混合体中发育的孔隙(LFD)及其能谱图，li673，Es3x，TOC=1.74%，Ro=0.82%.上图为电子图像；下图为能谱图Fig. 2. OM-clay-carbonate complexes in the Dongying sag3.1 有机质-粘土-碳酸盐混合体内孔隙微观特征
笔者对不同埋深的东营凹陷古近系湖相页岩进行了系统的观察，发现不同埋深的东营凹陷古近系湖相页岩中均发育有机质-粘土-碳酸盐混合体内孔隙.
在埋藏较浅的页岩中，有机质还没有大量生烃，有机质与矿物的接触关系保持了成岩作用早期最初的形态.镜下观察结果表明，在场发射电镜背散射照片中的暗色部分，有机质富集，能谱分析表明，暗色部分主要是有机质-粘土-碳酸盐混合体(图 2a~2d)，部分沙四段页岩为有机质-粘土-硫酸盐混合体(图 3)，富含有机质的暗色区域与其他矿物的接触关系呈条带状(图 3)，并具有较强的非均质性，背散射图像揭示了有机质在页岩中的赋存状态.富含有机质的矿物混合体在演化的过程中极易出现孔隙，在埋藏较浅(王129井2 553.7 m)的沙四段页岩中就发现了这类孔隙(图 4a)，随着埋深这类孔隙一直比较丰富，它常常沿着暗色区域的轮廓分布(图 4)，这类孔隙的尺度一般为微米级，但随着演化程度增高(埋深＞3 600 m)，在富含有机质的矿物混合体中纳米孔隙增加，并且呈密集分布(图 4d~4h).在高演化阶段有机质-粘土-碳酸盐混合体中纳米孔隙的分布特点与国外报道的有机孔隙的形态较为相似(Loucks et al., 2012).
图 3 东营凹陷有机质-粘土-硫酸盐混合体电子图像和能谱图a.9号白云石D晶间孔中充填含有机质、粘土Clay的硫酸盐Su矿物及其能谱图，fengshen1，Es4s，TOC=2.30%，Ro=0.70%；b.1号页岩低成熟阶段有机质与矿物的接触关系，wang33，Es4s，TOC=4.48%，Ro=0.39%；c.2号页岩低成熟阶段有机质与矿物的接触关系，wang129，Es4s，TOC=3.97%，Ro=0.32%；d.3号页岩低成熟阶段有机质与矿物的接触关系，liang206，Es4s，TOC=3.43%，Ro=0.49%；e.6号页岩片状伊蒙混层间充填了有机质，feng112，Es3x，TOC=6.85%，Ro=0.53%Fig. 3. OM-clay-sulfate complexes in the Dongying sag
图 4 东营凹陷沙四上亚段页岩富含有机质矿物混合体孔隙电子图像和能谱图a.2号有机质、粘土、碳酸盐混合体中发育的孔隙，wang129，Es4s，TOC=3.97%，Ro=0.32%；b.4号方解石、有机质和粘土混合体中发育孔隙，lai109，Es4s，TOC=5.31%，Ro=0.43%；c.8号有机质、粘土、碳酸盐混合体中发育的孔隙，niu872，Es3x，TOC=7.03%，Ro=0.55%；d.9号有机质、粘土、碳酸盐混合体中发育的孔隙，fengshen1，Es4s，TOC=2.30%，Ro=0.70%；e.10号有机质、粘土、碳酸盐混合体中发育的孔隙，wang78，Es3x，TOC=3.41%，Ro=0.66%；f.11号有机质、粘土、碳酸盐混合体中发育的孔隙，li673，Es3x，TOC=1.74%，Ro=0.82%；g.12号有机质、粘土、碳酸盐混合体中发育的孔隙，wang78，Es4s，TOC=3.63%，Ro=0.70%；h.13号硫酸盐有机质和粘土的混合体中发育的孔隙，li673，Es4s，TOC=3.49%，Ro=1.09%.C.有机质；I/S.伊蒙混层；Clay.粘土；Cc.方解石；Su.硫酸盐；Pr.黄铁矿；D.白云石；Q.石英Fig. 4. Pores in the Upper Es4 shales rich in OM-mineral complexes in the Dongying sag有机质-粘土-碳酸盐混合体内孔是东营凹陷沙三下、沙四上页岩中一种重要的孔隙类型，它从2 500~4 000 m连续分布，这类孔隙的发育涵盖了页岩的低成熟至高成熟演化阶段，与国外报道的有机孔隙发育与生烃转化有关，其主要出现在页岩高演化阶段具有一定的差异(Jarvie et al., 2007; Christopher and Scott, 2012).
3.2 有机质-粘土-碳酸盐混合体内孔成因分析
笔者对东营凹陷古近系页岩场发射电镜显微照片系统剖面进行观察发现，有机质-粘土-碳酸盐混合体演化孔开始出现的深度对应着页岩含油饱和度迅速增加的起始深度(图 5)，即排油门限(张林晔等，2005)，并且在小于3 600 m的深度范围内，镜下观察到有机质-粘土-碳酸盐混合体中发育的孔隙尺度较大，基本为微米级，笔者认为这类孔隙形成的机制包括两方面：即生烃作用和有机酸的溶蚀作用.
3.2.1 生烃作用
沙三下亚段和沙四上亚段页岩由于沉积环境的差异其沉积有机质的化学组成和结构也存在差异(Zhang et al., 1999, 2004, 2006)，咸水环境的沙四上亚段页岩中的有机质以非共价键缔合结构为主，非共价键的键能较低，以这种形式结合的有机质容易发生断裂，有机质发生转化所需要的温度较低，沙四上亚段页岩进入大量生烃并进行排烃的深度大约在2 500 m，页岩孔隙中含油饱和度迅速增加的起始深度也是在2 500 m左右.而半咸水环境的沙三下亚段页岩中的有机质以共价键缔合结构为主，共价键的键能要高于非共价键，有机质发生转化所需要的温度也要相应较高，沙三下亚段页岩进入大量生烃并进行排烃的深度大约在3 000 m(图 6)，页岩孔隙中含油饱和度迅速增加的起始深度对应3 000 m左右.在场发射电镜下观察到沙四上亚段页岩在2 500 m的深度开始出现有机质-粘土-碳酸盐混合体演化孔隙(图 4a)，而沙三下亚段页岩在3 100 m左右出现有机质-粘土-碳酸盐混合体演化孔隙(图 4c)，这两套页岩出现有机质-粘土-碳酸盐混合体演化孔隙的深度正好对应各自油气大量生成并开始排烃的深度，所以这类孔隙的形成与油气的生成和排驱有一定的关系，固体有机质因生成并排出一定量油气而形成空间.
图 6 不同湖相环境烃源岩生排烃模式差异Fig. 6. Different schemes of hydrocarbon generation and expulsion in lacustrine shales3.2.2 有机酸的溶蚀作用
有机酸的溶蚀作用是有机质-粘土-碳酸盐混合体演化孔隙形成的另一个重要原因.在泥页岩中有机酸的赋存形式有3种，即结合态有机酸、复合态有机酸和游离态有机酸.
结合态有机酸主要指羧基以酯的形式与页岩中的有机质如非烃、沥青和干酪根相结合形成的有机酸；复合态有机酸是指有机-无机复合体中的羧基与无机矿物和金属元素形成盐或有机复合物的有机酸；游离态有机酸主要指较易溶解于水的低碳数有机酸.另外，原油中也含有一定量的有机酸，主要包括正构饱和有机酸、正构不饱和有机酸、支链有机酸.
东营凹陷沙四段页岩中含有一定量结合态有机酸，沥青有机酸的含量0.002 0%~0.102 6%，干酪根有机酸的含量为0.008 5%~0.032 2%(表 2).结合态有机酸随埋深逐渐变小，但当进入排烃门限时(2 605 m)，沥青有机酸和干酪根有机酸的含量都有所增加，这一现象说明，结合态的有机酸在演化的过程中是可以生成的，这将对深部页岩溶蚀孔隙的发育具有重要意义.
表 2 东营凹陷沙四上亚段不同埋深页岩有机酸含量统计Table Supplementary Table Statistics of organic acid contents in the Upper Es4 shales at different depths in the Dongying sag编号 层位 埋深(m) 沥青“A”(μg/g) 族组成(%) 沥青酸(%) 干酪根酸(%) 烷烃 芳烃 非烃 沥青 SL952 Es4 1 138 2 476 9 5 80 6 0.036 5 0.016 3 SL953 Es4 1 341 11 253 10 8 70 12 0.102 6 0.032 2 SL954 Es4 2 021 1 454 16 7 70 7 0.016 6 0.014 9 SL955 Es4 2 605 8 294 50 15 29 6 0.029 5 0.020 3 SL957 Es4 3 608 5 049 35 15 41 9 0.002 0 0.008 5 据黄第藩等(黄第藩等, 2003)对辽河盆地古近系烃源岩中结合态的有机酸的模拟实验发现，随着热模拟温度的增加，干酪根有机酸的含量逐渐减少，它的减少可能一方面转化成了烃类，另一方面可能转移到非烃和沥青中了.加热到300 ℃后，沥青有机酸和干酪根有机酸略有增多现象，这可能与干酪根新生成的有机酸有关(表 2和表 3).自然演化剖面和模拟实验都表明页岩中结合态有机酸随演化程度升高而逐渐减少，在排烃门限附近结合态有机酸含量增加.结合态有机酸在演化的过程中转化成烃将形成有机储集空间.同时，由于结合态有机酸的脱羧作用将造成酸性环境，促使矿物的溶蚀而形成新的储集空间.
表 3 LH973页岩样品有机酸热模拟结果Table Supplementary Table Thermal simulation results on organic acid in LH973 shale样品 沥青/岩 沥青酸/岩 干酪根酸/岩 原样 2.470 0.400 0.102 175 ℃样 0.178 0.038 0.075 250 ℃样 0.169 0.024 0.011 300 ℃样 0.736 0.064 0.050 东营凹陷古近系页岩中含有丰富的游离态有机酸，笔者采用脱离子水低温超声萃取和离心分离前处理方法，利用离子色谱分别测定了东营凹陷古近系沙三下、沙四上、沙四下段页岩中低碳数游离态有机酸含量，该区游离态有机酸主要是甲酸、乙酸和草酸(表 4).
表 4 东营凹陷古近系泥页岩中游离态有机酸含量统计Table Supplementary Table Statistical contents of free state organic acid in the Paleogene shales in the Dongying sag层段 含量(μg/g) 乙酸根 甲酸根 草酸根 最小 最大 平均 最小 最大 平均 最小 最大 平均 Es3x 2.55 51.40 16.98 0.62 56.55 10.36 1.96 9.16 4.27 Es4s 0.00 69.06 19.49 3.38 45.42 14.64 0.00 6.56 4.14 Es4x 0.00 46.08 22.09 2.31 27.48 12.42 2.41 7.16 4.34 从表 4中可以看出，样品中甲酸根和乙酸根的含量明显高于草酸根的含量，即泥页岩中游离态的有机酸以低分子量的甲酸根和乙酸根为主.游离态总有机酸含量是沙四段下亚段＞沙四段上亚段＞沙三段下亚段，其数值分别是38.85 μg/g、38.27 μg/g和31.61 μg/g.游离态总有机酸含量的上述特征可能预示着有机酸含量与湖相环境存在一定关系，即盐度相对较高的环境有机酸含量更高一些.
从游离态有机酸含量随深度的变化来看(图 7和图 8)，从浅到深，有机酸含量经历了从低到高再到低的过程，在埋藏深度3 000 m左右出现峰值.游离态有机酸的形成过程与油气的生成过程基本是同步的，而且进入生烃高峰期以后，游离态有机酸仍保持了较高的含量.游离态有机酸与油气的生成过程保持了基本同步的特征也预示着泥页岩排出含烃流体的同时也伴随着大量的有机酸的排出，它不仅仅对泥页岩本身的孔隙结构产生影响，也将对砂岩、碳酸盐储层成岩过程和物性改变产生重要影响(郭佳等，2014).
图 7 东营凹陷不同层位页岩甲酸根随埋深关系Fig. 7. Relationship between formate in different shales and depth
图 8 东营凹陷不同层位页岩乙酸根随埋深关系Fig. 8. Relationship between acetate in different shales and depth通过对不同赋存状态有机酸的形成和演化的分析来看，它和油气的生成和排出是密切相关的，油气生成与有机酸的溶蚀对有机质-粘土-碳酸盐混合体演化孔隙的影响是同步的.笔者系统研究了东营凹陷古近系两套页岩总孔隙度的变化，从图 9中可以看出，沙四上亚段页岩孔隙度为0.3%~36.9%，沙三下亚段页岩孔隙度为0.21%~29.30%，分布范围较宽.从孔隙度与埋深关系来看，沙四上亚段页岩在2 800 m以浅，沙三下亚段页岩在3 000 m以浅整体孔隙度随深度增加而减小，且变化明显；而在埋深到达一定深度，即沙四上亚段页岩在2 800 m以深，沙三下亚段页岩在3 000 m以深，孔隙度值发生分异，部分样品的孔隙度随埋深增加而减小，而部分样品的孔隙度随埋深增加而增大.在2 800~3 000 m以浅，页岩孔隙度随埋深变小属于正常压实深度范围孔隙变化特点；而在2 800~3 000 m以深页岩孔隙度随埋深增大，主要是由于页岩的大量生烃，一方面固体有机质转化为流体烃类而导致孔隙度增加，另一方面，由于页岩生烃迅速导致生烃增压积累，岩石的有效应力下降致使页岩孔隙度增加(张善文等，2009；包友书等，2012；郭小文等，2013).同时在这个深度范围，伴随着有机质的演化排出大量有机酸使矿物溶解产生次生孔隙也是孔隙度增加的重要原因(图 4，图 7和图 8).
图 9 东营凹陷页岩孔隙度随埋深变化关系Fig. 9. Relationship between porosities and depths of shales in Dongying sag从东营凹陷古近系页岩的研究来看，由于在生烃高峰前(＜3 500 m)(图 6)，游离有机酸的含量相对较高(图 7和图 8)，溶蚀的影响要相对大一些，所以在这一阶段形成的有机质-粘土-碳酸盐混合体演化孔隙的尺度要大一些，一般为微米级.之后在机质-粘土-碳酸盐混合体中，随着有机酸的含量的降低，生烃作用产生的孔隙占主导作用，孔隙尺度多为纳米级，形态为蜂窝状，与国外报道的海相页岩高演化阶段的有机孔隙极为相似.
有机质-粘土-碳酸盐混合体演化孔隙是东营凹陷古近系页岩中一种重要的孔隙类型，它的形成是生烃和有机酸溶蚀共同作用的结果.
4. 结论
(1) 东营凹陷古近系沙三下段、沙四上段湖相页岩有机质丰度高，有机质类型为Ⅰ-Ⅱ1型，石英、碳酸盐等脆性矿物的含量大于粘土矿物含量，有机质演化主体处于生油窗范围.
(2) 利用氩离子抛光样品制备技术，分别使用Quanta200扫描电镜及EDAX能谱仪联机和JSM-6700f冷场发射扫描电子显微镜对处于生油窗范围的湖相页岩进行微观特征观察和岩石组分分析，镜下观察发现背散射图像中的暗色部分有机质富集，能谱分析表明，条带状暗色部分主要是有机质、粘土和碳酸盐混合体，部分沙四上段页岩为有机质-粘土-硫酸盐混合体.
(3) 背散射图像和二次电子图像均显示，有机质-粘土-碳酸盐或有机质-粘土-硫酸盐混合体内极易发育孔隙，从2 500~4 000 m，该类孔隙连续分布，基本涵盖了整个生油窗的范围.当埋深小于3 600 m时，这类孔隙的尺度一般为微米级，但随着演化程度增高纳米孔隙增加，并且呈密集分布.
(4) 有机质-粘土-碳酸盐和有机质-粘土-硫酸盐混合体内孔是东营凹陷古近系湖相页岩中一种重要的孔隙类型，这类孔隙的发育分别与页岩含油饱和度迅速增高及游离有机酸含量的增加同步，该类孔隙的发育不仅仅取决于生烃作用，它的形成是生烃转化和有机酸溶蚀共同作用的结果.
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图 1 乌兰敖包地区构造位置及区域地质略图
a.中亚造山带构造纲要图，据Jahn et al.(2000)修改；b.狼山地区构造纲要图，据Liu et al.(2016)修改
Fig. 1. Simplified geological map of Wulanaobao area and tectonic location
图 2 乌兰敖包地区“阿木山组”地层柱状图
Fig. 2. Stratigraphy stratum of Amushan Formation from Wulanaobao area
图 3 乌兰敖包地区“阿木山组”野外照片
a、b.阿木山组一段砂岩角度不整合在宝音图岩群大理岩之上；c.阿木山组一段砂岩中板状交错层理；d.阿木山组二段砂岩中平行层理；e.二段细砂岩中座延羊齿Alethopteris sp.(未定种)；f.二段灰岩中珊瑚化石；g.二段细砂岩中带科达Cordaites principalis Gein
Fig. 3. Outcrop photos of Amushan Formation in Wulanaobao area
图 4 乌兰敖包地区“阿木山组”中砂岩样品野外和镜下特征
a、b.阿木山组一段岩屑石英粗砂岩(P4-89)；c、d.阿木山组二段长石岩屑粗砂岩(B030)
Fig. 4. Characteristics of sandstone from Amushan Formation in Wulanaobao area
图 5 乌兰敖包地区砂岩部分碎屑锆石阴极发光图像
Fig. 5. CL images and ages of partial detrital zircons from Amushan Formation sandstone in Wulanaobao area
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