岩石圈动力学过程砂箱物理模拟研究进展

doi:10.11867/j.issn.1001-8166.2023.026

地球科学进展 ›› 2023, Vol. 38 ›› Issue (6): 644 -660. doi: 10.11867/j.issn.1001-8166.2023.026

研究简报上一篇

岩石圈动力学过程砂箱物理模拟研究进展

魏全超 ¹ ^, ²(

), 刘恣君 ², AHMEN Khalid ², 郭虹兵 ², 徐宏远 ², 王恒 ², 邓宾 ² ^, ³(

)

^1.中国石油化工股份有限分公司勘探分公司，四川成都 610000
^2.成都理工大学能源学院，四川成都 610059
^3.成都理工大学“油气藏地质及开发工程”国家重点实验室，四川成都 610059

收稿日期:2022-12-16 修回日期:2023-04-13 出版日期:2023-06-10
通讯作者: 邓宾 E-mail:weiqc.ktnf@sinopec.com;dengbin3000@163.com
基金资助:
四川省科技计划项目“基于地质大数据的四川盆地深部地质结构物理模拟研究”(2022JDRC0001)

A Review on Analog Experiments of Geodynamic Processes

Quanchao WEI ¹ ^, ²( ), Zijun LIU ², Khalid AHMEN ², Hongbing GUO ², Hongyuan XU ², Heng WANG ², Bin DENG ² ^, ³( )

^1.South Exploration and Exploitation Subsidiary Company of Sinopec, Chengdu 610000, China
^2.College of Energy, Chengdu University of Technology, Chengdu 610059, China
^3.State Key Laboratory of Oil and Gas Reservoir Geology and Exploitation, Chengdu University of Technology, Chengdu 610059, China

Received:2022-12-16 Revised:2023-04-13 Online:2023-06-10 Published:2023-06-07
Contact: Bin DENG E-mail:weiqc.ktnf@sinopec.com;dengbin3000@163.com
About author:WEI Quanchao (1981-), male, Liaocheng City, Shandong Province, Engineer. Research areas include sand box analog models and hydrocarbon accumulation. E-mail: weiqc.ktnf@sinopec.com
Supported by:
Scientific and Technological Innovation Talent Program of Sichuan Province “Research on analogue experiments of deep geological structure in Sichuan Basin based on geological big data”(2022JDRC0001)

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自20世纪中叶以来，基于地质构造过程自相似性的砂箱物理模拟实验为岩石圈动力学过程研究提供了独立有效的手段。基于以自然界岩石圈深部变形过程为研究对象的砂箱物理模拟实验研究结果，系统阐述岩石圈动力学变形过程的“自然原型—实验模型”间相似性机理，综述砂箱物理模拟所揭示的岩石圈动力学过程机制与特征，并以坎塔布里亚构造带和扎格罗斯—伊朗高原为实例，对比探讨了岩石圈变形过程与砂箱模拟实验之间的耦合性，以期为同行研究提供参考与借鉴。砂箱物理实验模型与自然原型之间相似性机理，强调二者具有流变学和几何学上非牛顿流体连续介质相似性，才能实现低惯量流动下（Reynolds数Re<<1）动力相似性。砂箱物理模拟实验通常使用干颗粒材料、（非）线性黏性流变学材料、黏弹性材料等构建多层物质结构模型，代表岩石圈双层、三层和四层结构模型。基于砂箱物理模拟实验装置及其实验过程中是否有外部动力和物质等加入，岩石圈动力学砂箱物理模型大致分为3类：系统能量物质守恒的内动力驱动模型、开放系统的外动力驱动模型和内外动力混合驱动模型。砂箱物理模拟研究表明，岩石圈动力学变形过程主要受控于岩石圈多圈层耦合性及其能干性（即弹性强度或黏性刚度）和先存（或继承性）非均质性结构特征，从而控制并影响着浅表盆—山系统变形与整体岩石圈层变形的特征。

关键词: 岩石圈圈层结构, 非均质性, 先存构造, 砂箱物理模型

Since the middle of the 20th century, analog experiments have provided an independent method for studying geodynamic processes. Based on analog experiments, this paper reviews the similarity mechanism between the natural prototype and experimental model of geodynamic processes and reviews the mechanism and characteristics of the lithosphere dynamic process revealed by analog experiments. Furthermore, we compare analog data of the Cantabria Belt and Zagros Iran Plateau. Analog experiments use dry particle materials, (non-) linear viscous rheological materials, and viscoelastic materials to establish multilayer material structure models (i.e., double-, three-, and four-layer lithosphere structures). In general, the analog experimental devices include three types: an internal dynamic drive model of the conservation of the system energy material, external dynamic drive model of the open system, and internal and external dynamic hybrid drive models. Geodynamic deformation of the lithosphere is controlled by the coupling of multiple layers of the lithosphere (i.e., elastic strength or viscous stiffness) and an inherited heterogeneous structure. This controls the deformation of the basin-mountain system in the shallow water and lithosphere. The analog experiment data can provide a better explanation of the geodynamic processes and would play an increasingly important role in tectonic evolution, big-data structure of the basin, and disaster warning.

Key words: Lithospheric structure, Heterogeneity, Inherited structure, Analogue experiment

中图分类号:

P542

图1 典型岩石圈分层模型及全球大陆岩石圈有效弹性厚度（ Te ）特征（据参考文献［ 18 - 19 ］修改）
（a）岩石圈差异应力强度与深度关系图，从左数第一幅图代表岩石圈果冻三明治结构，第二幅图代表岩石圈烤布蕾甜点结构，第三幅图代表岩石圈香蕉船结构；（b）岩石圈中含水等挥发份更易于形成湿的能干性较低的下地壳和地幔岩石圈，从而影响岩石圈强度。黑色线条方向代表 Te各向异性的方向，长度指的是 Te各向异性的大小（ Tmax- Tmin）/（ Tmax+ Tmin），灰色代表低可信度区域

Fig. 1 Mechanical layers of the continental lithosphere and global map of the elastic thickness （modified after references ［18-19］）
（a） Rock strength versus depth for various continental conditions， from left to right they represent jelly sandwich model， crème br?lée model and banana spilt model in sequence；（b） The water in the lithosphere makes it easier to form wet （weak） lower crust and wet （weak） mantle lithosphere，thereby affecting the strength of the lithosphere. The black bars indicate magnitude and direction of Te gradient， the length of black bars is given by the magnitude of Te anisotropy from the ratio （ Tmax- Tmin）/（ Tmax+ Tmin）， grey areas correspond to regions with low reliablity

图2 自然界实例—实验室模型物质应变速率特征对比（据参考文献［ 29 ］修改）

Fig. 2 Comparison of strain rate characteristics between natural examples and analogue models （modified after reference ［ 29 ］）

图3 岩石圈动力学过程的砂箱物理模拟实验多圈层结构模型（据参考文献［ 15 ］修改）
双层和四层岩石圈结构模型分别代表具高地温梯度—高地温场岩石圈特征和低地温梯度—低地温场岩石圈特征，而三层岩石圈结构模型代表二者之间的过渡型

Fig. 3 Simplified models of multi-layered lithospheric structure for analogue experiments of geodynamic processes （modified after reference ［ 15 ］）
The 2-layer and 4-layer lithospheric structural models represent the characteristics of the lithosphere with high temperature gradient-high temperature field and low geothermal gradient-low geothermal field，respectively. Whilst the 3-layer lithospheric structural model represents the transitional type between the two

图4 岩石圈俯冲作用动力学典型砂箱装置（据参考文献［ 39 ， 43 ， 50 - 53 ］修改）
（a）浮力驱动条件下洋陆汇聚碰撞模拟装置及其原理图，上地幔物质由葡萄糖浆构成，上部插图为其基本浮力驱动原理图；（b）浮力驱动下岩石圈俯冲（b ₁）与动力学外动力条件（b ₂）岩石圈俯冲砂箱物理模拟装置对比图；（c）外动力驱动变角度的岩石圈俯冲砂箱物理模拟装置，（c ₁）俯冲带模拟实验几何原理图代表俯冲带中不同类型板块的下沉和地幔流动，下倾下沉板块沿固定轨迹以速率 U_D 运动并驱动地幔楔中的拐角流， U_T 为俯冲后退时板块平移速率， U_R 是 U_D 和 U_T 的向量和，坐标轴显示了板块的对称轴位置；（c ₂）板块俯冲装置组件图（包含模拟地幔的葡萄糖浆）；（d）外动力驱动陆内碰撞变形过程砂箱物理模拟装置图，表示不同地区岩石圈强度特征；（e）外动力沟—弧—盆俯冲碰撞砂箱物理模拟装置图，（e ₁）顶面图，（e ₂）分别为剖面图和岩石圈层温度与应力特征图

Fig. 4 Typical experimental set-ups for the geodynamic lithosphere subduction sandbox modeling （modified after references ［39，43，50-53］）
（a） Experimental apparatus to model ocean-continent convergence and collision driven by buoyancy forces， with glucose syrup used to represent the sublithospheric upper mantle. the upper schematic diagram shows the principle of buoyancy-driven. （b） Three-dimensional laboratory models of upper mantle subduction，（b ₁） buoyancy-driven model，（b ₂） model driven by external approach. （c） Subduction zone geometry and experimental set-up driven by external approach. Diagram illustrating different styles of plate sinking and mantle flow in subduction zones. Downdip sinking involves plate motion along a fixed trajectory at a rate （ U_D ） which drives a corner flow in the mantle wedge．Rollback subduction involves downdip and translational （ U_T ） plate velocities，and drives a mantle return flow from the ocean side of the plate to the wedge. The rollback velocity （ U_R ） is a vector sum of U_D and U_T . The coordinate axes are shown，with the position of the plate’s axis of symmetry（c ₁）. Photograph showing components of the plate subduction apparatus with the tank of glucose syrup that simulates the mantle （c ₂）. （d） Modeling setup of collisional mountain belts driven by the external approach and initial strength variation among modeling domains as shown by strength envelopes （e） Sketch of the experimental set-up with trench-arc-basin subduction system driven by external approach，（e ₁） map-view of the model，（e ₂） cross-section of the model and rheological stratification of the model continental lithosphere

图5 岩石圈圈层耦合/非耦合变形作用特征（据参考文献［ 27 ， 45 ， 63 ， 67 ］修改）
（a）岩石圈纵弯褶皱变形作用分类图，当下地壳为软弱层时上地壳和岩石圈地幔形成不同波长褶皱变形（λ ₁<λ ₂）、深浅部解耦，其余情况下形成单级协调褶皱；（b）多圈层岩石圈结构模型（上下分别为双层和三层结构模型）模拟表明岩石圈低起伏度、长波长纵弯变形作用主要受控于上地壳和岩石圈地幔耦合；（c）岩石圈耦合性与对称性岩石圈变形结构相关性模式，岩石圈圈层耦合性主要取决于应变速率和岩石圈地幔强度

Fig. 5 Coupling and decoupling deformation of the multiply lithoshperical layers （modified after references ［27，45，63，67］）
（a） Sketch of typical folding models， when the lower crust is weak， the upper crust and lithospheric mantle thus form different wavelength folds and deformations（λ ₁ < λ ₂）， thus deep and shallow is decoupled. In other cases， single harmonic folds are formed；（b） Multi-layer model of lithospheric structure （consisting of 2-layer and 3-layer structure model） shows that the low undulation and long wavelength longitudinal bending deformation of the lithosphere， mainly controlled by the coupling of the upper crust and lithospheric mantle；（c） Coupling lithospheric strcutre and the deformation of symmetric lithospheric deformation， and coupling of lithospheric layer depends on strain rate and lithospheric mantle strength

图6 岩石圈深部结构与非均质性变形作用特征（据参考文献［ 47 ， 71 ， 73 ］修改）
（a）非均质性岩石圈板块边界控制岩石圈变形过程与俯冲作用，从上向下依次为垂直均一边界、倾斜非均质性边界和壳—幔解耦下倾斜非均质性边界，其中插图为岩石圈及其红色软弱层结构模型；（b）岩石圈先存构造走向与挤压方向斜度角对其走向结构再活化控制影响性，其中红色SD带表示先存构造带；（c）岩石圈上地幔强度沿走向变化导致洋—陆板块碰撞带走向上俯冲极性反转

Fig. 6 Structures in deep or heterogeneities influence on deformation of the multiply lithoshperical layers （modified after references ［47，71，73］）
（a） Heterogeneous/heterogeneous lithospheric plate boundaries control the deformation process and subduction of the lithosphere. From top to bottom， there are vertical plate boundary， inclined plate boundary and inclined plate boundary under crust-mantle decoupling. The illustration shows a model of the lithosphere and its red weak layer structure. （b） The influence of the inclination angle between the strike and compression directions of pre existing structures in the lithosphere on the reactivation control of their strike structures， with the red SD zone indicating the pre-existing structural zone. （c） Changes in the strength of the upper mantle along the strike in the lithosphere result in reversal of subduction polarity along-strike of the oceanic continental plate collision zone

图7 伊比利亚板内构造带砂箱物理模拟实验对比结果（据参考文献［ 78 ］修改）
（a）伊比利亚板内坎塔布里亚造山带区域位置图；（b）三层岩石圈结构砂箱物理模拟实验边界条件设置；（c）模型A和模型B在体积缩短量为20%时的顶面照片、结构解释图和数字地貌高程图，其中黑色实线为软弱岩石圈模型分界线

Fig. 7 Comparison results of sand box physical simulation experiment of Iberian intraplate structural belt （modified after reference ［ 78 ］）
（a） Tectonics of the Cantabria orocline in Iberian intraplate；（b） Analogue modeling setup of 3-layer lithospheric structure；（c） Top-view images， structural interpretation and digital elevation models show the results of 20% bulk shorteing of Model A and Model B， the black solid line represents the boundary between the weak lithosphere model and the strong lithosphere model

图8 扎格罗斯—伊朗高原砂箱物理模拟实验对比结果（据参考文献［ 77 ］修改）
（a）格罗斯—伊朗高原现今地质结构—构造特征，黑色箭头表示现今阿拉伯板块碰撞挤压方向；（b）双层岩石圈砂箱物理模拟实验边界条件设置；（c）模型演化过程顶面照片及其结构解释图（7%、14%和38%体积缩短量）

Fig. 8 Comparison results of Zagros Iran Plateau sandbox physical simulation experiment （modified after reference ［ 77 ］）
（a） Tectonics of the Zagros-Iranian Plateau， the black arrow indicates direction of convergence of Arabia Plate；（b） Sketch of the experimental apparatus and model construction；（c） Top-view and structural interpretation show the the evolution of experiments （7%，14% and 38% bulk shorteing）

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