Meso-Neoproterozoic tectono-thermal evolution in the northern margin of North China Craton: Constraints from zircon (U-Th)/He ages
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摘要: 由于复杂的构造沉积史和缺乏有效古温标，华北克拉通北缘燕辽裂陷带中—新元古界热史研究很薄弱，造成古老烃源岩成熟演化过程一直存在争议。研究利用锆石（U-Th）/He热定年技术探讨了燕辽裂陷带自中元古代以来的构造-热演化史，并分析了中元古界两套烃源岩成熟演化期次。燕辽裂陷带中—新元古界单颗粒锆石（U-Th）/He年龄均小于地层年龄，有效地记录了研究区早期的热信息，其中新元古界龙山组单颗粒（U-Th）/He年龄与有效铀浓度具有负相关性。通过正、反演耦合模拟明确了燕辽裂陷带曾经历过440~310 Ma和~220 Ma至今两期快速冷却事件，分别由白乃庙岛弧碰撞和蒙古-鄂霍次克洋洋壳俯冲引起；并揭示出奥陶纪末期和三叠纪末期地层温度变化对古老烃源岩成熟演化具有重要影响。
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关键词:
- 锆石(U-Th)/He /
- 燕辽裂陷带 /
- 中—新元古界 /
- 正演模拟 /
- 烃源岩成熟演化
Abstract: Due to the complicated tectonic and sedimentary history and the lack of effective paleo-thermal indicators, the Meso-Neoproterozoic thermal history of the Yanliao rift zone in the northern margin of the North China Craton is ambiguous, which causes the maturation evolution of ancient source rocks controversial. In this study, zircon (U-Th)/He dating is used to study the tectono-thermal evolution of the Yanliao rift zone since the Mesoproterozoic, and we also analyzed the maturation evolution stages of two sets of Mesoproterozoic source rocks. The single-grain zircon (U-Th)/He ages from the Meso-Neoproterozoic strata in the Yanliao rift zone are all younger than the corresponding stratigraphic ages and therefore recorded the thermal information in the past. Moreover, the single-grain zircon (U-Th)/He ages of the Neoproterozoic Longshan formation show a negative correlation with the effective uranium concentration. The forward and inverse coupling simulation revealed that the Yanliao rift zone experienced two rapid cooling events of 440~320 Ma and 220~0 Ma, probably related to the collision between the Bainaimiao island arc and the northern margin of the North China Craton and the subduction of Mongolia Okhotsk oceanic crust below the eastern North China Craton, respectively. In addition, the formation temperature variations at the end of Ordovician and the end of Triassic had an important influence on the maturation evolution of Mesoproterozoic source rock. -
0. 引言
(U-Th)/He热定年技术是基于矿物中U和Th放射性元素发生α衰变产生He提出的。通过测量矿物中238U、232Th和4He的含量, 就可以得到矿物的(U-Th)/He年龄。目前, 常用于(U-Th)/He热定年的矿物为磷灰石、锆石及榍石(Farley et al., 1996; Reiners et al., 2004; 杨美伶和陈宣华, 2005; 程璐瑶等, 2021)。其中, 磷灰石(U-Th)/He热定年技术仅能揭示40~80℃低温范围内的精细热历史(Wolf et al., 1996), 而锆石(U-Th)/He热定年技术具有较高的封闭温度(140~220℃), 可有效地用于研究深层、古老地质体的热历史。由于Reiners et al.(2004)建立的锆石He扩散模型仅考虑了温度对He扩散行为的影响, 无法解释同一样品中单颗粒锆石He年龄分散性。为了解决这一问题, Guenthner et al.(2013)提出了锆石辐射损伤积累和退火模型(Zircon Radiation Damage Accumulation and Annealing Model, ZRDAAM), 该模型能有效地解释由辐射损伤和U-Th分带性造成的单颗粒He年龄分散性, 极大地推动了锆石(U-Th)/He热定年的发展。许多学者基于该新模型对古老克拉通盆地早期热历史开展了细致研究(Orme et al., 2016; Powell et al., 2016; Baughman and Flowers, 2020)。例如, Orme et al.(2016)结合锆石(U-Th)/He实测年龄和正演模拟揭示了美国怀俄明克拉通自元古代以来的古温度史。相对于国外, 国内关于锆石(U-Th)/He热定年技术研究古老克拉通盆地构造-热演化的研究还很少(邱楠生等, 2020)。
位于中国东部的华北克拉通自元古宙以来经历了漫长且复杂的构造-热演化史(翟明国, 2019)。一些学者曾利用磷灰石裂变径迹技术探讨过华北克拉通北缘燕辽裂陷带中生代以来的热历史(吴珍汉等, 2000; 翟鹏济等, 2003; 李建锋等, 2010), 但由于该方法揭示的温度范围局限性, 无法研究更早期的热历史。相对于磷灰石裂变径迹技术, 锆石(U-Th)/He热定年技术可记录更高温度的热信息, 因此在研究华北克拉通北缘早期热演化方面具有优势。此研究系统分析了燕辽裂陷带中—新元古界样品单颗粒锆石(U-Th)/He年龄恢复的热史有效性以及单颗粒锆石(U-Th)/He年龄分散性的主控因素; 基于ZRDAAM模型开展正、反演耦合模拟, 精细揭示了燕辽裂陷带中元古代以来的构造-热历史, 并探讨了热演化对研究区古老烃源岩成熟演化的影响, 从而为华北克拉通北缘构造演化和油气勘探提供了理论依据。
1. 地质背景
燕辽裂陷带位于华北克拉通北缘燕山—辽西地区(图 1), 其北临内蒙地轴, 南接华北平原, 总面积约10.6×104 km2。燕辽裂陷带由宣龙、冀北、辽西、京西、冀东5个坳陷区和山海关、密怀2个隆起区所组成。燕辽裂陷带沉积具有中国最古老且未变质的中—新元古代沉积地层, 自下而上发育中元古界长城系、蓟县系、待建系和新元古界青白口系(图 2)。
图 1 华北克拉通北缘燕辽裂陷带构造单元及样品位置(据王铁冠等, 2016修改)Figure 1. Tectonic units of the Yanliao rift zone in the northern margin of North China Carton, showing the sample locations (modified after Wang et al., 2016)
图 2 燕辽裂陷带中新元古界地层柱状图(据王浩等, 2019修改)Figure 2. Stratigraphic column of Meso-Neoproterozoic strata in the Yanliao rift zone (modified after Wang et al., 2019)古元古代末期, 由于吕梁运动, 华北克拉通东、西陆块拼合在一起, 成为Columbia超大陆的一部分。随后, Columbia超大陆裂解作用造成华北克拉通形成多个裂陷槽(Hou et al., 2006)。这一时期华北克拉通构造基底不稳定, 断裂、地震火山活动频发(Wang et al., 2015), 地层沉积厚度巨大, 且横向变化显著, 地层之间多为不整合接触。长城系形成于中元古界早期, 自下而上包括常州沟组、串岭沟组、团山子组、大红峪组。其中常州沟组以砂砾岩为主, 与下伏太古宙—古元古代变质基底呈角度不整合接触。串岭沟组为潟湖沉积, 主要由页岩和白云岩组成。团山子组白云岩夹少量安山岩、凝灰岩, 为非造山岩浆活动的产物。大红峪组主要由石英砂岩、砂质白云岩组成。长城系沉积后华北克拉通北缘逐渐由陆内裂陷阶段向被动陆源阶段过渡, 沉积速率增加。蓟县系在此阶段内形成, 自下而上包括高于庄组、杨庄组、雾迷山组、洪水庄组和铁岭组。高于庄组以白云岩为主, 杨庄组以泥质白云岩为主, 雾迷山组沉积了巨厚的灰—深灰色白云岩, 洪水庄组岩性为灰色白云岩夹薄层褐色页岩。中元古代中期, 待建系下马岭组为黑色页岩、粉砂岩夹白云岩组合, 形成于相对缺氧及沉积物源供给缺乏的沉积环境。在区域上下马岭组与下伏铁岭组多为平行不整合接触, 与上覆龙山组存在明显的不整合界面, 被认为是Columbia超大陆裂解与Rodinia超大陆汇聚在华北克拉通内部的响应(陆松年等, 2012; 李怀坤等, 2020)。新元古代时期, 华北克拉通北缘受板块碰撞影响经历了一定程度的构造隆升过程(王伟锋等, 1997; 曲永强等, 2012), 沉积环境为滨岸浅水相沉积, 该时期形成的龙山组和景儿峪组以砂岩和页岩为主, 夹少量碳酸盐岩。
寒武纪至中奥陶世, 华北大部被海水淹没, 属于陆表海沉积环境, 华北克拉通北缘燕辽裂陷带内形成稳定的浅海碳酸盐岩沉积。中晚奥陶世以后, 整个华北板块主体同时受到南北两侧板块汇聚俯冲作用, 使得华北板块整体抬升, 从而缺失上奥陶统至下石炭统地层(张旗, 2011)。晚石炭世—中三叠世华北地区为海陆交互相、滨海和潟湖相沉积环境, 岩性主要为砂岩、粉砂岩和泥岩。晚三叠世开始, 由于燕山期强烈的构造运动, 使得下部地层倒转直立, 整个华北克拉通三叠系与上覆侏罗系之间存在明显的不整合(赵越等, 2004)。侏罗纪—白垩纪构造活动以断裂、褶皱和强烈的岩浆活动为主(马寅生等, 2002; 郑建平, 2020), 对中新元古界的褶皱构造起破坏作用。白垩纪以后区域内隆升抬起, 以剥蚀作用为主, 燕辽裂陷带内局部残留厚度不大的白垩系、古近系、新近系及第四系。
燕辽裂陷带中元古界主要发育高于庄组、洪水庄组、下马岭组等3套有效烃源岩, TOC含量≥0.5%, 其中洪水庄组和下马岭组为黑色页岩型烃源岩, 而高于庄组属于碳酸盐岩烃源岩(钟宁宁等, 2004)。洪水庄组烃源岩现今处于成熟—高成熟热演化阶段, 实测等效镜质体反射率介于0.96%~2.13%, 平均值1.43%;下马岭组和高于庄组热演化程度已达到过成熟阶段, 实测等效镜质体反射率平均值大于1.7%(王铁冠等, 2016)。
2. 样品与实验结果
为了精细揭示华北克拉通北缘燕辽裂陷带早期的构造-热演化史, 文中共采集了3块石英砂岩样品开展研究(图 1)。其中, 样品LX1采自辽西坳陷凌源地区的青白口系龙山组, 样品LX2和LX3分别采自冀北坳陷老庄户地区的长城系大红峪组和常州沟组。通过重矿物分选技术得到测试需要的锆石颗粒。
锆石(U-Th)/He年龄测试是在中国科学院地质与地球物理研究所40Ar/39Ar与(U-Th)/He年代学实验室完成的, 具体分析方法详见Wu et al.(2018)。主要实验步骤包括: 1在每个样品中挑选8颗自形程度高且不含包裹体的锆石颗粒, 并测量颗粒的长、宽和锥高; 2使用1mm×1mm的金属铌囊包裹锆石颗粒, 利用澳大利亚科学仪器公司生产的Alphachron MK Ⅱ氦提取测量仪进行矿物He含量测试; 3待完成锆石颗粒He含量测试后, 将铌囊从氦提取测量仪中取出, 放入PFA(铁氟龙)小瓶中, 并加入230Th、235U浓度已知的稀释剂溶液和浓HF溶液, 使用标准压力消解技术溶解样品, 使用Thermo Fisher X-Series Ⅱ电感耦合等离子体质谱仪测试锆石颗粒U、Th浓度; 4用IsoplotR(Vermeesch, 2018)计算锆石颗粒(U-Th)/He年龄, 同时根据Gautheron and Tassan-Got(2010)提出计算模型对年龄结果进行校正。锆石(U-Th)/He年龄测试结果见表 1。
表 1 燕辽裂陷带中新元古界锆石(U-Th)/He年龄测试结果Table 1. Zircon (U-Th)/He data of Meso-Neoproterozoic in the Yanliao rift zone样品号 U/×10-6 Th/×10-6 He/(nmol/g) Th/U 半径/μm 质量/μg eU/×10-6 年龄/Ma ±1σ/Ma Ft 校正年龄/Ma ±1σ/Ma LX1-1 215.141 147.737 378.94 0.710 39.8 3.08 249.9 276.46 4.49 0.721 383.44 20.16 LX1-2 64.033 63.799 160.62 1.030 37.1 2.63 79.0 367.82 6.53 0.701 524.71 27.84 LX1-3 121.428 116.531 269.33 0.992 31.9 1.64 148.8 328.55 5.53 0.657 500.08 26.38 LX1-4 98.279 90.884 308.12 0.956 37.3 2.43 119.6 462.42 8.71 0.702 658.72 35.20 LX1-5 122.785 76.599 313.18 0.645 42.2 3.37 140.8 401.21 7.09 0.737 544.38 28.87 LX1-6 93.467 83.668 284.90 0.925 32.1 1.53 113.1 452.50 8.92 0.662 683.53 36.74 LX1-7 558.091 324.982 602.87 0.602 29.6 1.37 634.5 174.73 2.96 0.637 274.30 14.48 LX1-8 255.394 177.548 429.69 0.718 33.0 1.69 297.1 263.93 4.57 0.671 393.34 20.81 LX2-1 109.620 66.037 92.85 0.622 50.9 6.41 125.1 136.88 2.27 0.779 175.71 9.26 LX2-2 187.939 93.531 124.31 0.514 39.1 2.69 209.9 109.52 2.07 0.718 152.53 8.15 LX2-3 172.895 104.976 152.60 0.627 46.6 4.96 197.6 142.43 2.34 0.759 187.65 9.88 LX2-5 174.687 100.043 111.15 0.592 41.6 2.98 198.2 103.76 1.83 0.734 141.36 7.49 LX2-6 347.411 93.139 140.20 0.277 30.1 1.31 369.3 70.49 1.23 0.646 109.12 5.78 LX2-7 171.052 99.991 104.70 0.604 48.2 5.15 194.5 99.60 1.66 0.767 129.86 6.84 LX2-8 213.721 173.049 156.02 0.837 41.4 2.96 254.4 113.33 1.89 0.731 155.03 8.17 LX3-1 220.110 98.923 124.56 0.464 40.2 2.99 243.4 94.79 1.60 0.725 130.74 6.90 LX3-2 230.152 109.995 169.00 0.494 44.2 4.05 256.0 121.97 2.23 0.748 163.06 8.68 LX3-3 735.832 442.919 466.39 0.622 33.8 1.76 839.9 102.74 1.69 0.678 151.53 7.98 LX3-4 159.371 50.203 80.15 0.486 38.0 2.40 136.0 108.99 1.89 0.712 153.08 8.10 LX3-5 99.963 30.396 86.51 0.325 38.8 2.38 171.2 93.64 1.56 0.72 130.06 6.85 LX3-6 297.526 84.226 46.24 0.314 27.2 0.99 107.1 80.08 1.71 0.613 130.64 7.10 LX3-7 165.490 37.400 177.01 0.293 37.4 2.21 317.3 103.27 1.82 0.71 145.45 7.71 LX3-8 159.371 50.203 86.37 0.234 33.7 1.80 174.3 91.85 2.34 0.681 134.88 7.57 注: Ft为α粒子射出效应的校正参数, 计算方法详见Farley et al. (1996); eU为有效铀浓度, 计算公式为eU=U+0.235×Th (Flowers et al., 2009) 样品LX1、LX2和LX3的实测单颗粒锆石(U-Th)/He年龄均小于相应的地层年龄, 表明这些样品沉积后曾经历过不同程度的高温He扩散。其中, 样品LX1单颗粒锆石(U-Th)/He年龄介于683.53~274.30 Ma, 且与有效U浓度呈负相关性(图 3a), 表现出较强的分散性, 这主要是由辐射损伤造成的(Guenthner et al., 2013)。样品LX2和LX3单颗粒锆石(U-Th)/He年龄集中分布于187.65~109.12 Ma之间, 表明它们在晚侏罗世时期经历过全部He扩散, 早期的热信息已被重置。另外, 这2个样品的单颗粒锆石(U-Th)/He年龄与有效铀浓度及颗粒半径无明显相关性(图 3)。
图 3 华北克拉通北缘燕辽裂陷带样品单颗粒锆石(U-Th)/He年龄与有效铀浓度和颗粒半径关系图图中虚线表示样品沉积年龄
a—锆石(U-Th)/He年龄与有效铀浓度关系; b—锆石(U-Th)/He年龄与颗粒半径关系Figure 3. Correlation of zircon (U-Th)/He age with effective uranium concentration (a) and particle radius (b) in the samples from the Yanliao rift zoneThe dotted lines in the figures indicate the deposition age of the samples3. 热史模拟
以实测锆石(U-Th)/He年龄为约束条件, 研究基于ZRDAAM模型的正演和反演耦合模拟揭示了研究区中元古代以来的构造-热演化史(Guenthner et al., 2013)。其中, 正演模拟是将ZRDAAM模型程序嵌入MATLAB软件中进行的; 而反演模拟是基于正演模拟路径, 利用HeFTy软件通过随机搜索获取得到最佳热史路径(Ketcham, 2005)。
对于正演模拟, 需要输入的参数包括颗粒的U、Th和He含量、颗粒半径平均值及标准差。由于样品中单颗粒He年龄较分散, 与有效铀浓度之间具有非线性相关性, Guenthner et al.(2014)提出了继承性包络线的概念, 即沉积物源、元素含量和颗粒半径均不相同的颗粒在经历相同热史情况下可能的He年龄分布区间(图 4), 继承性包络线的上、下边界分别由颗粒的平均半径加、减其标准差得出。在正演模拟中需要设置不同的热史路径, 当所有实测颗粒的(U-Th)/He年龄均落入继承性包络线内时, 认为假定热史是可靠的。
图 4 青白口系龙山组样品热史模拟结果a—正演模拟中输入的热史路径; b—e—分别表示不同热史路径下模拟得出的继承性包络线与实测年龄之间的关系(图中浅灰色、中灰色、深灰色区域分别对应起始时间为2500 Ma、1800 Ma和900 Ma的模拟结果); f—反演模拟得到的可能热史路径(其中绿色线代表拟合度较低的热史路径, 紫色线代表拟合度较高的热史路径, 黑色线为最佳热史路径, 黑色方框为反演模拟的约束条件)Figure 4. Thermal history modeling results of the samples from the Longshan formation in the Qingbaikou system(a) The input thermal history path in a forward modeling; (b-e) The inherited envelopes obtained from different thermal history paths; The light gray area, medium gray area and dark gray area in the figure represent the modeling results corresponding to the starting time of 2500 Ma, 1800 Ma, and 900 Ma, respectively; (f) The possible thermal history path obtained by inversion modeling, in which green lines represent the thermal history path with low fitting degree, purple lines represent the thermal history path with high fitting degree, black line is the most possible thermal history path, and black boxes are constraints of inverse modeling由于研究采集的样品为碎屑岩, 因此在正演过程中需要考虑部分颗粒沉积前已含有的He含量(即继承性He)。为了解决这个问题, Guenthner et al.(2015)将锆石开始形成到在研究区沉积的时间间隔经历的温度设定为沉积时的地表温度。早期研究表明, 青白口系龙山组碎屑锆石主要来源于~1.85 Ga和~2.5 Ga, 长城系常州沟组和大红峪组碎屑锆石年龄集中分布在~2.5 Ga(高林志等, 2007; 第五春荣等, 2011; Wan et al., 2011; 胡波等, 2013)。因此在设置正演热史路径时, 参考碎屑锆石形成时间及地层沉积时间(图 2), 将龙山组样品LX1的热史路径起始时间分别设置为2500 Ma、1850 Ma和900 Ma, 大红峪组样品LX2的热史路径起始时间设置为2500 Ma和1625 Ma, 常州沟组样品LX3的正演模拟起始时间设置为2500 Ma和1800 Ma。地层开始沉积时期古地表温度是热史模拟的重要约束条件, 根据前寒武纪气候和古沉积环境研究成果(Robert and Chaussidon, 2006; Gaucher et al., 2008), 中—新元古代时期平均温度为~20℃, 因此在热史模拟中将古地表温度设置为20℃。
对于反演模拟, 起始时间设定为对应地层开始沉积时间。青白口系龙山组样品起始时间为900 Ma, 长城系常州沟组和大红峪组的年龄分别为1800 Ma和1625 Ma, 初始热史路径基于正演模拟进行设置。由于反演模拟不能对分散性强的多个颗粒进行约束, 因此, 需选取典型颗粒进行模拟。
3.1 青白口系龙山组样品LX1
结合燕辽裂陷带东段残余地层厚度(图 2)和不整合面发育程度, 为样品LX1设置了4条完整的温度路径(图 4a中路径B—D、A—C、A—D和A—E), 用于反映新元古代以来样品完整的热演化史。奥陶纪末期的构造运动造成研究区志留系、泥盆系和上石炭统缺失, 形成广泛分布的不整合面(张旗, 2011)。由于缺乏对构造隆升剥蚀过程的精确研究, 文中在440~310Ma热史模拟中, 分别讨论快速隆升剥蚀(路径A)和匀速隆升剥蚀(路径B)两种情况对模拟结果的影响(图 4a)。对于热史路径B—D(~440 Ma地层温度为90℃, 440~310 Ma地层温度匀速降低, ~220 Ma地层温度为140℃), 部分颗粒实测结果落在继承性包络线下边界之外(图 4b); 而对于热史路径A—D(~440 Ma地层温度为90℃, 440~310 Ma地层温度下降速率减小, ~220 Ma地层温度为140℃), 实测结果均能落在继承性包络线范围内(图 4c)。因此, 相对于路径B—D, 路径A—D与实际热演化历史更接近。自三叠纪末期开始华北克拉通北缘长期处于构造隆升状态, 造成中—新元古界广泛出露于地表(赵越等, 2004)。在三叠纪以来的热史模拟中, 主要研究不同地层埋藏温度(路径C、路径D、路径E)对模拟结果的影响。对于热史路径A—C(~220 Ma地层温度为130℃), 继承性包络线下边界大于部分颗粒实测结果(图 4d), 说明设定地层温度过低; 对于温度路径A—E(~220 Ma地层温度为150℃), 继承性包络线上界小于部分颗粒实测结果(图 4e), 反映出设定地层温度过高; 当热史路径设置为A—D(~220 Ma地层温度为140℃)时, 颗粒实测结果均能落在继承性包络线内(图 4c)。因此, 相对于路径A—C和A—E, 路径A—D与实际热演化历史更接近。以正演模拟得到的热史路径A—D为基础, 选取样品中(U-Th)/He年龄中值的锆石颗粒进行反演模拟, 可以得到与青白口系龙山组样品的真实热演化史最符合的热史路径(图 4f中黑色路径)。
3.2 长城系大红峪组样品LX2
对于长城系大红峪组样品LX2, 结合残余地层和不整合面发育程度设置了4条完整的温度路径(图 5a中路径A—D、B—C、B—D和B—E)。大红峪组样品经历的构造运动与上覆青白口系相似, 在530~310 Ma之间设置了低温(路径A)和高温(路径B)两种热演化路径, 主要用于分析地层埋藏温度对模拟结果的影响。对于温度路径B—D(~440 Ma地层温度为140℃, ~220 Ma地层温度为230℃)和温度路径A—D(~440 Ma地层温度为140℃, ~220 Ma地层温度为230℃), 通过正演模拟得到的继承性包络线无明显差异, 实测结果均能落在包络线范围内(图 5b、5c)。考虑到青白口系龙山组与大红峪组之间地层厚度超过4000m(图 2), 而且龙山组在~440Ma时地层温度已达到90℃, 所以530~310 Ma热史路径B更接近地层的实际热历史。确定~440 Ma地层温度后, 改变~220 Ma时期的地层温度进行正演模拟, 对于热史路径B—C(~220 Ma地层温度为220℃), 继承性包络线下边界大于部分颗粒实测结果(图 5d), 说明设定地层温度过低; 对于温度路径B—E(~220 Ma地层温度为240℃), 继承性包络线上界小于部分颗粒实测结果(图 5e), 反应出设定地层温度过高; 当热史路径设置为B—D(~220 Ma地层温度为230℃)时, 颗粒实测结果均能落在继承性包络线内(图 5b)。正演模拟结果揭示出热史路径B—D与长城系大红峪组样品实际热演化过程更接近。以正演模拟结果为基础, 选取典型颗粒进行反演模拟得到了最可能的热史路径(图 5f中黑色路径)。
图 5 长城系大红峪组样品热史模拟结果a—正演模拟中输入的热史路径; b—e—分别表示不同热史路径下模拟得出的继承性包络线与实测年龄之间的关系(图中深灰色和灰色区域分别对应起始时间为2500 Ma和1620 Ma的模拟结果); f—反演模拟得到的可能热史路径(其中绿色线代表拟合度较低的热史路径, 紫色线代表拟合度较高的热史路径, 黑色线为最佳热史路径, 黑色方框为反演模拟的约束条件)Figure 5. Thermal history modeling results of the samples from the Dahongyu formation in the Changcheng system(a) The Input thermal history path in a forward modeling; (b-e) The inherited envelopes obtained from different thermal history paths; The dark gray area and the gray area in the figure represent the modeling results corresponding to the starting time of 2500 Ma and 1620 Ma, respectively; (f) The possible thermal history path obtained by inversion modeling, in which green lines represent the thermal history path with low fitting degree, purple lines represent the thermal history path with high fitting degree, black line is the most possible thermal history path, and black boxes are constraints of inverse modeling3.3 长城系常州沟组样品LX3
上已叙述, 样品LX3曾经历过高温He扩散, 其锆石(U-Th)/He年龄仅能有效地反映最后一期冷却事件的信息。同样地, 结合不整合面和残余地层厚度, 为样品LX3设置了4条完整的热史路径(图 6a中路径A—D、B—D、C—D和B—E)。由于华北克拉通北缘中—新元古界地层在三叠纪末期达到最大埋藏深度(马寅生等, 2002), 为了分析~220Ma地层温度对模拟结果的影响, 在正演模拟中分别设置了温度由低到高的3条热史路径(A、B、C)。对于温度路径A—D(~220 Ma地层温度为250℃), 有效铀浓度较低部分颗粒实测结果落在继承性包络线下边界之外, 有效铀浓度高的颗粒则落在继承性包络线上边界之外(图 6b)。对于温度路径C—D(~220 Ma地层温度为270℃), 部分颗粒实测结果则落在继承性包络线上边界之外(图 6c)。只有温度路径设为B—D(~220 Ma地层温度为260℃)时, 实测结果均能落在继承性包络线范围内(图 6d), 说明温度路径B—D最接近真实热演化过程。改变~220 Ma至今的冷却速率, 分析冷却速率降低(路径D)和冷却速率稳定(路径E)条件下热史模拟结果的差异。在设置温度路径B—E(~220 Ma至今匀速冷却)和B—D(~220 Ma至今冷却速率减缓)情况下进行正演模拟, 结果显示~220 Ma至今匀速冷却情况下有效铀浓度较高的颗粒实测结果落在继承性包络线上边界之外(图 6e), 而冷却速率减缓情况下实测结果均能落在继承性包络线内(图 6d)。正演模拟结果反映温度路径B—D与样品实际热演化情况最接近。依据正演模拟结果进行反演模拟得到拟合度较高的热史路径(图 6f中黑色路径)。
图 6 常州沟组样品热史模拟结果a—正演模拟中输入的热史路径; b—e—分别表示不同热史路径下模拟得出的继承性包络线与实测年龄之间的关系(图中深灰色和灰色区域分别对应起始时间为2500 Ma和1800 Ma的模拟结果); f—反演模拟得到的可能热史路径(其中绿色线代表拟合度较低的热史路径, 紫色线代表拟合度较高的热史路径, 黑色线为最佳热史路径, 黑色方框为反演模拟的约束条件)Figure 6. Thermal history modeling results of the samples from the Changzhougou formation in the Changcheng system(a) The input thermal history path in a forward modeling; (b-e) The inherited envelopes obtained from different thermal history paths; The dark gray area and the gray area in the figure represent the modeling results corresponding to the starting time of 2500 Ma and 1800 Ma, respectively; (f) The possible thermal history path obtained by inversion modeling, in which green lines represent the thermal history path with low fitting degree, purple lines represent the thermal history path with high fitting degree, black line is the most possible thermal history path, and black boxes are constraints of inverse modeling4. 讨论
研究利用锆石(U-Th)/He热定年技术揭示出华北克拉通北缘燕辽裂陷带经历了晚奥陶世—晚石炭世(440~310 Ma)和晚三叠世至今(220~0 Ma)两期冷却事件。在热史模拟路径设置中, 设定的4条热史路径均符合样品经历的构造演化过程, 但不同热史条件下模拟结果与实测锆石(U-Th)/He年龄之间的关系有明显差异。只有当所有单颗粒锆石(U-Th)/He年龄均落在继承性包络线内时(图 4—图 6), 此时给定的热史路径与样品真实构造-热演化过程最为接近。晚奥陶世至晚石炭世, 华北克拉通北缘与白乃庙岛弧带发生碰撞(张允平等, 2010; Zhang et al., 2014a), 导致华北克拉通北缘燕辽裂陷带长期处于隆升剥蚀状态, 形成了区域性的不整合面。热史模拟结果反映出长期隆升剥蚀状态造成的地层温度降低, 同时显示出440~310 Ma隆升剥蚀速率呈现下降趋势(图 4—图 6)。考虑到燕辽裂陷带长期处于低地温、低热流的热状态(李慧莉等, 2005; 邱楠生等, 2009, 2010), 设定其地温梯度为25℃/km, 计算得到晚奥陶世至晚石炭世剥蚀量约1600m。晚三叠世华北克拉通北侧蒙古-鄂霍次克洋洋壳向南俯冲, 引起华北克拉通北缘形成挤压构造应力场, 燕辽裂陷带开始了强烈的区域构造变形(Hu et al., 2010; Liu et al., 2012; Zhang et al., 2014b)。与热史模拟结果相对应, 中—新元古界地层隆升剥露至地表, 地层温度持续下降(图 4—图 6)。晚三叠世至今, 华北克拉通东部渤海湾盆地受到华北克拉通破坏作用影响经历了高热流阶段(Chang et al., 2018), 现今大地热流仍相对较高, 达到~64.5 mW/m2(Qiu et al., 2014)。然而华北克拉通北缘现今热流相对较低, 仅为~50 mW/m2(Jiang et al., 2019), 这表明华北克拉通破坏对北缘热流影响有限。虽然燕辽裂陷带在三叠纪以来经历了燕山运动等重要的构造-热事件, 在整体隆升剥蚀的综合影响下, 中—新元古界温度仍呈现持续降低的特征。
根据热史模拟得到的地层温度史和现今地温场数据(Jiang et al., 2019), 结合Easy%RO模型恢复了燕辽裂陷带中元古代以来的温度演化史及烃源岩成熟演化史(图 7)。模拟结果显示, ~1450 Ma之前的快速沉降造成高于庄组烃源岩成熟度迅速升高, 在~1520 Ma进入成熟阶段(RO为0.5%), ~1450 Ma进入生油阶段(RO为0.7%)。1450~540 Ma华北克拉通北缘以构造隆升作用为主(曲永强等, 2012), 高于庄组烃源岩在~540 Ma仍处于成熟阶段(RO为1.1%)。由于洪水庄组烃源岩埋深较小, 地层长期保持40℃以下, ~540 Ma烃源岩处于未成熟阶段(RO小于0.5%)。540~440 Ma由于地层沉降造成烃源岩成熟度进一步增加, 440 Ma高于庄组烃源岩RO接近1.3%, 洪水庄组烃源岩进入成熟阶段(RO为0.5%)。440~310 Ma期间燕辽裂陷带长期处于隆升剥蚀状态, 有机质热演化作用基本停滞。310~220 Ma时期, 由于地层埋藏深度增加和火山活动增强(Zhang et al., 2014a), 造成烃源岩成熟度快速升高。高于庄组烃源岩在230 Ma进入过成熟阶段(RO为2.6%), 洪水庄组烃源岩成熟度在~220 Ma升高至0.8%。~220 Ma至今地层温度持续下降, 烃源岩热演化作用基本停止。
图 7 燕辽裂陷带热演化史与烃源岩成熟度演化史Figure 7. Thermal evolution history and maturity evolution of source rocks in the Yanliao rift zone5. 结论
华北克拉通北缘燕辽裂陷带中—新元古界青白口系和长城系碎屑岩样品锆石(U-Th)/He年龄分别介于683.53~274.30 Ma和187.65~109.12 Ma, 均小于地层年龄, 其中青白口系样品单颗粒年龄与有效铀浓度具有负相关性。通过正、反演热史模拟不仅明确了青白口系和长城系在~220 Ma分别经历过140℃和230~260℃的高温, 而且揭示出晚奥陶世—晚石炭世和晚三叠世至今两期快速冷却事件, 分别由华北克拉通北缘与白乃庙岛弧带碰撞和蒙古-鄂霍次克洋洋壳俯冲造成的。受快速沉降和构造隆升事件影响, 蓟县系烃源岩经历了二次生烃。其中高于庄组烃源岩在三叠纪末期已进入高成熟阶段, 而洪水庄组烃源岩目前仍处于成熟阶段。
致谢: 感谢中国科学院地质与地球物理研究所吴林博士在锆石(U-Th)/He年龄测试中给予的帮助。责任编辑: 范二平 -
图 1 华北克拉通北缘燕辽裂陷带构造单元及样品位置(据王铁冠等, 2016修改)
Figure 1. Tectonic units of the Yanliao rift zone in the northern margin of North China Carton, showing the sample locations (modified after Wang et al., 2016)
图 2 燕辽裂陷带中新元古界地层柱状图(据王浩等, 2019修改)
Figure 2. Stratigraphic column of Meso-Neoproterozoic strata in the Yanliao rift zone (modified after Wang et al., 2019)
图 3 华北克拉通北缘燕辽裂陷带样品单颗粒锆石(U-Th)/He年龄与有效铀浓度和颗粒半径关系图
图中虚线表示样品沉积年龄
a—锆石(U-Th)/He年龄与有效铀浓度关系; b—锆石(U-Th)/He年龄与颗粒半径关系Figure 3. Correlation of zircon (U-Th)/He age with effective uranium concentration (a) and particle radius (b) in the samples from the Yanliao rift zone
The dotted lines in the figures indicate the deposition age of the samples
图 4 青白口系龙山组样品热史模拟结果
a—正演模拟中输入的热史路径; b—e—分别表示不同热史路径下模拟得出的继承性包络线与实测年龄之间的关系(图中浅灰色、中灰色、深灰色区域分别对应起始时间为2500 Ma、1800 Ma和900 Ma的模拟结果); f—反演模拟得到的可能热史路径(其中绿色线代表拟合度较低的热史路径, 紫色线代表拟合度较高的热史路径, 黑色线为最佳热史路径, 黑色方框为反演模拟的约束条件)
Figure 4. Thermal history modeling results of the samples from the Longshan formation in the Qingbaikou system
(a) The input thermal history path in a forward modeling; (b-e) The inherited envelopes obtained from different thermal history paths; The light gray area, medium gray area and dark gray area in the figure represent the modeling results corresponding to the starting time of 2500 Ma, 1800 Ma, and 900 Ma, respectively; (f) The possible thermal history path obtained by inversion modeling, in which green lines represent the thermal history path with low fitting degree, purple lines represent the thermal history path with high fitting degree, black line is the most possible thermal history path, and black boxes are constraints of inverse modeling
图 5 长城系大红峪组样品热史模拟结果
a—正演模拟中输入的热史路径; b—e—分别表示不同热史路径下模拟得出的继承性包络线与实测年龄之间的关系(图中深灰色和灰色区域分别对应起始时间为2500 Ma和1620 Ma的模拟结果); f—反演模拟得到的可能热史路径(其中绿色线代表拟合度较低的热史路径, 紫色线代表拟合度较高的热史路径, 黑色线为最佳热史路径, 黑色方框为反演模拟的约束条件)
Figure 5. Thermal history modeling results of the samples from the Dahongyu formation in the Changcheng system
(a) The Input thermal history path in a forward modeling; (b-e) The inherited envelopes obtained from different thermal history paths; The dark gray area and the gray area in the figure represent the modeling results corresponding to the starting time of 2500 Ma and 1620 Ma, respectively; (f) The possible thermal history path obtained by inversion modeling, in which green lines represent the thermal history path with low fitting degree, purple lines represent the thermal history path with high fitting degree, black line is the most possible thermal history path, and black boxes are constraints of inverse modeling
图 6 常州沟组样品热史模拟结果
a—正演模拟中输入的热史路径; b—e—分别表示不同热史路径下模拟得出的继承性包络线与实测年龄之间的关系(图中深灰色和灰色区域分别对应起始时间为2500 Ma和1800 Ma的模拟结果); f—反演模拟得到的可能热史路径(其中绿色线代表拟合度较低的热史路径, 紫色线代表拟合度较高的热史路径, 黑色线为最佳热史路径, 黑色方框为反演模拟的约束条件)
Figure 6. Thermal history modeling results of the samples from the Changzhougou formation in the Changcheng system
(a) The input thermal history path in a forward modeling; (b-e) The inherited envelopes obtained from different thermal history paths; The dark gray area and the gray area in the figure represent the modeling results corresponding to the starting time of 2500 Ma and 1800 Ma, respectively; (f) The possible thermal history path obtained by inversion modeling, in which green lines represent the thermal history path with low fitting degree, purple lines represent the thermal history path with high fitting degree, black line is the most possible thermal history path, and black boxes are constraints of inverse modeling
图 7 燕辽裂陷带热演化史与烃源岩成熟度演化史
Figure 7. Thermal evolution history and maturity evolution of source rocks in the Yanliao rift zone
表 1 燕辽裂陷带中新元古界锆石(U-Th)/He年龄测试结果
Table 1. Zircon (U-Th)/He data of Meso-Neoproterozoic in the Yanliao rift zone
样品号 U/×10-6 Th/×10-6 He/(nmol/g) Th/U 半径/μm 质量/μg eU/×10-6 年龄/Ma ±1σ/Ma Ft 校正年龄/Ma ±1σ/Ma LX1-1 215.141 147.737 378.94 0.710 39.8 3.08 249.9 276.46 4.49 0.721 383.44 20.16 LX1-2 64.033 63.799 160.62 1.030 37.1 2.63 79.0 367.82 6.53 0.701 524.71 27.84 LX1-3 121.428 116.531 269.33 0.992 31.9 1.64 148.8 328.55 5.53 0.657 500.08 26.38 LX1-4 98.279 90.884 308.12 0.956 37.3 2.43 119.6 462.42 8.71 0.702 658.72 35.20 LX1-5 122.785 76.599 313.18 0.645 42.2 3.37 140.8 401.21 7.09 0.737 544.38 28.87 LX1-6 93.467 83.668 284.90 0.925 32.1 1.53 113.1 452.50 8.92 0.662 683.53 36.74 LX1-7 558.091 324.982 602.87 0.602 29.6 1.37 634.5 174.73 2.96 0.637 274.30 14.48 LX1-8 255.394 177.548 429.69 0.718 33.0 1.69 297.1 263.93 4.57 0.671 393.34 20.81 LX2-1 109.620 66.037 92.85 0.622 50.9 6.41 125.1 136.88 2.27 0.779 175.71 9.26 LX2-2 187.939 93.531 124.31 0.514 39.1 2.69 209.9 109.52 2.07 0.718 152.53 8.15 LX2-3 172.895 104.976 152.60 0.627 46.6 4.96 197.6 142.43 2.34 0.759 187.65 9.88 LX2-5 174.687 100.043 111.15 0.592 41.6 2.98 198.2 103.76 1.83 0.734 141.36 7.49 LX2-6 347.411 93.139 140.20 0.277 30.1 1.31 369.3 70.49 1.23 0.646 109.12 5.78 LX2-7 171.052 99.991 104.70 0.604 48.2 5.15 194.5 99.60 1.66 0.767 129.86 6.84 LX2-8 213.721 173.049 156.02 0.837 41.4 2.96 254.4 113.33 1.89 0.731 155.03 8.17 LX3-1 220.110 98.923 124.56 0.464 40.2 2.99 243.4 94.79 1.60 0.725 130.74 6.90 LX3-2 230.152 109.995 169.00 0.494 44.2 4.05 256.0 121.97 2.23 0.748 163.06 8.68 LX3-3 735.832 442.919 466.39 0.622 33.8 1.76 839.9 102.74 1.69 0.678 151.53 7.98 LX3-4 159.371 50.203 80.15 0.486 38.0 2.40 136.0 108.99 1.89 0.712 153.08 8.10 LX3-5 99.963 30.396 86.51 0.325 38.8 2.38 171.2 93.64 1.56 0.72 130.06 6.85 LX3-6 297.526 84.226 46.24 0.314 27.2 0.99 107.1 80.08 1.71 0.613 130.64 7.10 LX3-7 165.490 37.400 177.01 0.293 37.4 2.21 317.3 103.27 1.82 0.71 145.45 7.71 LX3-8 159.371 50.203 86.37 0.234 33.7 1.80 174.3 91.85 2.34 0.681 134.88 7.57 注: Ft为α粒子射出效应的校正参数, 计算方法详见Farley et al. (1996); eU为有效铀浓度, 计算公式为eU=U+0.235×Th (Flowers et al., 2009) 
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