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GEOFLUIDS

Geofluids

1468 - 8123 1468 - 8115

Hindawi

10.1155 / 2020/9037429 9037429

研究文章

断裂、溶解和奥陶系碳酸盐储层胶结事件,塔里木盆地,西北中国

https://orcid.org/0000 - 0002 - 7779 - 4297 Baques Vinyet

Ukar Estibalitz Laubach 斯蒂芬·E。 Forstner 斯蒂芬妮·R。秋天安德拉斯 Gomez-Rivas 恩里克

经济地质学杰克逊地质学校德克萨斯大学奥斯汀分校 X奥斯汀大学站框 TX 78713 - 8924 美国 utexas.edu

2020年

18 4 2020年

2020年 18 10 2019年 12 01 2020年 14 02 2020年 18 4 2020年

这是一个开放的文章在知识共享归属许可下发布的,它允许无限制的使用,分布和繁殖在任何媒介,提供最初的工作是正确的引用。

奥陶系碳酸盐岩的形成Yijianfang Tabei隆起,塔里木盆地,含深埋地下的(> 6000),高产的石油和天然气储层与大蛀牙(> 10米)。之前的工人推断,大型腔paleocaves(古喀斯特)埋在地表附近,随后形成的。交替,形成的洞穴可能解散沿着断层深度。使用227 16核心样本,我们文档纹理和水泥复合轴承腔的历史与岩相、高分辨率扫描电子显微镜(SEM),同位素和流体包裹体microthermometric观察。结果表明,解散发生在深度和是由(1)酸性液体来源于中晚期的志留纪和/或Devonian-Permian生烃和成熟,(2)高温流体,其中一些是与晚二叠纪岩浆活动有关,和(3)Mg-rich液体,总结变形和部分开放性骨折和stylobreccias的形成(断层角砾岩)。的相对共生序列组织成岩作用表明压裂的七个阶段,溶蚀、胶结。斑点的面料Yijianfang形成含有泥质飞船在淤泥和生物扰动作用特性在海洋环境中形成的。那些斑驳的面料显然不同于上覆Lianglitage形成岩溶特征,由近地表解散和随后的填入外来沉积物的蛀牙。斑点面料是由压缩骨折横切充满phreatic-vadose海洋水泥和紧随其后的是后代注入水泥骨折和岩穴表明一些骨折和岩穴成为水泥填充后解散前的事件。方解石胶结物在骨折和岩穴逐渐枯竭的值 δ^{18O记录水泥降水在浅(220 ~),中间(625 ~),和深度(~ 2000)成岩环境。因此深(中期形成的)解散与骨折相关的高porosity-permeability水库的主要来源,与其他证据一致的蛀牙局部断层附近。

美国能源部

DE-FG02-03ER15430

骨折研究与应用联盟

CNPC-Tarim油田公司

CNPC-USA

1。介绍</gydF4y2Batitle>
<p>巨大的石油和天然气被包含在塔里木盆地奥陶系碳酸盐岩,西北中国,尤其是在他隆起,已探明石油/天然气储量超过30亿吨石油当量(<gydF4y2Baxref ref-type="bibr" rid="B1">
1</gydF4y2Baxref>]。钻井等反应和泥浆损失下降表明,多孔和效果区域,包括大型(> 10米)蛀牙,存在于深埋地下水库(> 6000)(<gydF4y2Baxref ref-type="bibr" rid="B2">
2</gydF4y2Baxref>- - - - - -<gydF4y2Baxref ref-type="bibr" rid="B5">
5</gydF4y2Baxref>]。被安置在许多经济碳酸盐岩储层岩石保护早期溶蚀孔隙度由陨石diagenesis-karstification-prior显著的葬礼(<gydF4y2Baxref ref-type="bibr" rid="B6">
6</gydF4y2Baxref>- - - - - -<gydF4y2Baxref ref-type="bibr" rid="B12">
12</gydF4y2Baxref>]。然而,在许多环境中,越来越多的证据支持的形成次生孔隙度在晚deep-burial条件(中期形成的;讨论了吉尔和马歇尔(<gydF4y2Baxref ref-type="bibr" rid="B13">
13</gydF4y2Baxref>],Mazzullo和哈里斯[<gydF4y2Baxref ref-type="bibr" rid="B14">
14</gydF4y2Baxref>],赖特和哈里斯(<gydF4y2Baxref ref-type="bibr" rid="B15">
15</gydF4y2Baxref>腐蚀性成岩流体)的不同性质(<gydF4y2Baxref ref-type="bibr" rid="B16">
16</gydF4y2Baxref>- - - - - -<gydF4y2Baxref ref-type="bibr" rid="B20">
20.</gydF4y2Baxref>]。</gydF4y2Bap>
<p>深层碳酸盐岩孔隙网络的起源Yijianfang塔里木盆地中部形成的讨论(<gydF4y2Baxref ref-type="bibr" rid="B4">
4</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B5">
5</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B21">
21</gydF4y2Baxref>- - - - - -<gydF4y2Baxref ref-type="bibr" rid="B23">
23</gydF4y2Baxref>]。岩溶特征出现在中奥陶世碳酸盐在附近Lunnan和塔河油田(<gydF4y2Baxref ref-type="bibr" rid="B2">
2</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B24">
24</gydF4y2Baxref>- - - - - -<gydF4y2Baxref ref-type="bibr" rid="B27">
27</gydF4y2Baxref>]。在这里,蛀牙与120 m.y的中断。沉积之前志留纪硅质碎屑的岩石(<gydF4y2Baxref ref-type="bibr" rid="B2">
2</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B25">
25</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B28">
28</gydF4y2Baxref>]。在古构造低Halahatang地区,然而,一个良好定义的不整合(缺席<gydF4y2Baxref ref-type="bibr" rid="B29">
29日</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B30">
30.</gydF4y2Baxref>]。近地表岩溶的主要证据是所谓的斑驳的面料,纹理Yijianfang形成中非常常见。这个功能已经被解释为近地表古喀斯特角砾岩或沉积物填充岩穴/腔[<gydF4y2Baxref ref-type="bibr" rid="B31">
31日</gydF4y2Baxref>- - - - - -<gydF4y2Baxref ref-type="bibr" rid="B34">
34</gydF4y2Baxref>但最近引入的问题[<gydF4y2Baxref ref-type="bibr" rid="B22">
22</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B35">
35</gydF4y2Baxref>]。此外,区域结构解释和断层映射Halahatang地区揭示网络共轭走向滑动断层系统,开发破坏区具有良好的协议与高生产(<gydF4y2Baxref ref-type="bibr" rid="B36">
36</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B37">
37</gydF4y2Baxref>]。吴et al。<gydF4y2Baxref ref-type="bibr" rid="B37">
37</gydF4y2Baxref>]暗示有更多解散发达沿着断层破坏区,表明流体通路在这些地区促进形成断层后解散。洞发育high-matrix水库和水库是相当不同的岩溶水库(陨石<gydF4y2Baxref ref-type="bibr" rid="B9">
9</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B38">
38</gydF4y2Baxref>),但强烈非均质储层接近中期形成的解散或热液岩溶作用沿断层带(<gydF4y2Baxref ref-type="bibr" rid="B14">
14</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B21">
21</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B39">
39</gydF4y2Baxref>]。</gydF4y2Bap>
<p>溶解过程部分或完全消除原始microstratigraphic和结构记录。沉淀水泥另一方面,尤其是precorrosion和postdissolution矿物充填龋齿和骨折,可能记录信息的元素和同位素化学溶解液参与结构成岩事件(<gydF4y2Baxref ref-type="bibr" rid="B40">
40</gydF4y2Baxref>]。水泥提供信息的物理和化学条件下储层在不同的成岩作用阶段,以及液体的组成,并允许获取信息,否则将无法从空的空洞。横切水泥和流体包裹体序列被困在他们可以提供洞察原点,液体的类型和途径以及深度的解散和胶结事件随时间(<gydF4y2Baxref ref-type="bibr" rid="B41">
41</gydF4y2Baxref>- - - - - -<gydF4y2Baxref ref-type="bibr" rid="B44">
44</gydF4y2Baxref>]。我们使用岩相学、扫描电子显微镜(SEM)、C、O,和锶同位素和流体包裹体显微温度学的核心样本16井Halahatang油田建立共生序列,温度条件下,液体和起源的事件,导致神秘的斑点的形成纹理以及溶解岩穴和骨折在这些深埋地下的奥陶系碳酸盐岩储层(5500 - 7500)。</gydF4y2Bap>
<p>在这里,我们表明,深(中期形成的)解散与骨折有关当前打开的蛀牙在水库的主要来源。斑点面料不是彻骨的岩溶过程的结果,但表示后来被中期形成的叠覆解散的洞穴。我们发现没有证据表明普遍的近地表解散。我们文档叠覆压裂的七阶段和解散,与降水的水泥的海洋深成岩环境。稳定同位素分析与地热梯度显示大部分的解散,先于每个额外fracture-dissolution事件发生在中期形成的环境中(220 - 2000)。溶解在不同阶段引起一系列的液体,包括大气、有机酸和高温和Mg-rich液体。</gydF4y2Bap>
</sec>
<sec id="sec2">
<title>2。地质背景</gydF4y2Batitle>
<p>塔里木盆地是中国西部最大的克拉通区占地面积近600000公里<gydF4y2Basup>2</gydF4y2Basup>(图<gydF4y2Baxref rid="fig1" ref-type="fig">
1</gydF4y2Baxref>)。盆地为界,西北的天山山脉,Kuluketage地区东北部,昆仑山脉南部和西南部、东南部,但是断裂带(图<gydF4y2Baxref rid="fig1" ref-type="fig">
1</gydF4y2Baxref>)。的前寒武纪结晶基底代表一个片段Rodinia超大陆经历了长期的地质演化的震旦(最新新元)新第三纪(<gydF4y2Baxref ref-type="bibr" rid="B45">
45</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B46">
46</gydF4y2Baxref>]。除了洪流玄武岩塔里木火成岩省的马~ 290 (<gydF4y2Baxref ref-type="bibr" rid="B47">
47</gydF4y2Baxref>)(图<gydF4y2Baxref rid="fig1" ref-type="fig">
1</gydF4y2Baxref>),塔里木盆地的演化特征是新元古代以来几乎连续沉积。长期多环塔里木盆地的构造演化形成了三个paleohighs(他、Tazhong中部和东南部Tadong)和四个萧条(库车、Manjiaer Tangguzibasi西南部和东南部Tadong) (<gydF4y2Baxref ref-type="bibr" rid="B45">
45</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B48">
48</gydF4y2Baxref>- - - - - -<gydF4y2Baxref ref-type="bibr" rid="B54">
54</gydF4y2Baxref>)(图<gydF4y2Baxref rid="fig1" ref-type="fig">
1</gydF4y2Baxref>)。末Sinian-Early奥陶纪时期,塔里木盆地是在扩展导致一系列正常的缺点和horst-graben结构(<gydF4y2Baxref ref-type="bibr" rid="B45">
45</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B55">
55</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B56">
56</gydF4y2Baxref>]。paleo-Altun的被动大陆边缘和海洋paleo-Kunlun塔里木南部的转换为一个活动大陆边缘的中奥陶世,经历强烈压缩从南到北,形成大规模的中产加里东推力带(<gydF4y2Baxref ref-type="bibr" rid="B45">
45</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B55">
55</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B56">
56</gydF4y2Baxref>]。奥陶系碳酸盐岩滇池流域暴露和部分侵蚀是由于隆起与加里东和海西造山运动(Ordovician-Permian),生成一系列的不整合和/或一致(图<gydF4y2Baxref ref-type="fig" rid="fig2">
2</gydF4y2Baxref>),和无处不在的岩溶事件直接相关的中断(<gydF4y2Baxref ref-type="bibr" rid="B25">
25</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B57">
57</gydF4y2Baxref>]。后关闭paleo-Altun、paleo-Kunlun paleo-Tianshan海洋海西晚期,塔里木变成陆内盆地在印支和有经验的连续沉积和埋葬。Indonesian-Yanshanian (Triassic-Cretaceous)在山坡上以密集的断裂构造带,而在喜马拉雅(新生代),断层集中在前陆盆地,密集的隆升密切相关,抽插,走向滑动推力,推力或走滑造山带周围的<gydF4y2Baxref ref-type="bibr" rid="B51">
51</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B58">
58</gydF4y2Baxref>]。盆地经历了一段快速埋葬自5 Ma (<gydF4y2Baxref ref-type="bibr" rid="B51">
51</gydF4y2Baxref>]。</gydF4y2Bap>
<fig id="fig1">
<label>图1</lgydF4y2Baabel>
<p>简化了塔里木盆地的大地构造图显示paleouplifts和萧条(赵后et al。<gydF4y2Baxref ref-type="bibr" rid="B25">
25</gydF4y2Baxref>]),平台的分配利润的奥陶系碳酸盐(林后et al。<gydF4y2Baxref ref-type="bibr" rid="B59">
59</gydF4y2Baxref>]),发生的玄武岩塔里木大火成岩省(徐后et al。<gydF4y2Baxref ref-type="bibr" rid="B47">
47</gydF4y2Baxref>])。</gydF4y2Bap>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.001"></graphic>
</fig>
<fig id="fig2">
<label>图2</lgydF4y2Baabel>
<p>地层和岩性Paleozoic-Cenozoic塔里木盆地沉积物,显示主要不整合和构造造山运动(修改Chang et al。<gydF4y2Baxref ref-type="bibr" rid="B57">
57</gydF4y2Baxref>和赵et al。<gydF4y2Baxref ref-type="bibr" rid="B25">
25</gydF4y2Baxref>])。</gydF4y2Bap>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.002"></graphic>
</fig>
<p>他在塔里木盆地北部隆起(图<gydF4y2Baxref rid="fig1" ref-type="fig">
1</gydF4y2Baxref>)由一系列Sinian-Devonian海洋,Carboniferous-Permian marine-terrigenous,和Triassic-Quaternary陆地沉积岩<gydF4y2Baxref ref-type="bibr" rid="B25">
25</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B59">
59</gydF4y2Baxref>)(图<gydF4y2Baxref ref-type="fig" rid="fig2">
2</gydF4y2Baxref>)。油气藏主要分布在奥陶系碳酸盐岩。在这段时间里,平台边缘延伸超过3000公里,间歇性地迁移和生产复杂的序列结构由于盆地构造作用之间的相互作用,地形开发和海平面变化(<gydF4y2Baxref ref-type="bibr" rid="B59">
59</gydF4y2Baxref>]。Halahatang油田(图<gydF4y2Baxref ref-type="fig" rid="fig3a">
3(一个)</gydF4y2Baxref>)位于Halahatang萧条,接壤轮台北隆起,Shuntuoguole低隆起南部,东部Lunnan低隆起,塔北低隆起西部[<gydF4y2Baxref ref-type="bibr" rid="B60">
60</gydF4y2Baxref>- - - - - -<gydF4y2Baxref ref-type="bibr" rid="B62">
62年</gydF4y2Baxref>]。其他重要的提升包括塔河油田Tabei和Lunnan油田东部[<gydF4y2Baxref ref-type="bibr" rid="B57">
57</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B63">
63年</gydF4y2Baxref>]。在Halahatang油田奥陶系系统包括了奥陶系鹰山形成(O<gydF4y2Basub>1 - 2</gydF4y2Basub>y)中奥陶世Yijianfang形成(O<gydF4y2Basub>2</gydF4y2Basub>y)和上奥陶系Tumuxiuke (O<gydF4y2Basub>3</gydF4y2Basub>t)和Lianglitage (O<gydF4y2Basub>3</gydF4y2Basub>l)的形成(图<gydF4y2Baxref ref-type="fig" rid="fig2">
2</gydF4y2Baxref>)。中下奥陶系碳酸盐岩储层是高度异构的、紧凑的泥灰岩和泥岩盖层的地层上奥陶系Tumuxiuke, Lianglitage, Sangtamu形成(<gydF4y2Baxref ref-type="bibr" rid="B25">
25</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B57">
57</gydF4y2Baxref>]。</gydF4y2Bap>
<fig-group id="fig3">
<label>图3</lgydF4y2Baabel>
<p>(一)主要油田Halahatang抑郁和Lunnan隆起(Chang et al。<gydF4y2Baxref ref-type="bibr" rid="B63">
63年</gydF4y2Baxref>])。红场显示了区域研究的核心。(b)吴Halahatang地区主要断层的痕迹(et al。<gydF4y2Baxref ref-type="bibr" rid="B36">
36</gydF4y2Baxref>])和位置的研究核心(绿点)。</gydF4y2Bap>
<fig id="fig3a">
<label>(一)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.003a"></graphic>
</fig>
<fig id="fig3b">
<label>(b)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.003b"></graphic>
</fig>
</fig-group>
</sec>
<sec id="sec3">
<title>3所示。材料和方法</gydF4y2Batitle>
<p>我们收集了227个样本的鹰,Yijianfang Tumuxiuke, Lianglitage形成来自16个核心研究区域(图<gydF4y2Baxref rid="fig3b" ref-type="fig">
3 (b)</gydF4y2Baxref>)。其中,262坯料被选为岩相分析标准的光学显微镜,强调Yijianfang形成。薄片染色茜素红S和铁氰化钾一半为了促进铁和nonferroan方解石的识别,以及白云石(<gydF4y2Baxref ref-type="bibr" rid="B64">
64年</gydF4y2Baxref>]。</gydF4y2Bap>
<p>四十薄片在阴极发光显微镜下检查(optical-CL)使用Reliotron三世阴极发光附件在10 - 18 kV枪潜力和0.5 - -0.6 V电子束电流。石灰岩地质结构特征和成岩胶结物是研究使用蔡司σ高真空场发射扫描电子显微镜(高压FE-SEM)。碳涂层样品(~ 15<gydF4y2Baitalic>
n</gydF4y2Baitalic>m)成像在SEM-CL Gatan MonoCL4探测器在5 kV和120年<gydF4y2Baitalic>
μ</gydF4y2Baitalic>米孔径。研究纳米级孔隙的形态和分布,我们跟着样品制备协议所描述的劳克斯et al。<gydF4y2Baxref ref-type="bibr" rid="B65">
65年</gydF4y2Baxref>]。我们准备好的<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M1">
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66年</gydF4y2Baxref>]。样本然后涂有5 nm的铱和分析使用范Nova 430 FE-SEM Nano。操作条件是10 - 15千伏,现货3 - 5纳米的大小,和光圈的30<gydF4y2Baitalic>
μ</gydF4y2Baitalic>m。</gydF4y2Bap>
<p>主机的岩石和断裂,vug-filling方解石胶结物的足够的样品(<gydF4y2Bainline-formula>
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我</gydF4y2Baxref>和<gydF4y2Baxref ref-type="supplementary-material" rid="supplementary-material-1">
二世</gydF4y2Baxref>)。分析了整除~ 0.3毫克<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C和<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O利用热费希尔科学GasBench II耦合热费希尔科学垫253同位素比率质谱计<gydF4y2Baxref ref-type="bibr" rid="B67">
67年</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B68">
68年</gydF4y2Baxref>]。样本的反应在helium-flushed瓶103% H<gydF4y2Basub>3</gydF4y2Basub>阿宝<gydF4y2Basub>4</gydF4y2Basub>在3小时50°C。数据校准使用方解石标准NBS-18 (<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M3">
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5.0</米米l:mn>
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</inline-formula>)和NBS-19 (<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M5">
<mml:msup>
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<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M6">
<mml:msup>
<mml:mrow>
<mml:mi>
δ</米米l:mi>
</mml:mrow>
<mml:mrow>
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</mml:mrow>
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<mml:mn>
1.95</米米l:mn>
<mml:mtext>
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</mml:math>
</inline-formula>)。十二碳酸复制的一个内部标准分析了整个分析会话占分析漂移和精度,达到±0.06‰的分析精度<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C<gydF4y2Basub>VPDB</gydF4y2Basub>和±0.10‰<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O<gydF4y2Basub>VPDB</gydF4y2Basub>经常。</gydF4y2Bap>
<p>碳酸盐样本淋溶pH值在0.2 M醋酸铵酸消化前8的锶同位素分析。方解石在4%醋酸10分钟和消化白云石在8%醋酸15分钟。老在3 M HNO分离<gydF4y2Basub>3</gydF4y2Basub>在70年使用Eichrom Sr特定树脂<gydF4y2Baitalic>
μ</gydF4y2Baitalic>l列。老的总过程空白样品<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M7">
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l</米米l:mtext>
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30.</米米l:mn>
<mml:mtext>
</mml:mtext>
<mml:mtext>
pg</米米l:mtext>
</mml:math>
</inline-formula>。Sr样本装上单与氟钽丝和0.05磷酸,随后分析了热费希尔Triton热电离质谱仪在静态模式。强度<gydF4y2Basup>87年</gydF4y2Basup>老的<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M8">
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8</米米l:mn>
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5</米米l:mn>
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</mml:math>
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<mml:msup>
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<mml:mrow>
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老</米米l:mtext>
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<mml:mrow>
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86年</米米l:mn>
</mml:mrow>
</mml:msup>
<mml:mtext>
老</米米l:mtext>
<mml:mo>
=</米米l:mo>
<mml:mn>
8.375209</米米l:mn>
</mml:math>
</inline-formula>和一个指数律。</gydF4y2Bap>
<p>流体包裹体显微温度学20双抛光薄片进行使用气体流heating-freezing阶段(液、Inc.-adapted、美国地质Survey-type)安装在一个奥林巴斯BX-51显微镜。舞台是校准使用有限公司<gydF4y2Basub>2</gydF4y2Basub>冰融化和H<gydF4y2Basub>2</gydF4y2Basub>阿冰融化和关键(合成流体包裹体均一化温度<gydF4y2Baxref ref-type="bibr" rid="B69">
69年</gydF4y2Baxref>]。流体包裹体岩相学和显微温度学遵循的程序和·博德纳尔<gydF4y2Baxref ref-type="bibr" rid="B70">
70年</gydF4y2Baxref>]。液汽均匀化温度(<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M10">
<mml:msub>
<mml:mrow>
<mml:mi>
T</米米l:mi>
</mml:mrow>
<mml:mrow>
<mml:mtext>
h</米米l:mtext>
</mml:mrow>
</mml:msub>
</mml:math>
</inline-formula>)被确定为±1.0°C的使用温度热循环步骤0.5°C (<gydF4y2Baxref ref-type="bibr" rid="B71">
71年</gydF4y2Baxref>(补充材料<gydF4y2Baxref ref-type="supplementary-material" rid="supplementary-material-1">
三世</gydF4y2Baxref>)。</gydF4y2Bap>
</sec>
<sec id="sec4">
<title>4所示。结果</gydF4y2Batitle>
<sec id="sec4.1">
<title>4.1。岩相学</gydF4y2Batitle>
<sec id="sec4.1.1">
<title>以下4.4.1。主机的岩石</gydF4y2Batitle>
<p>上鹰和Yijianfang形成我们的研究领域包括内碎屑泥粒灰岩和粒状灰岩(图<gydF4y2Baxref ref-type="fig" rid="fig4a">
4(一)</gydF4y2Baxref>)。这些相最好的开发研究区北部(图<gydF4y2Baxref ref-type="fig" rid="fig3b">
3 (b)</gydF4y2Baxref>通过我井),虽然不丰富,他们也共同在南部(图<gydF4y2Baxref ref-type="fig" rid="fig3b">
3 (b)</gydF4y2Baxref>通过P井),J。这些岩相表明沉积在浅水高能环境内wave-dominated架子上。mud-dominated Tumuxiuke形成,主要由生物碎屑wackestones和疗效泥wackestones(图<gydF4y2Baxref ref-type="fig" rid="fig4b">
4 (b)</gydF4y2Baxref>),这表明沉积环境是相对较低的能源和深层海洋水在海侵时期。的基底部分Lianglitage鲕粒的形成主要是由谷物和生物碎屑颗粒岩(图<gydF4y2Baxref ref-type="fig" rid="fig4c">
4 (c)</gydF4y2Baxref>),这表明基底的部分可能是沉积鲕粒浅滩或生物碎屑浅滩。向上,Lianglitage形成变化成疗效泥内碎屑泥粒灰岩和/或生物碎屑wackestone,和疗效泥wackestone也是本地,表明低——中能沉积环境。上间隔含有更多的细粒度的硅质碎屑的沉积物,表明陆源沉积物碳酸盐系统的整合。</gydF4y2Bap>
<fig-group id="fig4">
<label>图4</lgydF4y2Baabel>
<p>奥陶系碳酸盐的显微照片。(一)平面光的光学显微照片Yijianfang形成,Tumuxiuke形成(b)和(c) Lianglitage形成岩石。IP =颗粒间的孔隙;第九=晶间孔。(d) Optical-CL显微照片的颗粒岩巩固了纤维刃的方解石(Cc0a)和晶簇状的边缘镶嵌(Cc0b)水泥。(e) Optical-CL显微照片的颗粒岩巩固了共轴水泥(Cc0c)。(f)手标本内的岩溶地平线Lianglitage形成显示matrix-rich, clast-supported混乱的角砾岩。(g)平面光的光学显微照片角Lianglitage形成红色碎屑角砾岩。(h)显微照片特写的角砾岩矩阵。</gydF4y2Bap>
<fig id="fig4a">
<label>(一)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.004a"></graphic>
</fig>
<fig id="fig4b">
<label>(b)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.004b"></graphic>
</fig>
<fig id="fig4c">
<label>(c)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.004c"></graphic>
</fig>
<fig id="fig4d">
<label>(d)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.004d"></graphic>
</fig>
<fig id="fig4e">
<label>(e)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.004e"></graphic>
</fig>
<fig id="fig4f">
<label>(f)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.004f"></graphic>
</fig>
<fig id="fig4g">
<label>(g)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.004g"></graphic>
</fig>
<fig id="fig4h">
<label>(h)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.004h"></graphic>
</fig>
</fig-group>
<p>粒状灰岩、泥粒灰岩和wackestones形成包含原生孔隙度小,主要在intraparticle及晶间的形式<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M11">
<mml:mtext>
毛孔</米米l:mtext>
<mml:mo>
<</米米l:mo>
<mml:mn>
150年</米米l:mn>
<mml:mtext>
</mml:mtext>
<mml:mi>
μ</米米l:mi>
<mml:mtext>
米</米米l:mtext>
</mml:math>
</inline-formula>直径(图<gydF4y2Baxref rid="fig4c" ref-type="fig">
4 (c)</gydF4y2Baxref>)。Intraparticle毛孔大多发生在骨骼碎片棘皮动物、苔藓虫等。Lianglitage形成,intraparticle毛孔最丰富和局部颗粒岩区间,在那里他们是完全充满了沥青(图<gydF4y2Baxref rid="fig4c" ref-type="fig">
4 (c)</gydF4y2Baxref>)。在没有改变主岩颗粒间的微孔率可以忽略不计。</gydF4y2Bap>
<p>颗粒间的孔隙中充满了纤维刃的rim (Cc0a)、晶簇状的马赛克(Cc0b)和共轴方解石胶结物(Cc0c)(表<gydF4y2Baxref rid="tab1" ref-type="table">
1</gydF4y2Baxref>)。Cc0a水泥钢圈通常小于10<gydF4y2Baitalic>
μ</gydF4y2Baitalic>米厚,一般形式的第一代水泥颗粒岩和grain-dominated泥粒灰岩(图<gydF4y2Baxref rid="fig4d" ref-type="fig">
4 (d)</gydF4y2Baxref>)。Cc0b从细到粗结晶(50至250年<gydF4y2Baitalic>
μ</gydF4y2Baitalic>米),主要发生在intraparticle和颗粒间的孔隙。Cc0c增生水泥通常是250<gydF4y2Baitalic>
μ</gydF4y2Baitalic>米到1毫米大小和在echinoderm-dominant常见生物碎屑颗粒岩和泥粒灰岩(图<gydF4y2Baxref rid="fig4e" ref-type="fig">
4 (e)</gydF4y2Baxref>)。根据optical-CL, Cc0a和Cc0b给沉闷的红色发光(图<gydF4y2Baxref rid="fig4d" ref-type="fig">
4 (d)</gydF4y2Baxref>),而Cc0c显示nonluminescence划定的亮橙色发光(图<gydF4y2Baxref rid="fig4e" ref-type="fig">
4 (e)</gydF4y2Baxref>)。</gydF4y2Bap>
<table-wrap id="tab1">
<label>表1</lgydF4y2Baabel>
<p>总结的主要成岩岩相特征特性和水泥所示顺序(共生序列)。KB:矩阵岩溶角砾岩;F:骨折;V:解散晶簇;S:缝合线;答:方解石胶结物;Cs:方解石沉积;Dc:白云石水泥。</gydF4y2Bap>
<table>
<thead>
<tr>
<th align="left">功能</gydF4y2Bath>
<th align="center">水泥</gydF4y2Bath>
<th align="center">形成</gydF4y2Bath>
<th align="center">形态</gydF4y2Bath>
<th align="center">晶粒大小</gydF4y2Bath>
<th align="center">CL</gydF4y2Bath>
<th align="center">SEM-CL</gydF4y2Bath>
</tr>
</thead>
<tbody>
<tr>
<td align="left" rowspan="4">母岩</gydF4y2Batd>
<td align="center" rowspan="4">−</gydF4y2Batd>
<td align="center">鹰山</gydF4y2Batd>
<td align="center">泥晶灰岩</gydF4y2Batd>
<td align="center" rowspan="4">< 4毫米</gydF4y2Batd>
<td align="center" rowspan="4">橙色沉闷的红</gydF4y2Batd>
<td align="center" rowspan="4">Light-luminescent;稍微划</gydF4y2Batd>
</tr>
<tr>
<td align="center">Yijianfang</gydF4y2Batd>
<td align="center">泥晶灰岩</gydF4y2Batd>
</tr>
<tr>
<td align="center">Tumuxiuke</gydF4y2Batd>
<td align="center">泥晶灰岩</gydF4y2Batd>
</tr>
<tr>
<td align="center">Lianglitage</gydF4y2Batd>
<td align="center">泥晶灰岩</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="7">
<hr></td>
</tr>
<tr>
<td align="left" rowspan="3">母岩胶结</gydF4y2Batd>
<td align="center">Cc0a</gydF4y2Batd>
<td align="center">鹰山;Yijianfang;Tumuxiuke;Lianglitage</gydF4y2Batd>
<td align="center">rim</gydF4y2Batd>
<td align="center">< 10毫米</gydF4y2Batd>
<td align="center">无聊的红色</gydF4y2Batd>
<td align="center">Light-luminescent;稍微划</gydF4y2Batd>
</tr>
<tr>
<td align="center">Cc0b</gydF4y2Batd>
<td align="center">鹰山;Yijianfang;Tumuxiuke;Lianglitage</gydF4y2Batd>
<td align="center">晶簇状的</gydF4y2Batd>
<td align="center">50到250毫米</gydF4y2Batd>
<td align="center">无聊的红色</gydF4y2Batd>
<td align="center">黑暗——光发光;划</gydF4y2Batd>
</tr>
<tr>
<td align="center">Cc0c</gydF4y2Batd>
<td align="center">鹰山;Yijianfang;Tumuxiuke;Lianglitage</gydF4y2Batd>
<td align="center">共轴</gydF4y2Batd>
<td align="center">250毫米到1毫米</gydF4y2Batd>
<td align="center">Non-luminescent划定的明亮的橙色</gydF4y2Batd>
<td align="center">Light-luminescent;稍微划</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="7">
<hr></td>
</tr>
<tr>
<td align="left" rowspan="2">黑色的斑点</gydF4y2Batd>
<td align="center">Cs0a</gydF4y2Batd>
<td align="center">鹰山;Yijianfang;Tumuxiuke;</gydF4y2Batd>
<td align="center">淤泥</gydF4y2Batd>
<td align="center">< 20毫米</gydF4y2Batd>
<td align="center">橙色沉闷的红</gydF4y2Batd>
<td align="center">Light-luminescent;稍微划</gydF4y2Batd>
</tr>
<tr>
<td align="center">Cs0b</gydF4y2Batd>
<td align="center">顶级Yijianfang;Tumuxiuke</gydF4y2Batd>
<td align="center">泥</gydF4y2Batd>
<td align="center">< 4毫米</gydF4y2Batd>
<td align="center">橙色沉闷的红</gydF4y2Batd>
<td align="center">Light-luminescent;稍微划</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="7">
<hr></td>
</tr>
<tr>
<td align="left" rowspan="2">F1</gydF4y2Batd>
<td align="center">Cc1</gydF4y2Batd>
<td align="center">Yijianfang;Tumuxiuke;</gydF4y2Batd>
<td align="center">pallisade</gydF4y2Batd>
<td align="center">300 mm - 1毫米</gydF4y2Batd>
<td align="center">Non-luminescent划定的明亮的橙色</gydF4y2Batd>
<td align="center">Light-luminescent;稍微划</gydF4y2Batd>
</tr>
<tr>
<td align="center">Cs1</gydF4y2Batd>
<td align="center">Yijianfang;Tumuxiuke;</gydF4y2Batd>
<td align="center">淤泥</gydF4y2Batd>
<td align="center">10 - 75毫米</gydF4y2Batd>
<td align="center">Non-luminescent</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="7">
<hr></td>
</tr>
<tr>
<td align="left">岩溶角砾岩</gydF4y2Batd>
<td align="center">KB</gydF4y2Batd>
<td align="center">Lianglitage</gydF4y2Batd>
<td align="center">淤泥</gydF4y2Batd>
<td align="center">2毫米250毫米</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="7">
<hr></td>
</tr>
<tr>
<td align="left">V2</gydF4y2Batd>
<td align="center" rowspan="3">Cc2</gydF4y2Batd>
<td align="center" rowspan="3">鹰山;Yijianfang;Tumuxiuke;Lianglitage</gydF4y2Batd>
<td align="center" rowspan="3">块状</gydF4y2Batd>
<td align="center" rowspan="3">50 - 250毫米</gydF4y2Batd>
<td align="center" rowspan="3">Non-luminescent划定的明亮的橙色</gydF4y2Batd>
<td align="center" rowspan="3">黑暗——光发光;划</gydF4y2Batd>
</tr>
<tr>
<td align="left">F2a</gydF4y2Batd>
</tr>
<tr>
<td align="left">F2b</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="7">
<hr></td>
</tr>
<tr>
<td align="left">S1a &印地</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">鹰山;Yijianfang;Tumuxiuke;Lianglitage</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="7">
<hr></td>
</tr>
<tr>
<td align="left">F3a</gydF4y2Batd>
<td align="center" rowspan="2">Cc3a</gydF4y2Batd>
<td align="center" rowspan="2">鹰山;Yijianfang;Tumuxiuke;Lianglitage</gydF4y2Batd>
<td align="center" rowspan="2">rim</gydF4y2Batd>
<td align="center" rowspan="2">50 - 200毫米</gydF4y2Batd>
<td align="center" rowspan="2">深红色明亮的橙色发光</gydF4y2Batd>
<td align="center" rowspan="2">黑暗——light-luminescent;划</gydF4y2Batd>
</tr>
<tr>
<td align="left">F3b</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="7">
<hr></td>
</tr>
<tr>
<td align="left">F3c世锦赛</gydF4y2Batd>
<td align="center">沥青</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="7">
<hr></td>
</tr>
<tr>
<td align="left">V3</gydF4y2Batd>
<td align="center">Cc3b</gydF4y2Batd>
<td align="center">Lianglitage</gydF4y2Batd>
<td align="center">块状</gydF4y2Batd>
<td align="center">500 mm - 2毫米</gydF4y2Batd>
<td align="center">橙色发光</gydF4y2Batd>
<td align="center">Light-luminescent;unzoned</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="7">
<hr></td>
</tr>
<tr>
<td align="left">F4a</gydF4y2Batd>
<td align="center" rowspan="3">Cc4</gydF4y2Batd>
<td align="center" rowspan="3">Yijianfang;Tumuxiuke</gydF4y2Batd>
<td align="center" rowspan="3">块状</gydF4y2Batd>
<td align="center" rowspan="3">50 mm - 1毫米</gydF4y2Batd>
<td align="center" rowspan="3">红色发光</gydF4y2Batd>
<td align="center" rowspan="3">Dark-luminescent;unzoned</gydF4y2Batd>
</tr>
<tr>
<td align="left">F4b</gydF4y2Batd>
</tr>
<tr>
<td align="left">V4</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="7">
<hr></td>
</tr>
<tr>
<td align="left" rowspan="4">F5</gydF4y2Batd>
<td align="center">萤石</gydF4y2Batd>
<td align="center">Yijianfang</gydF4y2Batd>
<td align="center">自形的</gydF4y2Batd>
<td align="center">到5厘米</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center">重晶石</gydF4y2Batd>
<td align="center">Yijianfang</gydF4y2Batd>
<td align="center">自形的</gydF4y2Batd>
<td align="center">4毫米</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center">Cc5</gydF4y2Batd>
<td align="center">Yijianfang</gydF4y2Batd>
<td align="center">块状</gydF4y2Batd>
<td align="center">200 - 250毫米</gydF4y2Batd>
<td align="center">红色的红色发光</gydF4y2Batd>
<td align="center">Light-luminescent;稍微划</gydF4y2Batd>
</tr>
<tr>
<td align="center">再结晶母岩</gydF4y2Batd>
<td align="center">鹰山;Yijianfang</gydF4y2Batd>
<td align="center">水晶</gydF4y2Batd>
<td align="center">< 4 - 50 mm</gydF4y2Batd>
<td align="center">红色的红色发光</gydF4y2Batd>
<td align="center">Light-luminescent;稍微划</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="7">
<hr></td>
</tr>
<tr>
<td align="left">F6</gydF4y2Batd>
<td align="center" rowspan="2">Cc6</gydF4y2Batd>
<td align="center" rowspan="2">鹰山;Yijianfang</gydF4y2Batd>
<td align="center" rowspan="2">块状</gydF4y2Batd>
<td align="center" rowspan="2">200 - 600毫米</gydF4y2Batd>
<td align="center" rowspan="2">无聊的红色non-luminescent</gydF4y2Batd>
<td align="center" rowspan="2">光发光;unzoned</gydF4y2Batd>
</tr>
<tr>
<td align="left">V6</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="7">
<hr></td>
</tr>
<tr>
<td align="left">F7a</gydF4y2Batd>
<td align="center">Cc7a</gydF4y2Batd>
<td align="center">鹰山;Yijianfang;Tumuxiuke;Lianglitage</gydF4y2Batd>
<td align="center">桥梁</gydF4y2Batd>
<td align="center">50 - 100毫米</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">Light-luminescent;unzoned</gydF4y2Batd>
</tr>
<tr>
<td align="left">F7b</gydF4y2Batd>
<td align="center" rowspan="2">Cc7b</gydF4y2Batd>
<td align="center" rowspan="2">鹰山;Yijianfang;Tumuxiuke;Lianglitage</gydF4y2Batd>
<td align="center" rowspan="2">块状</gydF4y2Batd>
<td align="center" rowspan="2">50 mm - 1毫米</gydF4y2Batd>
<td align="center" rowspan="2">−</gydF4y2Batd>
<td align="center" rowspan="2">Light-luminescent;unzoned</gydF4y2Batd>
</tr>
<tr>
<td align="left">V7</gydF4y2Batd>
</tr>
<tr>
<td align="left">F7c & S2</gydF4y2Batd>
<td align="center">Dc1</gydF4y2Batd>
<td align="center">鹰山;Yijianfang;Tumuxiuke;Lianglitage</gydF4y2Batd>
<td align="center">自形的</gydF4y2Batd>
<td align="center">< 30毫米</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">Dark-luminescent</gydF4y2Batd>
</tr>
</tbody>
</table>
</table-wrap>
</sec>
<sec id="sec4.1.2">
<title>4.1.2。岩溶特征</gydF4y2Batitle>
<p>明确岩溶角砾岩包含外部Lianglitage形成沉积物只是观察。岩溶角砾岩包括裂纹角砾岩、马赛克角砾岩,clast-supported混乱的角砾岩,matrix-rich clast-supported混乱的角砾岩(图<gydF4y2Baxref rid="fig4f" ref-type="fig">
4 (f)</gydF4y2Baxref>)。最角砾碎屑有类似的岩性,浅红色,范围从非常好非常粗糙的鹅卵石大小,并稍有棱角的近圆形的形状(图<gydF4y2Baxref rid="fig4g" ref-type="fig">
4 (g)</gydF4y2Baxref>)。矩阵通常是黑棕色到红棕色和含有淤泥石英、粘土和铁氧化物形成鲜明的接触碎屑(图<gydF4y2Baxref rid="fig4h" ref-type="fig">
4 (h)</gydF4y2Baxref>)。</gydF4y2Bap>
</sec>
<sec id="sec4.1.3">
<title>4.1.3。斑点面料</gydF4y2Batitle>
<p>Yijianfang形成的一种独特的特点研究区是斑点面料(术语傅金et al .(2009)和(2019)),形成黑色的斑块与不规则几何图形(单一渠道或渠道的融合交织几何),突出核心样本。有些斑点织物圆或等分(图<gydF4y2Baxref ref-type="fig" rid="fig5a">
5(一个)</gydF4y2Baxref>),而其他人是细长的,这里被称为通道(数字<gydF4y2Baxref ref-type="fig" rid="fig5b">
5 (b)</gydF4y2Baxref>和<gydF4y2Baxref ref-type="fig" rid="fig5c">
5 (c)</gydF4y2Baxref>)。垂直和水平长通道内局部Yijianfang和Tumuxiuke地层的顶部。斑点面料是最好的发达在研究区北部(图<gydF4y2Baxref ref-type="fig" rid="fig3b">
3 (b)</gydF4y2Baxref>通过我井)。</gydF4y2Bap>
<fig-group id="fig5">
<label>图5</lgydF4y2Baabel>
<p>手标本中Yijianfang形成(a), Yijianfang形成(b), Tumuxiuke形成(c)显示圆形和长斑点面料(渠道)充满Cs0方解石沉积物。(d) Optical-CL泥粒灰岩的显微图显示次圆形的斑点面料充满方解石沉积Cs0a随后Cc2巩固了。(e, f)扫描电镜图片显示飞船碎片Cs0a内斑点面料。大部分的颗粒间的孔隙中充满了伊利石和/或沥青(f)。(g)平面光的光学显微照片充满了方解石沉积Cs0b wackestone显示垂直通道。(h i)扫描电镜图片显示飞船碎片Cs0b内垂直通道。大部分的颗粒间的孔隙中充满了伊利石、高岭石和/或沥青(我)。</gydF4y2Bap>
<fig id="fig5a">
<label>(一)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.005a"></graphic>
</fig>
<fig id="fig5b">
<label>(b)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.005b"></graphic>
</fig>
<fig id="fig5c">
<label>(c)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.005c"></graphic>
</fig>
<fig id="fig5d">
<label>(d)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.005d"></graphic>
</fig>
<fig id="fig5e">
<label>(e)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.005e"></graphic>
</fig>
<fig id="fig5f">
<label>(f)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.005f"></graphic>
</fig>
<fig id="fig5g">
<label>(g)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.005g"></graphic>
</fig>
<fig id="fig5h">
<label>(h)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.005h"></graphic>
</fig>
<fig id="fig5i">
<label>(我)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.005i"></graphic>
</fig>
</fig-group>
<p>圆形的斑点在Yijianfang面料形成包括内部,橙色,红色发光,泥质飞船<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M12">
<mml:mtext>
淤泥</米米l:mtext>
<mml:mtext>
</mml:mtext>
<mml:mfenced open="(" close=")">
<mml:mrow>
<mml:mtext>
Cs0a</米米l:mtext>
</mml:mrow>
</mml:mfenced>
<mml:mo>
<</米米l:mo>
<mml:mn>
20.</米米l:mn>
<mml:mtext>
</mml:mtext>
<mml:mi>
μ</米米l:mi>
<mml:mtext>
米</米米l:mtext>
</mml:math>
</inline-formula>在大小(图<gydF4y2Baxref ref-type="fig" rid="fig5d">
5 (d)</gydF4y2Baxref>)。小学(< 3%),中学(见下文)晶间微孔隙和纳米孔内斑点面料组成的~ 10%的体积岩石。大多数毛孔都少于20<gydF4y2Baitalic>
μ</gydF4y2Baitalic>米大小,包含3%伊利石,排列或满沥青(数字<gydF4y2Baxref ref-type="fig" rid="fig5e">
5 (e)</gydF4y2Baxref>和<gydF4y2Baxref ref-type="fig" rid="fig5f">
5 (f)</gydF4y2Baxref>)。相比之下,垂直和水平通道充满了各种混合物的支离破碎的化石和深棕色方解石泥岩矩阵,包含intergrown伊利石/绿泥石、石英、磷酸盐(Cs0b)(数据<gydF4y2Baxref ref-type="fig" rid="fig5g">
5 (g)</gydF4y2Baxref>和<gydF4y2Baxref ref-type="fig" rid="fig5h">
5 (h)</gydF4y2Baxref>)。晶间微孔隙在渠道构成< 10 - 15%的频道和部分填充的体积与5 - 10%伊利石、高岭石、沥青(图<gydF4y2Baxref ref-type="fig" rid="fig5i">
5(我)</gydF4y2Baxref>)。</gydF4y2Bap>
<p>奥陶系主机的岩石,包括斑点面料,由几种横切,一代又一代的部分完全巩固了骨折,缝合线,溶解岩穴(表<gydF4y2Baxref ref-type="table" rid="tab1">
1</gydF4y2Baxref>)。下面的分类建立了Yijianfang形成,但结构和地球化学相似性的基础上,我们把这种分类相似的特征出现在鹰山,Tumuxiuke, Lianglitage阵型。</gydF4y2Bap>
</sec>
<sec id="sec4.1.4">
<title>4.1.4。骨折</gydF4y2Batitle>
<p>横切关系的基础上,水泥填充的类型,我们定义了七组opening-mode骨折,从古老的(F1)到最小(F7)(表<gydF4y2Baxref ref-type="table" rid="tab1">
1</gydF4y2Baxref>)。Bed-perpendicular和bed-oblique calcite-filled骨折(F1)和不规则的墙壁和孔径0.5至1厘米的发生主要是在最Yijianfang和Tumuxiuke地层(图的一部分<gydF4y2Baxref ref-type="fig" rid="fig6a">
6(一)</gydF4y2Baxref>)。方解石水泥填充(Cc1)这些骨折包括等分刃的半形的晶体迅速分级栅栏形态。栅栏方解石晶体是300卡路里<gydF4y2Baitalic>
μ</gydF4y2Baitalic>米到1毫米长,10 - 50<gydF4y2Baitalic>
μ</gydF4y2Baitalic>米宽,可以开发3厘米厚度(图<gydF4y2Baxref ref-type="fig" rid="fig6b">
6 (b)</gydF4y2Baxref>)。晶体略微弯曲,起伏的灭绝。SEM-CL之下,他们是光发光和分区。前残余孔隙度在F1骨折充满内部黄色块状方解石组成的沉积物(Cs1) 10 - 75<gydF4y2Baitalic>
μ</gydF4y2Baitalic>米大小和粘土矿物(图<gydF4y2Baxref ref-type="fig" rid="fig6b">
6 (b)</gydF4y2Baxref>)。</gydF4y2Bap>
<fig-group id="fig6">
<label>图6</lgydF4y2Baabel>
<p>(一)手标本Tumuxiuke展示F1断裂形成。(b)平面光的光学显微照片栅栏方解石(Cc1)和内部沉积物(Cs1) F1断裂。(c)平面光的光学显微照片F2a骨折横切方解石沉积Cs0a在圆形的斑点面料。(d)平面光的光学显微照片显示F2b裂缝横切F2a骨折。(e) Optical-CL显微照片显示Cc2方解石充填F2骨折和V2岩穴。(f)的手标本Tumuxiuke形成显示F3骨折。F3断裂横切圆斑点面料。(g)全色SEM-CL图像显示Cc3a方解石晶体在SEM-CL分区。沥青填充剩余孔隙空间中心的骨折。(h i) Cc2和Cc3a方解石胶结物(h)平面光和optical-CL(我)。 (j) Hand sample specimen showing F4a fractures. (k) Plane light optical photomicrograph showing F4b fractures filled with blocky calcite (Cc4). (l) Plane light optical photomicrograph showing F4a fractures filled with blocky calcite (Cc4) and concurrent pyrite.</p>
<fig id="fig6a">
<label>(一)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.006a"></graphic>
</fig>
<fig id="fig6b">
<label>(b)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.006b"></graphic>
</fig>
<fig id="fig6c">
<label>(c)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.006c"></graphic>
</fig>
<fig id="fig6d">
<label>(d)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.006d"></graphic>
</fig>
<fig id="fig6e">
<label>(e)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.006e"></graphic>
</fig>
<fig id="fig6f">
<label>(f)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.006f"></graphic>
</fig>
<fig id="fig6g">
<label>(g)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.006g"></graphic>
</fig>
<fig id="fig6h">
<label>(h)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.006h"></graphic>
</fig>
<fig id="fig6i">
<label>(我)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.006i"></graphic>
</fig>
<fig id="fig6j">
<label>(j)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.006j"></graphic>
</fig>
<fig id="fig6k">
<label>(k)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.006k"></graphic>
</fig>
<fig id="fig6l">
<label>(左)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.006l"></graphic>
</fig>
</fig-group>
<p>第二组骨折(F2)包括bed-perpendicular和bed-oblique calcite-filled裂隙(< 0.5毫米孔径)直接不规则(s形)墙(F2a)(图<gydF4y2Baxref ref-type="fig" rid="fig6c">
6 (c)</gydF4y2Baxref>),平面,subhorizontal calcite-filled骨折(F2b)与光阑从100年<gydF4y2Baitalic>
μ</gydF4y2Baitalic>m(图4毫米<gydF4y2Baxref ref-type="fig" rid="fig6d">
6 (d)</gydF4y2Baxref>)。F2骨折存在于鹰、Yijianfang Tumuxiuke, Lianglitage形成。F2骨折充满了块状,分区,nonluminescent明亮的橙色方解石晶体(Cc2)在50到250不等<gydF4y2Baitalic>
μ</gydF4y2Baitalic>米直径(图<gydF4y2Baxref ref-type="fig" rid="fig6e">
6 (e)</gydF4y2Baxref>)。微米大小的(5 - 20<gydF4y2Baitalic>
μ</gydF4y2Baitalic>米)明亮的橙色Cc2方解石生长过度重叠Cs0a方解石沉积(图<gydF4y2Baxref ref-type="fig" rid="fig5d">
5 (d)</gydF4y2Baxref>)。</gydF4y2Bap>
<p>F3骨折出现在鹰山和Yijianfang岩层和一定程度上的Tumuxiuke和Lianglitage地层。这组包括bed-perpendicular和bed-oblique方解石,bitumen-filled骨折与直墙和孔径的100 - 500<gydF4y2Baitalic>
μ</gydF4y2Baitalic>m (F3a图<gydF4y2Baxref ref-type="fig" rid="fig6f">
6 (f)</gydF4y2Baxref>),略宽(500<gydF4y2Baitalic>
μ</gydF4y2Baitalic>m - 1厘米)骨折的类似的特征保留部分开孔率(F3b图<gydF4y2Baxref ref-type="fig" rid="fig6f">
6 (f)</gydF4y2Baxref>),平面bitumen-filled裂隙<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M13">
<mml:mtext>
光阑</米米l:mtext>
<mml:mo>
<</米米l:mo>
<mml:mn>
One hundred.</米米l:mn>
<mml:mtext>
</mml:mtext>
<mml:mi>
μ</米米l:mi>
<mml:mtext>
米</米米l:mtext>
</mml:math>
</inline-formula>(F3c世锦赛)。方解石胶结物在F3断裂是分区,深红色发光明亮的橙色,刃的块状rim水泥,50到200<gydF4y2Baitalic>
μ</gydF4y2Baitalic>米大小,自形的终端(Cc3a)(数据<gydF4y2Baxref ref-type="fig" rid="fig6g">
6 (g)</gydF4y2Baxref>- - - - - -<gydF4y2Baxref ref-type="fig" rid="fig6i">
6(我)</gydF4y2Baxref>)。保存一些F3断裂部分随后填充的多孔性沥青(数字<gydF4y2Baxref ref-type="fig" rid="fig6g">
6 (g)</gydF4y2Baxref>- - - - - -<gydF4y2Baxref ref-type="fig" rid="fig6i">
6(我)</gydF4y2Baxref>)。</gydF4y2Bap>
<p>第四组骨折(F4)是常见的Yijianfang形成和丰富Tumuxiuke和Lianglitage地层。这组包含平面bed-perpendicular和bed-oblique骨折介于0.5毫米和2厘米孔径与不规则的利润率和方解石+沥青±小晚黄铁矿水泥(F4a数字<gydF4y2Baxref ref-type="fig" rid="fig6j">
6 (j)</gydF4y2Baxref>和<gydF4y2Baxref ref-type="fig" rid="fig6l">
6(左)</gydF4y2Baxref>)和垂直裂隙,终止~ 1厘米距离水平缝合线和近似平行的缝合线的牙齿(F4b图<gydF4y2Baxref ref-type="fig" rid="fig6k">
6 (k)</gydF4y2Baxref>)。F4骨折充满了块状方解石晶体,50<gydF4y2Baitalic>
μ</gydF4y2Baitalic>米直径1毫米,在数据显示红色发光(Cc4<gydF4y2Baxref ref-type="fig" rid="fig6k">
6 (k)</gydF4y2Baxref>- - - - - -<gydF4y2Baxref ref-type="fig" rid="fig6l">
6(左)</gydF4y2Baxref>)。</gydF4y2Bap>
<p>骨折在第五集团(F5)只出现在鹰山和Yijianfang地层。F5骨折bed-perpendicular和/或bed-oblique床上用品,不规则的墙壁和孔径之间(图1毫米和> 7厘米<gydF4y2Baxref ref-type="fig" rid="fig7a">
7(一)</gydF4y2Baxref>)。F5骨折充满了自形的萤石、重晶石、方解石水泥(Cc5), 5厘米大小,在变量比例(图<gydF4y2Baxref ref-type="fig" rid="fig7b">
7 (b)</gydF4y2Baxref>),与方解石和天青石主机摇滚更换核心L, N, K(图<gydF4y2Baxref ref-type="fig" rid="fig3b">
3 (b)</gydF4y2Baxref>)。方解石和天青石成矿nonpenetrative和有限的几毫米至厘米远离F5断裂的墙壁。毛孔周围天青石晶体通常小于100<gydF4y2Baitalic>
μ</gydF4y2Baitalic>m大小(图<gydF4y2Baxref ref-type="fig" rid="fig7c">
7 (c)</gydF4y2Baxref>)。在大多数情况下,萤石和重晶石在方解石胶结(数字<gydF4y2Baxref ref-type="fig" rid="fig7a">
7(一)</gydF4y2Baxref>和<gydF4y2Baxref ref-type="fig" rid="fig7b">
7 (b)</gydF4y2Baxref>),虽然纹理模糊,天青石替代似乎萤石和重晶石矿化密切相关。在几个例子,重晶石和萤石似乎是同时代的人,而在别人,萤石是紧随其后的是方解石最后重晶石沉淀。Cc5 F5骨折是块状的,200年到250年<gydF4y2Baitalic>
μ</gydF4y2Baitalic>米,显示红色的红色发光(图<gydF4y2Baxref ref-type="fig" rid="fig7b">
7 (b)</gydF4y2Baxref>)。石英矿化(微晶quartzchert)发生在一些F5断裂(图<gydF4y2Baxref ref-type="fig" rid="fig7a">
7(一)</gydF4y2Baxref>)。硅化的区域内,形状各异的毛孔都高达400<gydF4y2Baitalic>
μ</gydF4y2Baitalic>米长(图<gydF4y2Baxref ref-type="fig" rid="fig7d">
7 (d)</gydF4y2Baxref>)。</gydF4y2Bap>
<fig-group id="fig7">
<label>图7</lgydF4y2Baabel>
<p>(一)手标本Lianglitage显示F5断裂形成巩固的萤石、方解石(Cc5)。硅沿断裂成矿母岩的墙。(b)平面光光学显微照片显示萤石、重晶石、方解石Cc5a水泥沉淀在F5断裂。(c)平面光的光学显微照片显示主岩的再结晶方解石和天青石矿化。注意毛孔(充满蓝色环氧树脂)形成在天青石晶体。(d) Plane-light光学显微照片显示部分替代寄主岩石的石英矿化。注意毛孔与硅的替代品。(e) Yijianfang形成的手标本显示F6骨折。(f)平面光的光学显微照片显示F6骨折填充Cc6水泥推迟日期Cc4-bearing F4骨折。(g)的手标本Yijianfang形成显示不规则,多向S2缝合线,给岩石pseudonodular外观(stylobreccia)。 Note that S2 is associated with F7 fractures and V7 vugs. (h) Plane light optical photomicrograph showing stylobreccias and their association with F7 fractures. Dolomite cement (Dc1) precipitated along S2 stylolites. F7a fractures filled with calcite cement (Cc7a). (i) Plane light optical photomicrograph showing F7b fractures and S2 tectonic stylolites containing blocky calcite (Cc7b) and dolomite cement (Dc1). Notice that pores around Dc1 crystals are filled with bitumen. (j) Plane light optical photomicrograph showing bedding-oblique stylolitic and sheared F7c fractures containing insoluble material, bitumen, and calcite cement (Cc7b). (k) Plane light optical photomicrograph showing an F7a fracture filled with calcite cement (Cc7a) forming synkinematic bridges and V7 vugs filled with blocky cement (Cc7b).</p>
<fig id="fig7a">
<label>(一)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.007a"></graphic>
</fig>
<fig id="fig7b">
<label>(b)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.007b"></graphic>
</fig>
<fig id="fig7c">
<label>(c)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.007c"></graphic>
</fig>
<fig id="fig7d">
<label>(d)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.007d"></graphic>
</fig>
<fig id="fig7e">
<label>(e)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.007e"></graphic>
</fig>
<fig id="fig7f">
<label>(f)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.007f"></graphic>
</fig>
<fig id="fig7g">
<label>(g)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.007g"></graphic>
</fig>
<fig id="fig7h">
<label>(h)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.007h"></graphic>
</fig>
<fig id="fig7i">
<label>(我)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.007i"></graphic>
</fig>
<fig id="fig7j">
<label>(j)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.007j"></graphic>
</fig>
<fig id="fig7k">
<label>(k)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.007k"></graphic>
</fig>
</fig-group>
<p>F6骨折bed-perpendicular, bed-oblique和/或顺层calcite-filled骨折与不规则的墙和1毫米和3厘米(图之间的光阑<gydF4y2Baxref rid="fig7e" ref-type="fig">
7 (e)</gydF4y2Baxref>)。块状方解石水泥(Cc6) F6骨折范围在200和600之间<gydF4y2Baitalic>
μ</gydF4y2Baitalic>m大小(图<gydF4y2Baxref rid="fig7f" ref-type="fig">
7 (f)</gydF4y2Baxref>nonluminescent),是暗红色,出现unzoned SEM-CL之下。</gydF4y2Bap>
<p>F7骨折形态存在。这组包括bed-perpendicular和bed-oblique calcite-filled骨折介于50<gydF4y2Baitalic>
μ</gydF4y2Baitalic>m和2毫米孔径(F7a数字<gydF4y2Baxref ref-type="fig" rid="fig7g">
7 (g)</gydF4y2Baxref>和<gydF4y2Baxref ref-type="fig" rid="fig7h">
7 (h)</gydF4y2Baxref>),张力的伤口(F7b图<gydF4y2Baxref ref-type="fig" rid="fig7i">
7(我)</gydF4y2Baxref>面向一个角度)与缝合线,床上用品(S2,见下文),和bedding-oblique bedding-perpendicular柱状和剪切骨折(F7c图<gydF4y2Baxref ref-type="fig" rid="fig7j">
7 (j)</gydF4y2Baxref>)。F7a骨折充满了方解石胶结物形成桥梁跨断裂的墙壁Cc7a图<gydF4y2Baxref ref-type="fig" rid="fig7h">
7 (h)</gydF4y2Baxref>。桥梁断裂wall-parallel轨迹证明的流体包裹体(见下文)表明crack-seal胶结机制在骨折开放(synkinematic水泥;讨论了着陆器和Laubach [<gydF4y2Baxref ref-type="bibr" rid="B72">
72年</gydF4y2Baxref>]和Ukar Laubach [<gydF4y2Baxref ref-type="bibr" rid="B73">
73年</gydF4y2Baxref>])。桥梁不溶解的残余方解石但表明方解石积累取决于热暴露和更新的断裂面积在重复骨折开放(<gydF4y2Baxref ref-type="bibr" rid="B72">
72年</gydF4y2Baxref>]。F7a骨折可能保留残余孔隙度25%。紧张的伤口(F7b)倒~ 1厘米远离S2缝合线和近似平行的缝合线的牙齿(图<gydF4y2Baxref ref-type="fig" rid="fig7i">
7(我)</gydF4y2Baxref>)。F7b骨折水泥(Cc7b)充满了块状方解石和白云石水泥(Dc1)(图<gydF4y2Baxref ref-type="fig" rid="fig7i">
7(我)</gydF4y2Baxref>)。Cc7b范围50之间<gydF4y2Baitalic>
μ</gydF4y2Baitalic>米和1毫米大小和出现unzoned和光SEM-CL下发光。Dc1形式分离,半形的自形的,黑暗的发光晶体30<gydF4y2Baitalic>
μ</gydF4y2Baitalic>米直径。毛孔Dc1晶体是100左右<gydF4y2Baitalic>
μ</gydF4y2Baitalic>m大小(图<gydF4y2Baxref ref-type="fig" rid="fig7i">
7(我)</gydF4y2Baxref>)。F7c骨折含有不溶性剩余材料,沥青,Cc7b Dc1水泥(图<gydF4y2Baxref ref-type="fig" rid="fig7j">
7 (j)</gydF4y2Baxref>)。</gydF4y2Bap>
</sec>
<sec id="sec4.1.5">
<title>4.1.5。缝合线</gydF4y2Batitle>
<p>顺层缝合岩面(S1a)和解决方案(印地)无处不在的和丰富的形成和核研究。S1a缝合线主要发生在内碎屑泥粒灰岩和粒状灰岩鹰,Yijianfang,降低Lianglitage阵型。S1a包含intergrown伊利石/绿泥石、石英、磷酸盐,黄铁矿,高岭石和沥青(图<gydF4y2Baxref rid="fig8a" ref-type="fig">
8(一个)</gydF4y2Baxref>)。印地解决煤层有类似的矿物学的细粒度的碎屑沉积物包括多达20%的伊利石、intergrown伊利石、绿泥石、石英(图<gydF4y2Baxref rid="fig8b" ref-type="fig">
8 (b)</gydF4y2Baxref>)。印地存在于mud-dominated岩相如生物碎屑wackestones和疗效泥wackestones Tumuxiuke和Lianglitage上部地层。S1是减少F1骨折,但有些S1横切F3, F4骨折表明S1形成持续的时间。</gydF4y2Bap>
<fig-group id="fig8">
<label>图8</lgydF4y2Baabel>
<p>(a, b)的手标本Yijianfang形成显示S1a,印地和S2缝合线和V3和V4溶解岩穴。(c)平面光的光学显微照片显示V3两旁Cc3a方解石水泥和沥青。(d)平面光的光学显微照片显示一个装满块状Cc6 V6晶簇。(e, f)手标本和(g)平面光Yijianfang形成的光学显微照片显示F3a之间的关联,S1a,黑暗的斑点。(h)平面光的光学显微照片显示V3岩穴发生在一个黑暗的斑点。在斑点面料Bitumen-infilled岩穴和颗粒间的孔隙度。(我)平面光光学显微照片显示黄铁矿矿化和二次解散的F4a裂缝扩大。(j)全色SEM-CL photomosaic显示腐蚀Cc4和高岭石的沉淀溶解的空洞。</gydF4y2Bap>
<fig id="fig8a">
<label>(一)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.008a"></graphic>
</fig>
<fig id="fig8b">
<label>(b)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.008b"></graphic>
</fig>
<fig id="fig8c">
<label>(c)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.008c"></graphic>
</fig>
<fig id="fig8d">
<label>(d)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.008d"></graphic>
</fig>
<fig id="fig8e">
<label>(e)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.008e"></graphic>
</fig>
<fig id="fig8f">
<label>(f)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.008f"></graphic>
</fig>
<fig id="fig8g">
<label>(g)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.008g"></graphic>
</fig>
<fig id="fig8h">
<label>(h)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.008h"></graphic>
</fig>
<fig id="fig8i">
<label>(我)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.008i"></graphic>
</fig>
<fig id="fig8j">
<label>(j)</lgydF4y2Baabel>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.008j"></graphic>
</fig>
</fig-group>
<p>Bed-perpendicular, bed-oblique缝合线(S2)本地丰富,最好的发达J, L, M, N, O和P核(图<gydF4y2Baxref ref-type="fig" rid="fig3b">
3 (b)</gydF4y2Baxref>)。面向随机S2给岩石pseudonodular外观描述为stylobreccia斯图尔特和汉考克(<gydF4y2Baxref ref-type="bibr" rid="B74">
74年</gydF4y2Baxref>)(图<gydF4y2Baxref ref-type="fig" rid="fig7g">
7 (g)</gydF4y2Baxref>和<gydF4y2Baxref ref-type="fig" rid="fig8a">
8(一个)</gydF4y2Baxref>)。S2水泥(Dc1)包含白云石,方解石水泥(Cc7b),不溶性材料,沥青(数字<gydF4y2Baxref ref-type="fig" rid="fig7i">
7(我)</gydF4y2Baxref>和<gydF4y2Baxref ref-type="fig" rid="fig7j">
7 (j)</gydF4y2Baxref>)。S2缝合线与F7骨折和横切所有先前的成岩特征(数字<gydF4y2Baxref ref-type="fig" rid="fig7g">
7 (g)</gydF4y2Baxref>和<gydF4y2Baxref ref-type="fig" rid="fig7k">
7 (k)</gydF4y2Baxref>)。</gydF4y2Bap>
</sec>
<sec id="sec4.1.6">
<title>4.1.6。蛀牙和岩穴</gydF4y2Batitle>
<p>孔隙比的平均晶粒尺寸(~ 20<gydF4y2Baitalic>
μ</gydF4y2Baitalic>米)在主机的岩石地层丰富。岩穴通常0.5至2毫米直径,虽然有些超过1厘米(图<gydF4y2Baxref ref-type="fig" rid="fig8a">
8(一个)</gydF4y2Baxref>),有不规则的边缘支持解散的形成机制。伴随着很多岩穴或终止在骨折,表明颞骨折和岩穴(图和基因之间的关系<gydF4y2Baxref ref-type="fig" rid="fig8a">
8(一个)</gydF4y2Baxref>)。横切不同类型的岩穴之间的关系不能成立,但骨折之间的关系的基础上,岩穴和相似的矿物填充,我们描述五代的岩穴形成同步F2-F7骨折。</gydF4y2Bap>
<p>虽然结构证据表明斑点面料未公开空洞的岩溶角砾岩等中发现Lianglitage形成斑点面料Yijianfang形成最早的溶解特性。我们指定这些第一代的岩穴(V1)。V2岩穴套印斑点面料和与块状填充,nonluminescent明亮的橙色发光方解石(Cc2;图<gydF4y2Baxref ref-type="fig" rid="fig6e">
6 (e)</gydF4y2Baxref>),而V3岩穴部分填充与刃的块状rim水泥(Cc3a)和沥青(数字<gydF4y2Baxref ref-type="fig" rid="fig8b">
8 (b)</gydF4y2Baxref>和<gydF4y2Baxref ref-type="fig" rid="fig8c">
8 (c)</gydF4y2Baxref>)和V4岩穴包含红色发光方解石(Cc4;图<gydF4y2Baxref ref-type="fig" rid="fig8a">
8(一个)</gydF4y2Baxref>)。没有V5岩穴中确定核心。V6和V7岩穴与粗块状方解石填充水泥(分别Cc6和Cc7b)(数据<gydF4y2Baxref ref-type="fig" rid="fig7k">
7 (k)</gydF4y2Baxref>和<gydF4y2Baxref ref-type="fig" rid="fig8d">
8 (d)</gydF4y2Baxref>)。V3 Yijianfang最丰富的类型的晶簇的形成和也出现在鹰山和Tumuxiuke地层,在岩溶Lianglitage形成的地平线。V3中ⅰ的核心,与斑点的位置面料在研究区北部(图<gydF4y2Baxref ref-type="fig" rid="fig3b">
3 (b)</gydF4y2Baxref>)。事实上,F3, V3、S1和斑点面料表现出密切的关系(数据<gydF4y2Baxref ref-type="fig" rid="fig8e">
8 (e)</gydF4y2Baxref>和<gydF4y2Baxref ref-type="fig" rid="fig8f">
8 (f)</gydF4y2Baxref>);在F3和/或S1遇到黑暗的斑点,岩石孔隙度(二级)增加给假角砾岩的方面被傅(<gydF4y2Baxref ref-type="bibr" rid="B35">
35</gydF4y2Baxref>]。在某些情况下,这二次溶解影响周围的地区立即斑点织物(图<gydF4y2Baxref ref-type="fig" rid="fig8g">
8 (g)</gydF4y2Baxref>)。孔隙空间内斑点面料随后填充与沥青给这些地区深色(图特征<gydF4y2Baxref ref-type="fig" rid="fig8h">
8 (h)</gydF4y2Baxref>)。</gydF4y2Bap>
<p>Cc3b Cc4沉淀在骨折显示溶解腐蚀(数字<gydF4y2Baxref ref-type="fig" rid="fig8b">
8 (b)</gydF4y2Baxref>和<gydF4y2Baxref ref-type="fig" rid="fig8i">
8(我)</gydF4y2Baxref>)提供的证据dissolution-enhanced骨折。腐蚀Cc4方解石通常是与金属硫化物(黄铁矿矿化)和高岭石(数字<gydF4y2Baxref ref-type="fig" rid="fig8i">
8(我)</gydF4y2Baxref>和<gydF4y2Baxref ref-type="fig" rid="fig8j">
8 (j)</gydF4y2Baxref>)。这个解散事件导致高达15%的形成次生孔隙度。</gydF4y2Bap>
</sec>
</sec>
<sec id="sec4.2">
<title>4.2。地球化学</gydF4y2Batitle>
<p>稳定同位素和流体包裹体进行了分析以揭示液体的来源,导致骨折的降水,vug-filling水泥。地球化学分析表进行了总结<gydF4y2Baxref ref-type="table" rid="tab2">
2</gydF4y2Baxref>和补充材料<gydF4y2Baxref ref-type="supplementary-material" rid="supplementary-material-1">
我</gydF4y2Baxref>,<gydF4y2Baxref ref-type="supplementary-material" rid="supplementary-material-1">
二世</gydF4y2Baxref>,<gydF4y2Baxref ref-type="supplementary-material" rid="supplementary-material-1">
三世</gydF4y2Baxref>。</gydF4y2Bap>
<table-wrap id="tab2">
<label>表2</lgydF4y2Baabel>
<p>总结的主要成岩特征和地球化学和microthermometric特性水泥所示顺序(共生序列)。KB:矩阵岩溶角砾岩;F:骨折;V:解散晶簇;S:缝合线;答:方解石胶结物;Cs:方解石沉积;Dc:白云石水泥。</gydF4y2Bap>
<table>
<thead>
<tr>
<th align="left">功能</gydF4y2Bath>
<th align="center">水泥</gydF4y2Bath>
<th align="center">
<italic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O (VPDB)</gydF4y2Bath>
<th align="center">
<italic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C (VPDB)</gydF4y2Bath>
<th align="center"><sup>87年</gydF4y2Basup>Sr /<gydF4y2Basup>86年</gydF4y2Basup>老</gydF4y2Bath>
<th align="center">Th (<gydF4y2Basup>o</gydF4y2Basup>C)</gydF4y2Bath>
<th align="center">盐度(wt. % eq。氯化钠)</gydF4y2Bath>
<th align="center">石油包裹体</gydF4y2Bath>
<th align="center">T油(<gydF4y2Basup>o</gydF4y2Basup>C)</gydF4y2Bath>
</tr>
</thead>
<tbody>
<tr>
<td align="left" rowspan="4">母岩</gydF4y2Batd>
<td align="center" rowspan="4">−</gydF4y2Batd>
<td align="center">-7.4到-5.5</gydF4y2Batd>
<td align="center">-0.1到1.1</gydF4y2Batd>
<td align="center">0.7088</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">没有</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center">-7.7到-4.7</gydF4y2Batd>
<td align="center">-0.3到1.6</gydF4y2Batd>
<td align="center">0.7088到0.7089</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">没有</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center">-6.7到-5.9</gydF4y2Batd>
<td align="center">-0.6到1.7</gydF4y2Batd>
<td align="center">0.7089到0.7090</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">没有</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center">-8.7到-4.3</gydF4y2Batd>
<td align="center">-0.6到3.2</gydF4y2Batd>
<td align="center">0.70856</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">没有</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="9">
<hr></td>
</tr>
<tr>
<td align="left" rowspan="3">母岩胶结</gydF4y2Batd>
<td align="center">Cc0a</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">没有</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center">Cc0b</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">74年到150年</gydF4y2Batd>
<td align="center">1.4到7.7</gydF4y2Batd>
<td align="center">没有</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center">Cc0c</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">75年到131年</gydF4y2Batd>
<td align="center">1.6到5.6</gydF4y2Batd>
<td align="center">没有</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="9">
<hr></td>
</tr>
<tr>
<td align="left" rowspan="2">黑色的斑点</gydF4y2Batd>
<td align="center">Cs0a</gydF4y2Batd>
<td align="center">-9.1到-6.3</gydF4y2Batd>
<td align="center">-0.5到1.1</gydF4y2Batd>
<td align="center">0.7091</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">没有</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center">Cs0b</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">没有</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="9">
<hr></td>
</tr>
<tr>
<td align="left" rowspan="2">F1</gydF4y2Batd>
<td align="center">Cc1</gydF4y2Batd>
<td align="center">-7.8到-3.6</gydF4y2Batd>
<td align="center">0.3到2.1</gydF4y2Batd>
<td align="center">0.7087</gydF4y2Batd>
<td align="center">76.9到113.9</gydF4y2Batd>
<td align="center">1.9到2.7</gydF4y2Batd>
<td align="center">没有</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center">Cs1</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">没有</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="9">
<hr></td>
</tr>
<tr>
<td align="left">岩溶角砾岩</gydF4y2Batd>
<td align="center">KB</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">0.7099</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">没有</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="9">
<hr></td>
</tr>
<tr>
<td align="left">V2</gydF4y2Batd>
<td align="center" rowspan="3">Cc2</gydF4y2Batd>
<td align="center" rowspan="3">-9.1到-4.5</gydF4y2Batd>
<td align="center" rowspan="3">-3.8到2.2</gydF4y2Batd>
<td align="center" rowspan="3">−</gydF4y2Batd>
<td align="center" rowspan="3">74年到135年</gydF4y2Batd>
<td align="center" rowspan="3">2.4到5.7</gydF4y2Batd>
<td align="center" rowspan="3">没有</gydF4y2Batd>
<td align="center" rowspan="3">−</gydF4y2Batd>
</tr>
<tr>
<td align="left">F2a</gydF4y2Batd>
</tr>
<tr>
<td align="left">F2b</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="9">
<hr></td>
</tr>
<tr>
<td align="left">S1a &印地</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="9">
<hr></td>
</tr>
<tr>
<td align="left">F3a</gydF4y2Batd>
<td align="center" rowspan="2">Cc3a</gydF4y2Batd>
<td align="center" rowspan="2">-11.7到-7.1</gydF4y2Batd>
<td align="center" rowspan="2">-0.2到2.8</gydF4y2Batd>
<td align="center" rowspan="2">0.7085到0.7088</gydF4y2Batd>
<td align="center" rowspan="2">60到165</gydF4y2Batd>
<td align="center" rowspan="2">0.4到12.3</gydF4y2Batd>
<td align="center" rowspan="2">黄色的蓝色</gydF4y2Batd>
<td align="center" rowspan="2">60到75</gydF4y2Batd>
</tr>
<tr>
<td align="left">F3b</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="9">
<hr></td>
</tr>
<tr>
<td align="left">V3</gydF4y2Batd>
<td align="center">Cc3b</gydF4y2Batd>
<td align="center">-12.8到-9.3</gydF4y2Batd>
<td align="center">1到2</gydF4y2Batd>
<td align="center">0.7085</gydF4y2Batd>
<td align="center">50到100</gydF4y2Batd>
<td align="center">7.7到14.1</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="9">
<hr></td>
</tr>
<tr>
<td align="left">F4a</gydF4y2Batd>
<td align="center" rowspan="3">Cc4</gydF4y2Batd>
<td align="center" rowspan="3">-15.8到-13.7</gydF4y2Batd>
<td align="center" rowspan="3">-0.4到1.7</gydF4y2Batd>
<td align="center" rowspan="3">0.7094到0.7102</gydF4y2Batd>
<td align="center" rowspan="3">80年到96年</gydF4y2Batd>
<td align="center" rowspan="3">13.5</gydF4y2Batd>
<td align="center" rowspan="3">明亮的蓝色,蓝绿色</gydF4y2Batd>
<td align="center" rowspan="3">−</gydF4y2Batd>
</tr>
<tr>
<td align="left">F4b</gydF4y2Batd>
</tr>
<tr>
<td align="left">V4</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="9">
<hr></td>
</tr>
<tr>
<td align="left" rowspan="4">F5</gydF4y2Batd>
<td align="center">萤石</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">79年到112年</gydF4y2Batd>
<td align="center">9.6到10.5</gydF4y2Batd>
<td align="center">黄绿色绿色</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center">重晶石</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">117年到144年</gydF4y2Batd>
<td align="center">11.1 - 19</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center">Cc5</gydF4y2Batd>
<td align="center">-13.7到-9.7</gydF4y2Batd>
<td align="center">-2.4到-2.2</gydF4y2Batd>
<td align="center">0.7090</gydF4y2Batd>
<td align="center">61 - 97.8</gydF4y2Batd>
<td align="center">5.7到14.7</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center">再结晶母岩</gydF4y2Batd>
<td align="center">-11.1到-6.4</gydF4y2Batd>
<td align="center">-1.8到-0.1</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="9">
<hr></td>
</tr>
<tr>
<td align="left">F6</gydF4y2Batd>
<td align="center" rowspan="2">Cc6</gydF4y2Batd>
<td align="center" rowspan="2">-15.4到-8.5</gydF4y2Batd>
<td align="center" rowspan="2">-4.8到-0.2</gydF4y2Batd>
<td align="center" rowspan="2">0.7093到0.7094</gydF4y2Batd>
<td align="center" rowspan="2">95年到123年</gydF4y2Batd>
<td align="center" rowspan="2">4.7到10.5</gydF4y2Batd>
<td align="center" rowspan="2">−</gydF4y2Batd>
<td align="center" rowspan="2">−</gydF4y2Batd>
</tr>
<tr>
<td align="left">V6</gydF4y2Batd>
</tr>
<tr>
<td align="center" colspan="9">
<hr></td>
</tr>
<tr>
<td align="left">F7a</gydF4y2Batd>
<td align="center">Cc7a</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">无聊的蓝色</gydF4y2Batd>
<td align="center">44到58</gydF4y2Batd>
</tr>
<tr>
<td align="left">F7b</gydF4y2Batd>
<td align="center" rowspan="2">Cc7b</gydF4y2Batd>
<td align="center" rowspan="2">-18.3</gydF4y2Batd>
<td align="center" rowspan="2">-1.1</gydF4y2Batd>
<td align="center" rowspan="2">−</gydF4y2Batd>
<td align="center" rowspan="2">−</gydF4y2Batd>
<td align="center" rowspan="2">−</gydF4y2Batd>
<td align="center" rowspan="2">浅蓝色的</gydF4y2Batd>
<td align="center" rowspan="2">−</gydF4y2Batd>
</tr>
<tr>
<td align="left">V7</gydF4y2Batd>
</tr>
<tr>
<td align="left">F7c & S2</gydF4y2Batd>
<td align="center">Dc1</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
<td align="center">−</gydF4y2Batd>
</tr>
</tbody>
</table>
</table-wrap>
<sec id="sec4.2.1">
<title>4.2.1。准备碳和氧同位素</gydF4y2Batitle>
<p>鹰和Yijianfang形成岩石了<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O值从-7.7到-4.7‰VPDB和<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C值从-0.1 + 1.6‰VPDB(图<gydF4y2Baxref rid="fig9" ref-type="fig">
9</gydF4y2Baxref>)。<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O Tumuxiuke形成的碳酸盐范围从-6.7到-5.9‰VPDB和<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M14">
<mml:msup>
<mml:mrow>
<mml:mi>
δ</米米l:mi>
</mml:mrow>
<mml:mrow>
<mml:mn>
13</米米l:mn>
</mml:mrow>
</mml:msup>
<mml:mtext>
C</米米l:mtext>
</mml:math>
</inline-formula>从-0.6 + 1.7‰VPDB,而<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O Lianglitage形成的碳酸盐范围从-8.7到-4.3‰VPDB和<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C从-0.6 + 3.2‰VPDB不等。红色碎屑在Lianglitage岩溶角砾岩<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>从-7.3到-6.4‰VPDB和阿<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C从+ 1.2 + 1.7‰VPDB(图<gydF4y2Baxref rid="fig9" ref-type="fig">
9</gydF4y2Baxref>)。</gydF4y2Bap>
<fig id="fig9">
<label>图9</lgydF4y2Baabel>
<p>
<italic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O -<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C和<gydF4y2Basup>87年</gydF4y2Basup>Sr /<gydF4y2Basup>86年</gydF4y2Basup>Sr -<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O交会图安排的形成。浅灰色多边形显示<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O -<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C和<gydF4y2Basup>87年</gydF4y2Basup>Sr /<gydF4y2Basup>86年</gydF4y2Basup>老的中奥陶世和上奥陶系海相碳酸盐从盾牌等。<gydF4y2Baxref ref-type="bibr" rid="B76">
76年</gydF4y2Baxref>]。人力资源:母岩;KB: red-clast岩溶角砾岩;RHR:再结晶母岩;答:方解石胶结物;Cs:方解石沉积;Dc:白云石水泥。</gydF4y2Bap>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.009"></graphic>
</fig>
<p>Cs0斑点面料的鹰,Yijianfang, Tumuxiuke形成<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O值耗尽略高于周围的母岩。<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>从9到-6.3‰VPDB O值,而<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C值是-0.5 + 0.8‰VPDB(图<gydF4y2Baxref ref-type="fig" rid="fig9">
9</gydF4y2Baxref>)。Cc1 Yijianfang和Tumuxiuke形成了<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>-7.8和-3.6‰VPDB与O值<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C从-0.3 + 2.1‰VPDB。逐渐减少的值<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>Cc2 O记录,介于-9.1和-4.8‰VPDB之间<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O和-0.5,+ 3.8‰VPDB之间<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>c . Cc3已经<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O值从-11.7到-7.1‰VPDB和<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C值从-0.2 + 2.8‰VPDB。Cc3a沉淀在岩穴内Lianglitage形成显示<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>-11.3和-8.6‰VPDB与O值<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C + 1.3 + 2.8‰VPDB之间,而Cc3b显示<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>从-12.8到-9.3‰VPDB和阿<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>从+ 1到+ 2‰VPDB C。Cc4 Yijianfang和Tumuxiuke形成<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O和-18.3和-13.0‰VPDB之间<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C从-1.1 + 1.7‰VPDB。Cc5 Cc6,只有出现在鹰山和Yijianfang岩层中,重<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O值和枯竭<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>比之前的成岩胶结物C值,<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>从-11.1到-6.4‰VPDB和O值<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C值从-1.8到-0.1‰VPDB Cc5,和<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>从-15.4到-8.5‰VPDB和O值<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C值从-2.4到-0.2‰VPDB Cc6。Cc7b Yijianfang形成的18.3‰VPDB的价值观<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O和-1.1‰VPDB<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C(图<gydF4y2Baxref ref-type="fig" rid="fig9">
9</gydF4y2Baxref>)。</gydF4y2Bap>
<p>克雷格的同位素平衡温度方程(<gydF4y2Baxref ref-type="bibr" rid="B75">
75年</gydF4y2Baxref>)可以应用于计算近似水泥温度降水。我们使用最稳定的同位素值的海洋流体从主机获得岩石和同位素值报告中奥陶世碳酸盐(<gydF4y2Baxref ref-type="bibr" rid="B76">
76年</gydF4y2Baxref>)(图<gydF4y2Baxref rid="fig9" ref-type="fig">
9</gydF4y2Baxref>)。降水寄主岩石中的Cc0推断是发生在~ 25°C,而Cc1沉淀在< 20°C, Cc2 ~ 30°C, Cc3在< < 45°C, Cc4 80°C。外来矿物质的Cc5 F5骨折的存在表明,系统是开放的,<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O<gydF4y2Basub>SMOW</gydF4y2Basub>父母的流体可能有不同的成分比奥陶系假设值海水呈现这方法不可靠和随后的水泥。</gydF4y2Bap>
</sec>
<sec id="sec4.2.2">
<title>4.2.2。锶同位素</gydF4y2Batitle>
<p>的<gydF4y2Basup>87年</gydF4y2Basup>Sr /<gydF4y2Basup>86年</gydF4y2Basup>老比鹰形成主机的岩石是0.7088,而它的范围从0.7087到0.7088的Yijianfang形成,Tumuxiuke形成0.7089到0.7090,和0.7085 Lianglitage形成。在Lianglitage岩溶角砾岩形成的矩阵所示<gydF4y2Basup>87年</gydF4y2Basup>Sr /<gydF4y2Basup>86年</gydF4y2Basup>老的0.7099,远高于母岩(图<gydF4y2Baxref rid="fig9" ref-type="fig">
9</gydF4y2Baxref>)。</gydF4y2Bap>
<p>Cs0斑点面料(Yijianfang形成)显示值为0.7091,和Cc1 (Tumuxiuke形成)显示了一个比率为0.7087。同位素值Cc3a (Yijianfang和Lianglitage地层)在0.7085和0.7088之间变化,这是Cc3b 0.7086。Cc4显示值从0.7094到0.7102在Yijianfang Tumuxiuke地层形成和0.7093到0.7097。<gydF4y2Basup>87年</gydF4y2Basup>Sr /<gydF4y2Basup>86年</gydF4y2Basup>Sr值Cc5和Cc6 (Yijianfang形成)0.7090为Cc6 Cc5和范围在0.7093和0.7094之间(图<gydF4y2Baxref ref-type="fig" rid="fig9">
9</gydF4y2Baxref>)。由于其体积小,我们没有为Cc7巩固老数据。</gydF4y2Bap>
</sec>
<sec id="sec4.2.3">
<title>4.2.3。流体包裹体显微温度学</gydF4y2Batitle>
<p>大多数裂缝和溶洞水泥形成困主水液和碳氢化合物(石油)夹杂物在流体包裹体组合(FIA)发生在不同世代的增长区域或拥挤不堪的集群在一个区域或主机谷物(图的核心<gydF4y2Baxref ref-type="fig" rid="fig10">
10</gydF4y2Baxref>)。几个fia的二次水和烃FIs也被观察到。水溶液包裹体的范围从5到25<gydF4y2Baitalic>
μ</gydF4y2Baitalic>米的直径,但大多数是< 10<gydF4y2Baitalic>
μ</gydF4y2Baitalic>m。fia包含单相液体包裹体只或两相液汽夹杂物。在一些情况下,我们观察到夹杂物也包含一个固相通常不透明的黑色或浅琥珀色,解释可能是固体碳氢化合物阶段(蜡或沥青)。固体出现只有零星几夹杂物在相同的组合,所以他们的比率(liquid-vapor-solid)阶段有所不同。相比例变化的夹杂物在这些fia解释表明,固体被困在夹杂物而不是偶然从流体沉淀的结果。均化温度的摘要(<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M15">
<mml:msub>
<mml:mrow>
<mml:mi>
T</米米l:mi>
</mml:mrow>
<mml:mrow>
<mml:mtext>
h</米米l:mtext>
</mml:mrow>
</mml:msub>
</mml:math>
</inline-formula>初级阶段)和盐度水夹杂物在各种水泥呈现在图<gydF4y2Baxref ref-type="fig" rid="fig11">
11</gydF4y2Baxref>和表<gydF4y2Baxref ref-type="table" rid="tab2">
2</gydF4y2Baxref>。</gydF4y2Bap>
<fig id="fig10">
<label>图10</lgydF4y2Baabel>
<p>典型的流体包裹体的显微照片。(a)拉伸夹杂物的例子:深蓝色箭头强调初级阶段水夹杂物不一致<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M16">
<mml:mi>
l</米米l:mi>
</mml:math>
</inline-formula>:<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M17">
<mml:mi>
V</米米l:mi>
</mml:math>
</inline-formula>比率和浅蓝色箭头强调初级单相水夹杂物。(b)浅蓝色箭头强调pseudosecondary单相水夹杂物被困在一个平面,终止在晶体边缘。(c)深蓝色箭头强调集群初级阶段与同质水溶液包裹体<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M18">
<mml:mi>
l</米米l:mi>
</mml:math>
</inline-formula>:<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M19">
<mml:mi>
V</米米l:mi>
</mml:math>
</inline-formula>比率。(d)深蓝色箭头强调主要水两相包裹体与同质<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M20">
<mml:mi>
l</米米l:mi>
</mml:math>
</inline-formula>:<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M21">
<mml:mi>
V</米米l:mi>
</mml:math>
</inline-formula>比率被困在一个增长区域。(e)深绿色箭头强调主要三相油(<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M22">
<mml:mi>
l</米米l:mi>
</mml:math>
</inline-formula>:<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M23">
<mml:mi>
V</米米l:mi>
</mml:math>
</inline-formula>:<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M24">
<mml:mi>
年代</米米l:mi>
</mml:math>
</inline-formula>)夹杂物被困在一个增长区域。固相是固体碳氢化合物。(f)蓝色油包裹体的荧光在紫外光照射下(e)。(g)深绿色箭头强调主要单相油包裹体被困在增长区域。亮绿色箭头凸显了中学阶段石油包裹体的踪迹。(h)蓝色(深绿色箭头)和沉闷的橙色(亮绿色箭头)油包裹体的荧光在紫外光照射下(g)。</gydF4y2Bap>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.0010"></graphic>
</fig>
<fig id="fig11">
<label>图11</lgydF4y2Baabel>
<p>盒子,须情节展示显微温度学两相水包体的结果为个人fia(最低捕获和盐度)按时间顺序安排的形成和成岩特征。</gydF4y2Bap>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.0011"></graphic>
</fig>
<p>总的来说,水流体包裹体显示广泛的<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M25">
<mml:msub>
<mml:mrow>
<mml:mi>
T</米米l:mi>
</mml:mrow>
<mml:mrow>
<mml:mtext>
h</米米l:mtext>
</mml:mrow>
</mml:msub>
</mml:math>
</inline-formula>从~ 50°C到165°C水泥,温度变化从~ 2°C在个人fia 40°C。冰融化的温度也显示大范围从1.1到11.1°C,对应于盐度0.4 19 wt %氯化钠等价物(<gydF4y2Baxref ref-type="bibr" rid="B77">
77年</gydF4y2Baxref>]。共晶(第一个冰融化)观察包含液体的温度大约在-50°C,表明水流体被困在夹杂物可以充分描述为H<gydF4y2Basub>2</gydF4y2Basub>O-NaCl-CaCl<gydF4y2Basub>2</gydF4y2Basub>——(±MgCl<gydF4y2Basub>2</gydF4y2Basub>”液体。融化的其他阶段在这个温度,如antarcticite [<gydF4y2Baxref ref-type="bibr" rid="B77">
77年</gydF4y2Baxref>),没有观察到由于小尺寸夹杂物。然而,我们观察到的一个示例包含流体包裹体的融化在freezing-heating运行两个固体阶段。第一个固体融化温度从-22.6°C到-21.2°C, hydrohalite解释,第二融化温度从-12.6°C到-4.8°C,解释是水冰。这两个阶段的融化使我们能够确定水溶液包含0到3.9 wt % CaCl<gydF4y2Basub>2</gydF4y2Basub>和7.7 - 15.7 wt %氯化钠<gydF4y2Baxref ref-type="bibr" rid="B77">
77年</gydF4y2Baxref>]。F5断裂分析显示一个明确的水泥与分区降水序列萤石形成第一,其次是重晶石和方解石(Cc5)。所有这些水泥困主要含水流体包裹体显示系统温度变化~ 80°C到110°C的萤石、重晶石从120 ~ 140°,~ 60到100°C在Cc5晚期方解石(图<gydF4y2Baxref ref-type="fig" rid="fig11">
11</gydF4y2Baxref>)。流体的盐度反映温度显示了一个类似的趋势,从9.6 wt % 10.5 wt %氯化钠等价物萤石,~ 19 wt %氯化钠等价物的重晶石,从5.7到14.7 wt %氯化钠等价物在Cc5(图<gydF4y2Baxref ref-type="fig" rid="fig11">
11</gydF4y2Baxref>)。</gydF4y2Bap>
<p>主要在Cc3石油夹杂物存在,Cc4,和萤石水泥在所有三个地层,但没有Cc0主机的岩石,月初Cc1骨折,Cc2晶簇水泥。我们没有主要石油Cc5包含数据和Cc6水泥。FIA的石油包裹体显示异构和明显均匀liquid-to-vapor比率在同一FIA在室温下。石油包裹体与齐次liquid-to-vapor fia比率显示<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M26">
<mml:msub>
<mml:mrow>
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T</米米l:mi>
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<mml:mtext>
h</米米l:mtext>
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</mml:math>
</inline-formula>从44到75°C(表<gydF4y2Baxref ref-type="table" rid="tab2">
2</gydF4y2Baxref>)。油包裹体的荧光颜色在紫外光范围从黄色绿色在Cc3方解石和F5萤石Yijianfang形成的水泥,和绿色明亮的蓝色在Cc3 Lianglitage水泥和Tumuxiuke形成以及后续Cc7 Yijianfang形成(图的水泥<gydF4y2Baxref ref-type="fig" rid="fig11">
11</gydF4y2Baxref>)。</gydF4y2Bap>
</sec>
</sec>
</sec>
<sec id="sec5">
<title>5。讨论</gydF4y2Batitle>
<p>的蛀牙形成的浅(表观遗传学)解散那些由于根深蒂固的(中期形成的)解散具有挑战性,因为根据定义,蛀牙本身不能取样。在蛀牙是足够小的情况下由核心取样(岩穴),孔隙保存它们的起源的迹象。在许多情况下,然而,岩穴和相关骨折研究碳酸盐包含水泥衬里和内填充,可用于获取信息的物理和化学条件在不同阶段的解散和影响这些岩石胶结。信息温度、压力、应力和流体成分在变形(<gydF4y2Baxref ref-type="bibr" rid="B40">
40</gydF4y2Baxref>- - - - - -<gydF4y2Baxref ref-type="bibr" rid="B44">
44</gydF4y2Baxref>是记录在水泥和流体包裹体被困其中。巩固了岩穴和dissolution-enhanced骨折中确定本研究减少后代的巩固了岩穴和骨折,表明水泥记录条件前和后解散。结构性成岩特征识别的序列在这项研究中,特别是水泥中沉淀,可以用来限制物理的发展,化学和机械条件导致Halahatang地区hydrocarbon-hosting蛀牙的形成。</gydF4y2Bap>
<p>虽然空和上奥陶系碳酸盐岩显示许多相似的结构成岩演化过程中,并不是所有的功能都出现在所有的形成。样本套件允许建立最完整Yijianfang形成共生序列,这是下面(图<gydF4y2Baxref ref-type="fig" rid="fig12">
12</gydF4y2Baxref>)。</gydF4y2Bap>
<fig id="fig12">
<label>图12</lgydF4y2Baabel>
<p>摘要在研究了奥陶系碳酸盐成岩序列。</gydF4y2Bap>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.0012"></graphic>
</fig>
<sec id="sec5.1">
<title>5.1。成岩环境</gydF4y2Batitle>
<sec id="sec5.1.1">
<title>5.1.1。0阶段:海洋成岩作用</gydF4y2Batitle>
<p>的<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O和<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C值主机的岩石是一致的同位素值推断的盾牌et al。<gydF4y2Baxref ref-type="bibr" rid="B76">
76年</gydF4y2Baxref>)和Veizer et al。<gydF4y2Baxref ref-type="bibr" rid="B78">
78年</gydF4y2Baxref>]因为中间上奥陶系海相碳酸盐(图<gydF4y2Baxref ref-type="fig" rid="fig9">
9</gydF4y2Baxref>)。因此,主岩水泥(Cc0)最有可能从海洋孔隙流体沉淀。然而,<gydF4y2Basup>87年</gydF4y2Basup>Sr /<gydF4y2Basup>86年</gydF4y2Basup>Sr Tumuxiuke和Lianglitage岩层的比率略高于预期值为上奥陶系海相碳酸盐,可能由于粘土矿物内容矩阵的泥岩和wackestones<gydF4y2Baxref ref-type="bibr" rid="B79">
79年</gydF4y2Baxref>]。低矿化度,类似的海水,Cc0主机的流体包裹体岩胶结物沉淀在海洋成岩领域(图的支持<gydF4y2Baxref ref-type="fig" rid="fig11">
11</gydF4y2Baxref>)。然而,<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M27">
<mml:msub>
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T</米米l:mi>
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h</米米l:mtext>
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</inline-formula>是最低捕获温度(<gydF4y2Baxref ref-type="bibr" rid="B80">
80年</gydF4y2Baxref>)——盐度一些夹杂物是高度可变的,远高于预期的浅海洋环境。此外,流体包裹体温度远高于那些计算氧同位素的基础内容。的高可变性<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M28">
<mml:msub>
<mml:mrow>
<mml:mi>
T</米米l:mi>
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h</米米l:mtext>
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</inline-formula>的推理和盐度支持高温度和盐度的流体包裹体的结果reequilibration埋葬的液体在进步的葬礼来更高的深度(<gydF4y2Baxref ref-type="bibr" rid="B81">
81年</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B82">
82年</gydF4y2Baxref>]。reequilibration可以调整夹杂物的组合来新的温度和压力条件下拉伸或改变夹杂物的体积或部分渗透新的液体,包含液体的混合。夹杂物的推断reequilibration表明必须采取谨慎如果温度与埋藏热史模型时间限制(例如,<gydF4y2Baxref ref-type="bibr" rid="B83">
83年</gydF4y2Baxref>])。</gydF4y2Bap>
<p>我们的研究表明,斑点面料既不穿透地表岩溶过程的结果也不深成岩特征,但随后通过中期形成的叠覆解散的洞穴。Channel-shaped斑点面料填充与分散的化石支持解释这些是calcite-filled洞穴特征的早期成岩作用(<gydF4y2Baxref ref-type="bibr" rid="B84">
84年</gydF4y2Baxref>]。水泥在斑点面料和主机的岩石有相似的地球化学特征表明毛孔形成由于小主岩的溶解。<gydF4y2Basup>87年</gydF4y2Basup>Sr /<gydF4y2Basup>86年</gydF4y2Basup>Sr比率高于主机可能是由于蚀变岩石的伊利石和高岭石晶间孔隙内Cs0 [<gydF4y2Baxref ref-type="bibr" rid="B64">
64年</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B85">
85年</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B86">
86年</gydF4y2Baxref>)(图<gydF4y2Baxref ref-type="fig" rid="fig9">
9</gydF4y2Baxref>)。我们的结果广泛兼容以前的解释斑驳面料被选择性的结果成岩蚀变和随后的渗透沥青(<gydF4y2Baxref ref-type="bibr" rid="B35">
35</gydF4y2Baxref>]。不规则的斑点织物墙及其分布可能反映了解散由含烃流体upwelled从潜在的烃源岩(<gydF4y2Baxref ref-type="bibr" rid="B22">
22</gydF4y2Baxref>]。</gydF4y2Bap>
</sec>
<sec id="sec5.1.2">
<title>5.1.2中。阶段1:海洋潜水成岩作用</gydF4y2Batitle>
<p>隆升过程,比如那些经历了加里东、海西地区造山运动,通常导致降低温度和压力,可能会伴随着大量的孔隙流体成分的变化由于陨石深层渗透液体从高架充电区域(<gydF4y2Baxref ref-type="bibr" rid="B87">
87年</gydF4y2Baxref>]。这种液体可以沿着骨折并导致溶解,形成solution-enhanced骨折与F1等不规则的墙壁。栅状方解石胶结物(Cc1)和内部沉积物(Cs1) F1断裂是phreatic-vadose水平内的降水特征(<gydF4y2Baxref ref-type="bibr" rid="B8">
8</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B41">
41</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B88">
88年</gydF4y2Baxref>]。然而,<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O和<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C同位素值表明降水从海洋流体<gydF4y2Baxref ref-type="bibr" rid="B40">
40</gydF4y2Baxref>]。迅速渗透水与孔隙水混合液体会显示低,但非零,盐度。低盐度流体包裹体Cc1水泥在上覆Tumuxiuke形成支持海洋降水,但高<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M29">
<mml:msub>
<mml:mrow>
<mml:mi>
T</米米l:mi>
</mml:mrow>
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h</米米l:mtext>
</mml:mrow>
</mml:msub>
</mml:math>
</inline-formula>建议reequilibration进步的葬礼期间(<gydF4y2Baxref ref-type="bibr" rid="B81">
81年</gydF4y2Baxref>]。使用地热梯度28°C /公里的他在中奥陶世隆起(<gydF4y2Baxref ref-type="bibr" rid="B89">
89年</gydF4y2Baxref>),计算温度< 20°C表明Cc1水泥表面沉淀很近,符合沉淀在中奥陶世<gydF4y2Baxref ref-type="bibr" rid="B90">
90年</gydF4y2Baxref>- - - - - -<gydF4y2Baxref ref-type="bibr" rid="B93">
93年</gydF4y2Baxref>)(图<gydF4y2Baxref ref-type="fig" rid="fig13">
13</gydF4y2Baxref>)。</gydF4y2Bap>
<fig id="fig13">
<label>图13</lgydF4y2Baabel>
<p>估计时间和深度发生的成岩阶段所描述的文本上下文中的埋藏史模型计算出井之一我们的研究区域(埋藏史曲线从朱et al。<gydF4y2Baxref ref-type="bibr" rid="B61">
61年</gydF4y2Baxref>];HA601-4)。</gydF4y2Bap>
<graphic xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.fig.0013"></graphic>
</fig>
</sec>
<sec id="sec5.1.3">
<title>5.1.3。阶段2:海洋浅埋藏成岩作用</gydF4y2Batitle>
<p>这一阶段被埋葬的发病特点,形成compaction-related骨折和缝合线(S1)以及解散。Cc2水泥在F2骨折和V2岩穴<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C值与寄主岩石相似,而<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O值这些水泥稍微减少(图<gydF4y2Baxref ref-type="fig" rid="fig9">
9</gydF4y2Baxref>)。这个损耗表明Cc2沉淀从海洋流体在岩石的进步的葬礼<gydF4y2Baxref ref-type="bibr" rid="B94">
94年</gydF4y2Baxref>]。估计30°C的温度指示降水Cc2的~ 220米深度,在浅埋藏成岩环境中(<gydF4y2Baxref ref-type="bibr" rid="B95">
95年</gydF4y2Baxref>]。流体包裹体在Cc2 Yijianfang和上覆地层显示一个范围,但是一般温度升高,表明,同样,reequilibration夹杂物的更高的埋藏深度。的<gydF4y2Basup>87年</gydF4y2Basup>Sr /<gydF4y2Basup>86年</gydF4y2Basup>老比的水泥类似于主机的岩石(图<gydF4y2Baxref ref-type="fig" rid="fig9">
9</gydF4y2Baxref>),表明高rock-fluid相互作用[<gydF4y2Baxref ref-type="bibr" rid="B96">
96年</gydF4y2Baxref>]。比较有代表性的埋藏史曲线研究表明,中奥陶世地层区域达到这种深度在奥陶纪末(图<gydF4y2Baxref ref-type="fig" rid="fig13">
13</gydF4y2Baxref>)。缺乏主要的石油包裹体Cc2或更早的水泥赞同这一时机,之前的第一阶段生烃在志留纪(<gydF4y2Baxref ref-type="bibr" rid="B1">
1</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B61">
61年</gydF4y2Baxref>]。类似的液体很可能导致第一阶段解散碳酸盐在这个阶段的持续造成腐蚀。</gydF4y2Bap>
</sec>
<sec id="sec5.1.4">
<title>5.1.4。阶段3:中间埋藏成岩作用</gydF4y2Batitle>
<p>这一阶段以F3断裂的形成和V3岩穴。空间关联F3、V3和斑点面料表明V3最有可能由dissolution-prone增大,多孔,diagenetically改变地区(斑点面料)。Cc3沉淀在F3断裂和V3岩穴显示耗尽<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O值相对于母岩指示埋葬和降水从低收入到介质温度形成水(图<gydF4y2Baxref ref-type="fig" rid="fig9">
9</gydF4y2Baxref>)。计算的温度< 45°C表明Cc3水泥沉淀在~ 625米深度,在中间埋藏成岩环境中(<gydF4y2Baxref ref-type="bibr" rid="B17">
17</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B95">
95年</gydF4y2Baxref>),与上覆地层的高温流体包裹体(图<gydF4y2Baxref ref-type="fig" rid="fig11">
11</gydF4y2Baxref>)。的相似性<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C值Cc3和主机之间的岩石表明碳被寄主岩石缓冲(<gydF4y2Baxref ref-type="bibr" rid="B94">
94年</gydF4y2Baxref>]。的<gydF4y2Basup>87年</gydF4y2Basup>Sr /<gydF4y2Basup>86年</gydF4y2Basup>老比,类似于母岩,也表明石灰石盛行的流体和宿主之间的相互作用(图<gydF4y2Baxref ref-type="fig" rid="fig9">
9</gydF4y2Baxref>)。</gydF4y2Bap>
<p>Cc3a填充V3岩穴和F3骨折包含主要石油包裹体,表明石油系统中沉淀的时候这些水泥。石油沥青存在进一步支持3组骨折和岩穴。第一次石油积累在研究区,来自寒武纪烃源岩(<gydF4y2Baxref ref-type="bibr" rid="B90">
90年</gydF4y2Baxref>),日期末Caledonian-Early海西期(<gydF4y2Baxref ref-type="bibr" rid="B1">
1</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B61">
61年</gydF4y2Baxref>]。这个时机的石油生成和推断深度Cc3水泥兼容组3的形成和部分胶结特性在志留纪(见Ukar et al。<gydF4y2Baxref ref-type="bibr" rid="B93">
93年</gydF4y2Baxref>])。重质原油在该研究领域有丰富的H<gydF4y2Basub>2</gydF4y2Basub>年代,含硫量可能高达2%<gydF4y2Baxref ref-type="bibr" rid="B63">
63年</gydF4y2Baxref>]。水库的温度上升引起的葬礼将会引发硫化合物的热分解产生更多的H<gydF4y2Basub>2</gydF4y2Basub>年代(<gydF4y2Baxref ref-type="bibr" rid="B1">
1</gydF4y2Baxref>]。高硫油与水混合,可以创建H<gydF4y2Basub>2</gydF4y2Basub>所以<gydF4y2Basub>4</gydF4y2Basub>相似的过程中创建的卡尔斯巴德洞窟瓜达卢佩圣母山(美国德克萨斯州)[<gydF4y2Baxref ref-type="bibr" rid="B97">
97年</gydF4y2Baxref>]。液体,包括碳氢化合物和酸性流体与高硫油、流动F3断裂和S1a缝合线造成局部解体和岩穴的形成。母岩返工和解散穴居导致早期成岩斑点的形成面料生成1 - 3%的孔隙度在这些地区,允许渗透溶解液体和本地化的后续解散dissolution-prone斑点面料。一个F3和/或S1a遇到了一个黑暗的斑点,岩石孔隙度(二级)增加给假角砾岩的方面<gydF4y2Baxref ref-type="bibr" rid="B35">
35</gydF4y2Baxref>]。</gydF4y2Bap>
</sec>
<sec id="sec5.1.5">
<title>是5.1.5。阶段4 - 7:深埋藏成岩作用</gydF4y2Batitle>
<p>Cc4沉淀在F4骨折和V4岩穴显示更多的损耗<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O母岩相比。较低的值<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O表示进一步埋葬的岩石和循环高温地层水(图<gydF4y2Baxref ref-type="fig" rid="fig9">
9</gydF4y2Baxref>)。Cc2 Cc4跟随趋势的轻微的增加<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C和减少<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O表明rock-water交互在越来越高的温度下。计算的温度< 80°C表明Cc4沉淀在~ 2000米深度,在深埋藏成岩环境中(<gydF4y2Baxref ref-type="bibr" rid="B17">
17</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B95">
95年</gydF4y2Baxref>]。的相似性<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>Cc4和主机的岩石之间C值表明,碳是由主机碳酸盐缓冲(<gydF4y2Baxref ref-type="bibr" rid="B94">
94年</gydF4y2Baxref>]。然而,高<gydF4y2Basup>87年</gydF4y2Basup>Sr /<gydF4y2Basup>86年</gydF4y2Basup>Sr值这些存在方解石表明掺入放射性Sr源自古老的岩石如蒸发寒武纪地层(<gydF4y2Baxref ref-type="bibr" rid="B98">
98年</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B99">
99年</gydF4y2Baxref>),前寒武纪基底(<gydF4y2Baxref ref-type="bibr" rid="B100">
One hundred.</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B101">
101年</gydF4y2Baxref>),和/或改变长石组成的粘土和其他碎屑陆源矿物存在深层地层内(<gydF4y2Baxref ref-type="bibr" rid="B102">
102年</gydF4y2Baxref>]。</gydF4y2Bap>
<p>Cc5 Cc6显示更多的枯竭<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>13</gydF4y2Basup>C和/或重<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>啊,离开的一般趋势增加温度(图<gydF4y2Baxref ref-type="fig" rid="fig9">
9</gydF4y2Baxref>)和指向流体混合在一个水文开放系统(<gydF4y2Baxref ref-type="bibr" rid="B16">
16</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B40">
40</gydF4y2Baxref>]。非碳酸盐矿物的沉淀在F5(萤石、重晶石和天青石)支持流体化学和/或温度的变化。高温液体的渗透是由一般高温FI F5、F6水泥(图内<gydF4y2Baxref ref-type="fig" rid="fig11">
11</gydF4y2Baxref>)。经历的部分溶解等F4骨折可能是由于高温液体,可能从一个更深的来源。这是支持的并行计算和系统的温度和盐度的变化,显示增加然后减少的趋势,从早期的萤石晚期方解石胶结物在F5骨折。黄铁矿的氧化与F4和缝合线将伴随着降低pH值创建一个酸性环境,将解散(<gydF4y2Baxref ref-type="bibr" rid="B103">
103年</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B104">
104年</gydF4y2Baxref>]。腐蚀性液体可能也伴随着后续降水萤石(<gydF4y2Baxref ref-type="bibr" rid="B16">
16</gydF4y2Baxref>]。</gydF4y2Bap>
<p>一个<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M30">
<mml:mn>
400年</米米l:mn>
<mml:mo>
±</米米l:mo>
<mml:mn>
37</米米l:mn>
<mml:mtext>
</mml:mtext>
<mml:mtext>
马</米米l:mtext>
</mml:math>
</inline-formula>等时线年龄的F5断裂报道Ukar et al。<gydF4y2Baxref ref-type="bibr" rid="B93">
93年</gydF4y2Baxref>]表明形成和随后的矿物填充的泥盆纪,方解石沉淀与推断深度一致,达成的奥陶系地层(图<gydF4y2Baxref ref-type="fig" rid="fig13">
13</gydF4y2Baxref>)。<gydF4y2Basup>87年</gydF4y2Basup>Sr /<gydF4y2Basup>86年</gydF4y2Basup>Sr值沉淀的后续Cc6骨折符合中产二叠纪岩浆的同位素值(~ 295 - 263 Ma) (<gydF4y2Baxref ref-type="bibr" rid="B91">
91年</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B92">
92年</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B105">
105年</gydF4y2Baxref>]表明Cc6获得高锶同位素比值通过合并放射Sr来源于岩浆流体(<gydF4y2Baxref ref-type="bibr" rid="B64">
64年</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B79">
79年</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B84">
84年</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B86">
86年</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B106">
106年</gydF4y2Baxref>]。</gydF4y2Bap>
<p>方解石和白云石(Dc1)水泥(Cc7)矿化与F7骨折,V7岩穴,stylobreccias (S2,断层角砾岩)表示的存在Mg-rich液体在二叠纪后的系统活动。插入式变形记录下这些结构最有可能发生在白垩纪Jurassic-Early ([<gydF4y2Baxref ref-type="bibr" rid="B93">
93年</gydF4y2Baxref>])。</gydF4y2Bap>
<p>年轻Cc7水泥Yijianfang形成包含主要石油包裹体与API重力高值(沉闷的淡蓝色;°~ 40 - API重力)比年长Cc3和萤石水泥(黄色绿色;°~ - API重力)与系统中增加石油成熟度一致(图<gydF4y2Baxref rid="fig11" ref-type="fig">
11</gydF4y2Baxref>)。UV光油包裹体的荧光颜色Cc3和上覆Tumuxiuke Cc4水泥Lianglitage形成更成熟的浅蓝色(绿色)比等效特性Yijianfang内形成和类似于Cc7 Yijianfang内形成。这一趋势预计的相反变化的热成熟油的深度(<gydF4y2Baxref ref-type="bibr" rid="B107">
107年</gydF4y2Baxref>]。没有限制油的成分,可能的解释为紫外线荧光颜色的变化之间的油形成包括本地发生生物降解等因素,水洗涤,运移分馏([<gydF4y2Baxref ref-type="bibr" rid="B107">
107年</gydF4y2Baxref>)在一个潜在的弱互联流体系统整个clay-rich Tumuxiuke Cc3胶结时形成。</gydF4y2Bap>
</sec>
</sec>
<sec id="sec5.2">
<title>5.2。解散和流体通路</gydF4y2Batitle>
<p>在他隆起奥陶系顶部的地震解释说明了一个侵蚀地形和地震地貌模式相关的不整合,与众多蜿蜒的河流渠道和峡谷、河流山谷,灰岩坑,塔岩溶和山<gydF4y2Baxref ref-type="bibr" rid="B2">
2</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B108">
108年</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B109">
109年</gydF4y2Baxref>]。密集的喀斯特作用假设是相关长期海平面下降和地面上的曝光,恰逢一个大冰期结束时奥陶系(<gydF4y2Baxref ref-type="bibr" rid="B110">
110年</gydF4y2Baxref>]。</gydF4y2Bap>
<p>然而,Halahatang地区,我们唯一遇到类似岩溶角砾岩馅料是Lianglitage中形成的。本地化的淤泥石英、粘土和铁氧化物角砾区域内表明这些沉积物大多是运输到蛀牙在陆上暴露(表观遗传溶解)。已经广为记载类似的沉积物填充腔Lianglitage核的形成在其他研究领域<gydF4y2Baxref ref-type="bibr" rid="B27">
27</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B111">
111年</gydF4y2Baxref>]。此外,存在广泛的近地表古喀斯特是明显的地震模式,100年代的地形起伏的米类似现代桂林活跃岩溶地区的地形是可见的顶部上奥陶系碳酸盐。fracture-cavity网络相关下切河谷,祖先的结果河的顶部Lianglitage形成(<gydF4y2Baxref ref-type="bibr" rid="B112">
112年</gydF4y2Baxref>]。</gydF4y2Bap>
<p>岩溶角砾岩中缺席Yijianfang形成我们的研究区域。早期成岩特征斑点面料,但这些显示类似的同位素和岩性成分作为东道主摇滚表明他们形成原位由于轻微的返工和解散与穴居。原生孔隙度与近地表斑点织物解散是< 3%,类似于矩阵的1 - 3%。储层的孔隙度报告5 - 12% (<gydF4y2Baxref ref-type="bibr" rid="B113">
113年</gydF4y2Baxref>)必须因此造成的后续解散。结构和同位素记录的证据表明,大多数解散Yijianfang形成地层发生在中间和深成岩环境(中期形成的溶解)。虽然Lianglitage和Tumuxiuke中期形成的溶解,形成包含证据的一些结构性成岩特征识别Yijianfang形成上覆岩层(表中缺席<gydF4y2Baxref ref-type="table" rid="tab1">
1</gydF4y2Baxref>)。Lianglitage之间的这种差异在结构成岩作用和Yijianfang岩层表明水文盖层的存在孤立的紧凑Tumuxiuke形成的泥灰岩地层间<gydF4y2Baxref ref-type="bibr" rid="B25">
25</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B57">
57</gydF4y2Baxref>]。</gydF4y2Bap>
<p>然而,岩相、SEM-CL和同位素组成的晶簇,裂隙充填胶结物的结构确定成岩特征是相同的在Tumuxiuke形成显示下面的碳酸盐岩,超过这个限制地平线以某种方式连接,在协议与观测朱et al。<gydF4y2Baxref ref-type="bibr" rid="B114">
114年</gydF4y2Baxref>]。骨折之间的密切联系和溶解岩穴表明腐蚀性液体流淌在骨折,其中一些必须垂直扩展形成数十到数百米。成岩胶结物沉淀沿着缝合线表明这些也作为流动路径,而不是障碍。</gydF4y2Bap>
</sec>
<sec id="sec5.3">
<title>5.3。多个浅和深解散事件</gydF4y2Batitle>
<p>多个岩溶事件与地面的接触和浅深穿透地下水在古生代碳酸盐岩广泛的序列,和地下水可以穿透深度和导致解散(例如,<gydF4y2Baxref ref-type="bibr" rid="B115">
115年</gydF4y2Baxref>])。断层解散也被广泛接受(<gydF4y2Baxref ref-type="bibr" rid="B18">
18</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B20">
20.</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B116">
116年</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B117">
117年</gydF4y2Baxref>]。但是证据我们发现重复的解散和降水主要在大深度和不一定与接触表面或地下水的风险提出了一个问题的有用的“古喀斯特”这个词来形容两个(1)特性明确联系地表或近地表过程和(2)解散大断层由于腐蚀性液体穿透深度和骨折可能不确定或没有连接与喀斯特地形或地下水。我们认为的结构描述可能不是有效地归类为古喀斯特,由于流程操作在深度可能显著不同的特点和解散的时机,可能模式,与那些由很大的不同手段和其他近地表控制。例如,腐蚀性液体可能促进断层和断层孔隙度演化由于化学-机械交互(例如,<gydF4y2Baxref ref-type="bibr" rid="B118">
118年</gydF4y2Baxref>])。我们宁愿用描述性术语确定和分类溶解特性。</gydF4y2Bap>
<p>大规模解散在深埋藏深度(20%)一直在怀疑<gydF4y2Baxref ref-type="bibr" rid="B119">
119年</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B120">
120年</gydF4y2Baxref>]。Ehrenberg et al。<gydF4y2Baxref ref-type="bibr" rid="B119">
119年</gydF4y2Baxref>埃伦伯格]和[<gydF4y2Baxref ref-type="bibr" rid="B120">
120年</gydF4y2Baxref>)认为埋藏溶解碳酸盐不会显著影响净碳酸盐岩储层孔隙度的增加。此外,他们指出,孔隙水高度欠饱和对方解石在大多数情况下会迅速中和在迁移之前碳酸盐储层,因此解散会局限于一个狭窄的反应前在骨折情况下酸性水域将达到储层水平。但Halahatang而言,活动断裂的流行导致了多级复活的缺点在剪切和扩展,以及多孔断层岩石和dissolution-enhanced蛀牙的形成,就是明证stylobreccias和相关的骨折和岩穴以及断层岩石暴露在附近露头([<gydF4y2Baxref ref-type="bibr" rid="B93">
93年</gydF4y2Baxref>])和空腔附近断层成像(<gydF4y2Baxref ref-type="bibr" rid="B23">
23</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B36">
36</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B37">
37</gydF4y2Baxref>,<gydF4y2Baxref ref-type="bibr" rid="B121">
121年</gydF4y2Baxref>]。断层孔隙度和丰富和核心的基础上观察,Ukar et al。<gydF4y2Baxref ref-type="bibr" rid="B93">
93年</gydF4y2Baxref>]表明,当地的中期形成的孔隙度增强5 - 10%是合理的。多孔岩石断层和dissolution-enhanced蛀牙和骨折可以提供油气存储和迁移途径和负责decameter-scale下降和大量的钻井泥浆损失。</gydF4y2Bap>
</sec>
</sec>
<sec id="sec6">
<title>6。结论</gydF4y2Batitle>
<p>岩石、地球化学和microthermometric 16 ~ 230样本结果整个Halahatang油田井表明,中奥陶世岩石经历了多个阶段的压裂,解散和矿化。</gydF4y2Bap>
<p>与上覆Lianglitage形成广泛的近地表岩溶角砾岩,cave-fill Yijianfang我们没有发现证据形成的沉积物,彻骨的表观遗传引起岩溶过程。近地表Yijianfang成岩特征的形成是局限于斑点面料充满移置碳酸盐淤泥和水泥形成生物扰动作用的结果(0)阶段,原生孔隙度与近地表解散类似改变主机的岩石(1 - 3%),反对显著增加porosity-permeability与这个事件有关。后续二次溶解导致斑点面料内孔隙度增加多达10%。</gydF4y2Bap>
<p>横切部分序列之间的关系巩固了骨折后斑点和岩穴,面料和方解石水泥馅料的稳定同位素组成表明多个后续结构成岩阶段发生在浅到深埋藏成岩环境。<gydF4y2Baitalic>
δ</gydF4y2Baitalic><sup>18</gydF4y2Basup>O分析与地热梯度表明水泥降水在浅(~ 220 m,阶段1 - 2)、中级(~ 625,第三阶段),和深度(4 - 7 ~ 2000 m,阶段)成岩环境。石油流体包裹体的存在在巩固阶段3和年轻确认系统中碳氢化合物的存在时填空矿物沉淀。</gydF4y2Bap>
<p>阶段0 - 2解散与可能的大气流体的渗透,而3 - 4阶段可能造成的酸性液体与中晚期的志留纪和Devonian-Permian生烃。第五阶段是与萤石和重晶石矿化有可能更深的流体来源。的等时线年龄<gydF4y2Bainline-formula>
<mml:math xmlns:mml="http://www.w3.org/1998/Math/MathML" id="M31">
<mml:mn>
400年</米米l:mn>
<mml:mo>
±</米米l:mo>
<mml:mn>
37</米米l:mn>
<mml:mtext>
</mml:mtext>
<mml:mtext>
马</米米l:mtext>
</mml:math>
</inline-formula>证实了第五阶段解散和随后的胶结发生在年底前泥盆世。阶段6方解石升高<gydF4y2Basup>87年</gydF4y2Basup>Sr /<gydF4y2Basup>86年</gydF4y2Basup>Sr由于外部流体渗透与二叠纪岩浆活动有关。阶段7 stylobreccias和骨折与Mg-rich液体和总结变形有关。波动,但高(80 - 120°C)、均化温度和一般高盐度(5 - 20% NaCl电化学当量)的流体包裹体被困在晚期方解石胶结物表明潜在reequilibration更深的流体包裹体,高温液体。骨折的密切联系与岩穴沿着缝合线的所有阶段和矿化表明,他们都是腐蚀性流体通路。</gydF4y2Bap>
</sec>
<back>
<sec sec-type="data-availability">
<title>数据可用性</gydF4y2Batitle>
<p>的数据支持本研究的发现提供的补充材料。</gydF4y2Bap>
</sec>
<sec sec-type="COI-statement">
<title>的利益冲突</gydF4y2Batitle>
<p>没有利益冲突声明。</gydF4y2Bap>
</sec>
<ack>
<title>确认</gydF4y2Batitle>
<p>我们感谢杨Haijun Zhibin黄,春燕气,艾米丽兴,Wenqing锅,Kuanzhi赵,于你们,从石油和其他访问核心和富有成果的讨论。乾隆这手稿受益与鲍勃•劳克斯讨论傅,Chaozhong Ning,利维亚Sivila。我们要感谢莎拉艾略特对她的帮助和SEM分析和图像处理和贝弗利Dejarnett为她帮助理解生物扰动作用在碳酸盐岩和挖掘过程。这个手稿的出版授权的经济地质学的主任。这项研究是由CNPC-USA CNPC-Tarim油田公司和骨折的研究和应用财团。断裂模式发展我们的工作和成岩作用部分是由格兰特DE-FG02-03ER15430化学科学、地球科学和生物科学部门,办公室基本能源科学,美国能源部科学办公室,。</gydF4y2Bap>
</ack>
<sec sec-type="supplementary-material" id="supplementary-material-1">
<title>补充材料</gydF4y2Batitle>
<supplementary-material xlink:href="//www.newsama.com/downloads/journals/geofluids/2020/9037429.f1.pdf" id="supp-1" mimetype="application/pdf">
<label>补充材料</lgydF4y2Baabel>
<p>补充材料包括稳定同位素分析、放射性同位素分析和流体包裹体分析。辅料我:稳定同位素分析。补充材料II:放射性同位素分析。辅料III:流体包裹体分析。</gydF4y2Bap>
</supplementary-material>
</sec>
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地质学会杂志》上</gydF4y2Baitalic>
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