Analysis method and product for earth crust equal thickness line-stress field-geological structure

Abstract

The invention relates to the field of earth science, in particular to an analysis method for an earth crust equal-thickness line-stress field-geological structure and a product, the method comprises the steps that a stratigraphic layered structure is determined, a physical parameter model is established, and the layered structure comprises an earth crust layer, a plastic layer and a magma layer; based on the change of the magma density gradient, constructing a magma flow model to analyze the laminar flow characteristic of the magma flow model and the flow velocity distribution of the magma flow model in an earth crust thickness change area; in combination with a regional crustal thickness contour map, stress field distribution of magma flow on different crustal thickness regions and a driving effect of magma flow on fracture structure activity are analyzed, and a dynamic coupling relationship between magma flow and fracture structure activity is obtained; according to the method, an accurate basis can be provided for analyzing the influence of magma flow on the activity of the earth crust structure. A flow model is established based on magma density gradient change, and the flow characteristics and flow velocity distribution characteristics of a magma layer, especially complex flow behaviors in an earth crust thickness change area, are determined.

Description

Technical Field

[0001] The present invention relates to the field of earth science, and in particular to an analysis method and product for crust isopach-stress field-geological structure. Background Art

[0002] The power source and dynamic mechanism of crustal tectonic activity is an important research field in earth science. Its research objects include the movement laws of crustal plates, the flow characteristics of magma layers and their coupling with crustal tectonic activity. Since its proposal, the plate tectonic theory has become the core theory to explain crustal movement and related geological phenomena. This theory is based on physical phenomena such as mantle convection, crustal thickness distribution and magma activity, and establishes a basic framework for describing crustal activity.

[0003] At present, scientists have conducted extensive research on the dynamic characteristics of crustal movement by combining theoretical research with experimental observation. For example, through geophysical detection technologies such as seismic wave propagation characteristics and gravity measurement, the deep structure of the crust and mantle has been studied, providing rich data support for the study of the dynamic mechanism of crustal tectonic activity. In addition, based on the crustal isostatic theory and density gradient model, the distribution law of stress field caused by magma flow has been deeply explored, and combined with regional fault tectonic activities, the regional crustal dynamic behavior has been predicted and analyzed.

[0004] Despite many research results, the dynamic mechanism of crustal tectonic activity remains an unsolved mystery, especially in the coupling effect between magma flow and crustal tectonic activity. Existing research is still insufficient. For example, there is no unified understanding of the impact of thick and thin crust regions on magma flow characteristics, and there is also a lack of systematic description of the distribution and evolution of stress fields in different tectonic units. Therefore, further exploring the mechanism of the impact of magma flow on the distribution of crustal stress fields and fault tectonic activity has important scientific significance and application value. Summary of the invention

[0005] The technical problem to be solved by the present invention is how to accurately analyze the influence of magma flow on crustal tectonic activities and its coupling mechanism, and the purpose is to provide an analysis method and product for crustal isopach-stress field-geological structure, which can fully reveal the relationship between magma flow and regional stress field distribution and fault tectonic activities through hierarchical modeling and quantitative analysis, thereby providing a scientific basis for the prediction of crustal tectonic activities and the prevention and control of geological disasters.

[0006] The present invention is achieved through the following technical solutions:

[0007] An analysis method for crustal isopach-stress field-geological structure, comprising:

[0008] Determine the layered structure of the crust, plastic layer and magma layer, and establish the physical parameter model of each layer;

[0009] Based on the change of magma density gradient, a magma layer flow model is constructed to analyze the laminar flow characteristics of magma and its flow velocity distribution in thick and thin crustal regions;

[0010] Combined with the regional crust thickness contour map, the influence of magma flow on the stress field distribution in different crust thickness regions is analyzed to determine the coupling relationship between magma flow and regional stress field;

[0011] By utilizing the shear stress and normal stress distribution caused by magma flow and combining it with the fault development conditions, we analyze the driving effect of magma flow on fault tectonic activity and determine the relationship between magma flow and fault structure.

[0012] Specifically, establishing the physical parameter model of each layer includes the following steps:

[0013] The stratigraphic structure is determined by geophysical detection methods, and three macroscopic layers are divided in the deep area, including the crust layer, plastic layer and magma layer, and a layered model is established;

[0014] The density gradient model is used to describe the variation of density of each layer with depth, and the Young's modulus, shear modulus and compression modulus of each layer are determined;

[0015] Analyze the viscous shear force transmission mechanism between the magma layer and the plastic layer, and determine the distribution of shear stress and its influence on the deformation of the plastic layer in combination with laminar flow characteristics;

[0016] The friction transmission mechanism between the plastic layer and the crust is analyzed, and the interlayer coupling effect is determined by combining the effect of friction on the driving force of horizontal movement of the crust and stress accumulation.

[0017] Specifically, the method for establishing the magma layer flow model includes:

[0018] Based on crust thickness, temperature and pressure data, a distribution model of magma density changing with depth is established to determine the magnitude and direction of density gradient;

[0019] Based on the spatial distribution of density gradient, the flow area of ​​the magma layer is divided to determine the velocity distribution characteristics of the magma in the area where the thickness of the crust changes, including the flow deceleration behavior in the thickening area and the flow acceleration behavior in the thinning area;

[0020] Through comprehensive analysis of flow direction, velocity distribution and density change, the shear stress generated by magma flow on the plastic layer and its transmission effect in the plastic layer are calculated.

[0021] Specifically, the method for calculating the shear stress generated by magma flow on the plastic layer includes:

[0022] Determine the flow velocity V in the magma layer k, density variation within the layer and viscosity coefficient η k , calculate the viscous shear stress τ in the plastic layer k =f(σ k , V k , η k , ...), σ k is the horizontal stress of the plastic layer;

[0023] Based on the shear stress distribution model and combined with the physical properties of the plastic layer, including Young's modulus and shear modulus, a stress transfer model in the plastic layer is established;

[0024] According to the magma flow characteristics in thick and thin regions of the crust, the shear stress concentration area in the plastic layer and its influence on the crustal stress distribution are analyzed;

[0025] Through the layered analysis method, the transfer effect of shear stress at different depths in the plastic layer is quantified, and its coupling effect on the crust is calculated.

[0026] Specifically, the method for determining the coupling relationship between magma flow and regional stress field includes:

[0027] Obtain the crust thickness contour map, divide the crust thickness variation area in the region, and determine the thickening area, thinning area and the thickness rapid change zone;

[0028] Analyze the velocity distribution characteristics of magma flow in different crustal thickness regions, including the deceleration effect in thickening regions, the acceleration effect in thinning regions, and the flow direction deflection effect in the zone with rapid thickness change;

[0029] Calculate the shear stress and normal stress distribution caused by magma flow in different regions, and establish a regional stress field distribution model based on the regional crust thickness variation characteristics;

[0030] By comparing and analyzing the regional stress field distribution model and the magma flow model, the driving effect of magma flow on the stress field and its coupling relationship are determined.

[0031] Specifically, the magma flow direction is related to the principal stress direction of the regional stress field, which is the resultant direction of the secondary compressive stress induced by the magma flow;

[0032] If the magma flow direction is stable, the principal stress direction is consistent with the direction of earth displacement, and the angle between them is acute; if the flow direction is unstable, the principal stress direction will deviate from the direction of earth displacement.

[0033] Specifically, methods for determining the relationship between magma flow and fault structure include:

[0034] Based on the magma flow model, the distribution of shear stress and normal stress caused by changes in flow direction and velocity in the fault structure area is calculated;

[0035] Combined with the fault development conditions, including the fault surface inclination, shear strength and stress concentration effect, the triggering effect of shear stress and normal stress on fault activity is analyzed;

[0036] Targeting areas with varying crust thickness, identify shear stress concentration zones and normal stress concentration zones, and determine high-risk areas for fault tectonic activity;

[0037] The dynamic coupling relationship between magma flow and fault activity is analyzed to determine the impact of magma flow as a driving source on the fault structural morphology.

[0038] Specifically, the method for analyzing the dynamic coupling relationship between magma flow and fault activity includes: determining the type of surface rupture, including compression fault, strike-slip fault and tension fault, based on shear stress concentration zones and normal stress concentration zones;

[0039] Among them, in the crust thickening area, the normal stress in the area caused by magma flow is concentrated, and the compressive stress increases; the distribution characteristics of the normal stress are analyzed, the stress concentration zone caused by the magma flow is identified, and the location and direction of the surface compression fracture are determined;

[0040] In the area where the magma flow direction is deflected, the shear stress increases; the driving effect of the magma flow velocity difference and direction change on the horizontal displacement of the fault surface is analyzed in combination with the shear stress, and the active area of ​​the strike-slip fault is determined;

[0041] In the area of ​​crust thinning, the magma flow speed increases, the normal stress decreases, and a tensile stress concentration zone is formed; the driving effect of tensile stress on the tensile cracking activity of the fault surface is analyzed to determine the occurrence area and direction of tensile fracture.

[0042] A computer-readable storage medium stores a computer program, which, when executed by a processor, implements the above-mentioned analysis method for crustal isopach lines-stress field-geological structure.

[0043] A computer program product comprises a computer program / instruction, which, when executed by a processor, implements the above-mentioned analysis method for crustal isopach lines-stress field-geological structure.

[0044] Compared with the prior art, the present invention has the following advantages and beneficial effects:

[0045] The present invention determines the stratigraphic layered structure and establishes a physical parameter model through a geophysical detection method. The layered structure includes a crust layer, a plastic layer and a magma layer. Based on the change of the magma density gradient, a magma flow model is constructed to analyze its laminar flow characteristics and the flow velocity distribution in the area where the crust thickness changes. Combined with the regional crust thickness contour map, the stress field distribution of magma flow in different crust thickness areas and its driving effect on fault tectonic activities are analyzed to obtain the dynamic coupling relationship between magma flow and fault tectonic activities.

[0046] The present invention provides an accurate basis for analyzing the impact of magma flow on crustal tectonic activity. The flow model established based on the change of magma density gradient determines the flow characteristics and flow velocity distribution characteristics of the magma layer, especially the complex flow behavior in the area where the crust thickness changes. Combined with the regional crust thickness contour map to analyze the stress field distribution, through the quantitative analysis of shear stress and normal stress, the precise identification of the coupling relationship between magma flow and stress field is achieved, thus providing a scientific basis for predicting high-risk areas of fault tectonic activity.

[0047] In addition, the method of the present invention can also be used to analyze the correlation between geological structure traces, crust thickness contours and geostress fields. By knowing any one condition, such as crust thickness, magma flow or stress distribution, other conditions can be derived and analyzed, thereby providing a scientific basis for geological structure research, crust dynamic monitoring and geostress field distribution prediction. BRIEF DESCRIPTION OF THE DRAWINGS

[0048] The accompanying drawings illustrate exemplary embodiments of the present invention and, together with the description thereof, are used to explain the principles of the present invention. These drawings are included to provide a further understanding of the present invention, and the accompanying drawings are included in and constitute a part of this specification and do not constitute a limitation of the embodiments of the present invention.

[0049] Figure 1 It is a schematic flow chart of an analysis method for crustal isopach lines-stress field-geological structure according to the present invention.

[0050] Figure 2 It is a diagram of an analytical model based on the assumption of the crust surface rupture mechanism described in the present invention.

[0051] Figure 3 It is a schematic diagram of the Mohr-Coulomb compression-shear failure mechanics model according to the present invention.

[0052] Figure 4 It is a schematic diagram of the magma flow model according to the present invention.

[0053] Figure 5 Schematic diagram of the ductile shear model according to the present invention.

[0054] Figure 6This is a contour map of crust thickness of the western Sichuan block according to the present invention.

[0055] Figure 7 This is an analysis diagram of underground magma flow trends in the western Sichuan block according to the present invention.

[0056] Figure 8 This is an analysis diagram of the relationship between magma flow and regional stress field according to the present invention.

[0057] Fig. 9 This is an analysis diagram of the relationship between magma flow and fault activity according to the present invention. DETAILED DESCRIPTION

[0058] To make the purpose, technical solution and advantages of the present invention more clearly understood, the present invention is further described in detail below in conjunction with the accompanying drawings and implementation methods. It is understood that the specific implementation methods described herein are only used to explain the relevant content, rather than to limit the present invention.

[0059] It should also be noted that, for the convenience of description, only the parts related to the present invention are shown in the drawings.

[0060] In the absence of conflict, the embodiments and features of the embodiments of the present invention may be combined with each other. The present invention will be described in detail below with reference to the accompanying drawings and in combination with the embodiments.

[0061] The dynamic sources and dynamic mechanisms of the tectonic activities of the Earth's crust are important research areas in Earth science. The dynamic sources usually refer to the initiation mechanisms and dynamic processes that cause crustal activities, while the dynamic mechanisms describe how these processes occur and their impact on crustal tectonic activities. These studies are not only the key to understanding crustal movement, but also provide a theoretical basis for predicting regional geological activities, and have important scientific and practical significance, such as in the fields of natural disaster assessment, construction site evaluation, and mineral resource exploration.

[0062] At present, plate tectonic theory, as a widely recognized theoretical framework, provides a basic framework for understanding the dynamic mechanism of crustal movement. Relevant research around this theory has made significant progress:

[0063] In terms of theoretical research: in-depth research has been conducted on mantle convection, thermodynamic processes in the earth's interior, ocean-continent interaction, etc., and the concepts of large-system science and interdisciplinary research have been introduced to obtain more information about the earth's deep structure and internal processes, further enriching the theory of plate tectonics.

[0064] In terms of theoretical verification: through geophysical detection technologies such as seismic wave propagation characteristics, gravity measurement of crust and mantle structure, geomagnetic measurement, etc., the scale, speed and direction of crustal movement were obtained. In addition, new technologies (such as synthetic aperture radar, satellite remote sensing) and numerical simulation methods were used to intuitively understand and verify the dynamic mechanisms such as mantle convection and plate interaction.

[0065] In terms of plate dynamics research: the current mainstream views include thrust models (such as the seafloor spreading theory) and pull models (such as the subducting plate drag hypothesis). In addition, the gravity slip self-driven model and the New World Drift theory proposed by Chinese scholars believe that the upwelling of magma behind the continental plate is the main driving force for continental drift.

[0066] Although important progress has been made in the research, due to the complexity of the earth's deep structure and the limitations of detection technology, the study of the crustal power source and dynamic mechanism still faces many challenges, such as the analysis of internal deformation of plates and interaction between plates.

[0067] In summary, since Wegener proposed the theory of continental drift in 1912, the theory of plate tectonics has gradually formed and been widely verified, but there are still many unknown areas in the power source and dynamic mechanism of plate movement. This paper proposes improvements based on the crust equilibrium model and attempts to explain and explore the geological tectonic activities in western Sichuan.

[0068] The crustal isostasy hypothesis is a theoretical model based on the plate tectonic theory to explain the movement of the earth's crust. It believes that the crust is composed of multiple rock plates of different thickness and density. Under the influence of thermal convection inside the earth, the crust moves relative to the asthenosphere of the mantle, which leads to the redistribution of crustal materials and changes in topography. This model can well explain geological phenomena such as plate drift, orogeny and earthquakes, but it also has the following limitations:

[0069] Density difference assumption problem: The density difference setting in the assumption may be unreasonable.

[0070] Limitations of mantle convection models: Current models do not accurately describe mantle convection.

[0071] Insufficient consideration of interlayer interactions: the material exchange and relative interaction between the crust and mantle are ignored.

[0072] Problem of simplified dynamic mechanism: The dynamic mechanism of plate boundaries is simplified, and there is a lack of systematic analysis of the movement within the plates.

[0073] The present invention divides the stratigraphic structure into three macroscopic layers: crustal layer, plastic layer and magma layer. The Young's modulus, shear modulus and compression modulus can be used to characterize the deformation resistance of each layer, and the material form and deformation resistance between these layers and within the layers are all in a gradual state.

[0074] The present invention believes that the plate movement of the crust is the result of deep magma movement (flow): compression shear deformation occurs during the magma flow, and viscosity is generated between the magma layer and the plastic layer → causing ductile shear deformation of the plastic layer, forming a ductile shear zone in the layer, and generating friction on the crust → friction acts on the crust, driving the crust to move horizontally, but because the crust's ability to resist deformation is enhanced, shear stress is formed in the crust. Once it exceeds its shear strength, intralayer rupture occurs.

[0075] The following provides a theoretical basis for the present invention.

[0076] The present invention constructs a layered model of the crust, plastic layer and magma layer to analyze the mechanical coupling between the layers and their impact on the crustal tectonic activity. Through a simplified model of the middle plastic layer, the stress transfer mechanism and rupture effect caused by magma flow are deeply analyzed.

[0077] Stratigraphic stratification and stress analysis: In the plastic layer, magma moves at a speed V k Flow, generating viscous shear stress τ k = x k (σ k , v k , η k ...), where η k represents the viscosity coefficient within the layer. This shear stress is transmitted to the crust through the plastic layer and is associated with the horizontal stress σ1 in the crust. The value of σ1 in the crust can be expressed as σ 1k =λ k (σ 1k , v 1k , η 1k ...).

[0078] When the crust is of uniform thickness, Figure 2 As shown in (1), the viscosity-friction force generated by the magma between layers is τ k1 = x k1 (σ k1 , v k1 , η k1 ...). This force is related to the vertical self-weight normal stress σ 3k =σ 3k (y) is closely related, where y is a function of depth. At this point, the crust can be regarded as a viscoelastic body, and its unit deformation follows the Mohr-Coulomb strength criterion, such as Figure 3 shown.

[0079] When the crust thickness increases, Figure 2 As shown in (2), the magma flow velocity V1 decreases. In the horizontal direction, the velocity component V x The upper crustal layer produces a large shear stress; in the vertical direction, the velocity component Vx Increasing the value of the environmental normal stress σ1 can easily lead to stress concentration, thereby accelerating the formation of thrust fractures.

[0080] When the crust thickness decreases, Figure 2 (3) shows that the magma flow velocity V1 increases. In the horizontal direction, the velocity component V x The shear stress on the upper crust is more significant, which is likely to cause the formation of normal faults; but the vertical velocity component V x The decrease in the value of the environmental normal stress σ1 reduces the possibility of thrust fracture.

[0081] Therefore, by taking the crust thickness as a reference, magma flows usually from thick to thin areas. However, its fault pattern shows the following characteristics: thrust faults mainly appear in the sharp change zone from thin to thick. Normal faults are concentrated in the central area of ​​the dome from thick to thin, such as Figure 4 shown.

[0082] like Figure 5 As shown, the crust, plastic layer and magma layer are further divided into multiple microscopic layers. The deformation modulus of each layer has a functional relationship with the depth y, including the following expressions: Young's modulus: Shear modulus: Compression modulus: Deformation distance L of each layer k With vertical stress σ1, horizontal stress σ3, viscous shear stress τ k+1 The relationship between and modulus can be expressed as the following function:

[0083] When deep magma flows, compression and shear deformation will occur over a long distance, and this deformation will gradually be transmitted to the semi-liquid and semi-solid area of ​​the upper layer, forming ductile shear deformation. As the deformation is transmitted, the deformation range gradually shrinks, and the stress gradually concentrates. When the accumulated stress exceeds the shear strength of the crust, the crust will be sheared.

[0084] From the profile, the entire deformation area shows an obvious triangular distribution. The deformation range and intensity are closely related to the following factors: stress state (σ1, σ3), rock mass (or magma) density, layer material state (liquid, semi-liquid semi-solid, solid), shear stress τ transmitted from the lower layer k+1 , deformation modulus, burial depth

[0085] The movement of deep magma is flow, which is driven by changes in the magma density gradient: magma with a certain density gradient in a flowing state deep in the earth is produced by melting caused by high pressure and has a tendency to move to a low-pressure state, thus causing flow.

[0086] The layers from the crust to the mantle are not 2 or 3 relatively uniform density zones, but should be gradual zones with a certain density gradient formed under the gradually increasing surrounding rock pressure, and the temperature gradually increases. Theoretically, when the confining pressure is large enough to exceed the melting point of the material, the material will turn into a liquid state. Of course, the liquid at this time is very different from the molten liquid state under high temperature and normal pressure. Its density is greater than that of the solid state, and its state is unstable. It has a clear trend of developing towards a state with lower density and smaller confining pressure. Therefore, it has the natural property of moving towards the dome position with thinner crust thickness. This is the main driving mechanism for magma flow and also the internal driving mechanism of magma flow. This mechanism can form a theoretical closed loop with the inference in the previous article, which can also explain why geophysical detection has found that the thickness of the crust is constantly changing.

[0087] The movement of magma is driven by "flow potential": that is, when it flows from a high-density (high confining pressure) area to a low-density (low confining pressure) area, the density will decrease and the speed will increase due to the change in confining pressure during the flow process. This is the main drive; on the contrary, the density increases and the speed decreases, which is the passive drive; its flow performance is laminar. Therefore, the density gradient from the crust to the mantle is constant, but the density at the same depth is constantly changing, so the value of the density gradient is changing, and as long as there is a density gradient, the "flow potential" will exist, and the flow of magma will proceed spontaneously.

[0088] Embodiment 1

[0089] like Figure 1 As shown, a method for analyzing crustal isopach lines-stress field-geological structure is provided, comprising:

[0090] The layered structure of the crust, plastic layer and magma layer is determined by geophysical detection methods, and a physical parameter model of each layer is established; this model includes parameters such as Young's modulus, shear modulus, compression modulus, etc., which are used to describe the deformation resistance and mechanical properties of each layer.

[0091] Based on the change of magma density gradient, the flow behavior of deep magma in different crustal thickness areas is analyzed, a magma layer flow model is constructed, and the flow velocity distribution of deceleration in crust thickening areas and acceleration in crust thinning areas is calculated.

[0092] Combined with the regional crust thickness contour map, the shear stress and normal stress distribution caused by magma flow are used to analyze the impact of magma flow on the stress field distribution in different crustal thickness regions, and the coupling relationship between magma flow and regional stress field is determined; by studying the stress concentration phenomenon in crust thickening and thinning areas, the coupling relationship between magma flow and regional stress field is determined.

[0093] By utilizing the distribution of shear stress and normal stress caused by magma flow and combining it with fault development conditions (such as fault surface inclination, shear strength, etc.), we analyze the driving effect of magma flow on fault tectonic activity. By quantifying the concentration areas of shear stress and normal stress, we determine the high-risk fault activity areas and the relationship between magma flow and fault structure.

[0094] Embodiment 2

[0095] The establishment of the physical parameter model of each layer includes the following steps:

[0096] The stratigraphic structure is determined by geophysical detection methods, and three macroscopic layers are divided in the deep area, including the crust layer, plastic layer and magma layer, to establish a layered model; the crust layer is a rigid geological structure of the surface layer. The plastic layer is between the crust and the magma layer and has strong toughness and plasticity. The magma layer is composed of high-temperature molten material and has fluidity.

[0097] The density gradient model is used to describe the change of density of each layer with depth, and the Young's modulus, shear modulus and compression modulus of each layer are determined; Young's modulus is the ability of each layer to resist tensile deformation. The shear modulus is the resistance of each layer to shear deformation. The compression modulus is the resistance of each layer to volume deformation. The density distribution from the crust to the mantle increases with depth, and the confining pressure causes the density of the material to gradually increase, but the density gradient varies with the properties of the material. The deep temperature increases with depth, which may induce the transition of solid rock to liquid. Theoretical analysis shows that when the confining pressure exceeds the melting point pressure, the material will transform into a high-density liquid, and the density gradient changes significantly.

[0098] The viscous shear force transmission mechanism between the magma layer and the plastic layer is analyzed, and the distribution of shear stress and its influence on the deformation of the plastic layer are determined in combination with the laminar flow characteristics; the shear force is transmitted to the plastic layer layer by layer, causing local ductile shear deformation and accumulating stress in the shear zone. The distribution of shear stress affects the deformation range and strength of the plastic layer.

[0099] The friction transmission mechanism between the plastic layer and the crust is analyzed, and the interlayer coupling effect is determined by combining the effect of friction on the driving force of horizontal movement of the crust and stress accumulation. The friction transmitted from the plastic layer to the crust forms the main driving force of horizontal movement of the crust. Under the action of friction, the shear stress inside the crust gradually accumulates. When the stress exceeds the shear strength of the crust, it will cause local rupture of the crust, which manifests as fault activity or crustal movement.

[0100] The method for establishing the magma layer flow model comprises:

[0101] Based on the crust thickness, temperature and pressure data, a distribution model of magma density changing with depth is established to determine the size and direction of the density gradient; the melting of deep magma due to high pressure presents a non-uniform density distribution, and its gradient change is controlled by the confining pressure, temperature and magma composition. The local difference in density gradient in the area where the crust thickness changes directly affects the flow direction and speed. By establishing a distribution model, the trend of high-density areas flowing to low-density areas is clarified, and this trend is the basis of the "flow potential" driving mechanism.

[0102] Based on the spatial distribution of density gradient, the flow area of ​​the magma layer is divided, and the velocity distribution characteristics of the magma in the area where the crust thickness changes are determined, including the flow deceleration behavior in the thickening area and the flow acceleration behavior in the thinning area; in the thickening area of ​​the crust, the magma flow velocity decreases, showing flow retardation characteristics. In the thinning area of ​​the crust, the magma flow velocity is significantly accelerated due to the reduction of confining pressure. The flow direction tends to the area with small density gradient, showing accelerated flow. In complex crustal morphology, such as dome or trough area, magma flow shows local velocity changes and direction deflection.

[0103] Through comprehensive analysis of flow direction, velocity distribution and density changes, the shear stress generated by magma flow on the plastic layer and its transmission effect in the plastic layer are calculated. The flow of the magma layer produces a ductile shear zone in the plastic layer, and the shear stress concentration area becomes the main path for stress transmission. The shear stress is gradually transmitted to the crust along the interlayer, affecting its deformation mode and rupture mechanism. Especially in the thickening or thinning areas of the crust, the transmission characteristics of shear stress play a key role in the distribution of crustal stress. The density gradient and flow velocity field are combined to calculate the shear stress size and its change law in different depths and regions, and establish a stress distribution model.

[0104] Methods for calculating the shear stress caused by magma flow on the plastic layer include:

[0105] Determine the flow velocity V in the magma layer k , density variation within the layer and viscosity coefficient η k , calculate the viscous shear stress τ in the plastic layer k =f(σ k , V k , η k , ...), σ k is the horizontal stress of the plastic layer; the flow velocity of the magma layer varies with depth and is affected by the density gradient and pressure field. The density of the magma is non-uniformly distributed due to changes in confining pressure and temperature, showing a gradient characteristic. The viscosity coefficient characterizes the rheological properties of the magma, and its value depends on the material composition and environmental conditions.

[0106] Based on the distribution model of shear stress and combined with the physical properties of the plastic layer, including Young's modulus and shear modulus, a stress transfer model within the plastic layer is established; that is, a model is established to describe the transfer law of shear stress within the layer and its influence on the deformation within the layer. The model can combine density gradient and flow characteristics to clarify the action range and concentration area of shear stress.

[0107] According to the magma flow characteristics in the thick and thin regions of the earth's crust, analyze the shear stress concentration area within the plastic layer and its influence on the crustal stress distribution; in the thickening area, due to the decrease in flow velocity and the increase in normal stress, the shear stress concentration is more significant and has a stronger impact on the crustal thickness. In the thinning area, due to the acceleration of the flow velocity, the action range of shear stress expands, but the concentration degree is weaker.

[0108] Through the hierarchical analysis method, quantify the transfer effect of shear stress at different depths within the plastic layer and calculate its coupling effect on the crustal layer. It is transferred from the magma layer to the plastic layer and then conducted to the crustal layer. During the transfer process, the deformation range shrinks, but the stress gradually concentrates. After the shear stress is transferred to the crustal layer, it causes changes in the crustal stress distribution and may trigger regional fracture activities.

[0109] As Figure 6 and Figure 7 shown, referring to the geographical parameters in western Sichuan, the methods for determining the coupling relationship between magma flow and the regional stress field include:

[0110] Obtain the isopach map of the crustal thickness and divide the thick and thin change regions of the crust within the region to determine the thickening areas, such as some island-shaped or belt-shaped thickening zones, such as the areas west of Mao Ribar and Barkam, with a thickness change range of several kilometers to more than ten kilometers. The thinning areas, such as the trough zones and dome areas in the western Sichuan block, with a thickness change range of several kilometers to more than ten kilometers. The areas with sharp thick and thin changes, such as the areas where the "乀"-shaped resistance lines are located, and these change zones are important areas for the deflection of the magma flow direction.

[0111] Analyze the flow velocity distribution characteristics of magma flow in different thick and thin regions of the crust, including the deceleration effect in the thickening area, the acceleration effect in the thinning area, and the flow direction deflection effect in the areas with sharp thick and thin changes; the deceleration effect in the thickening area: due to the increase in normal stress, the magma flow velocity decreases. This effect is particularly significant in the thickening area from Daofu to Qianning, resulting in a slowdown in flow. The acceleration effect in the thinning area: the decrease in confining pressure leads to an increase in the magma flow velocity, which is commonly seen in trough areas such as from Mount Emei to Leshan. The deflection effect in the areas with sharp thick and thin changes: in these areas, the magma flow direction deflects due to changes in the stress field, such as the flow trend in the area from Daofu to Shimian.

[0112] The shear stress and normal stress distribution caused by magma flow in different regions are calculated, and the regional stress field distribution model is established in combination with the regional crust thickness variation characteristics; Normal stress: Due to the compression effect of magma flow, the normal stress is concentrated in the thickening area, which manifests as a higher crust deformation capacity. The stress calculation results show that the stress distribution is directly related to the thick and thin regional characteristics, and is quantified through regional specific models.

[0113] By comparing the regional stress field distribution model with the magma flow model, the driving effect of magma flow on the stress field and its coupling relationship are determined. By comparing the magma flow model with the regional stress field distribution model, the driving effect of magma flow on the stress field is clarified:

[0114] The direction of magma flow is related to the direction of the principal stress in the regional stress field, which is the direction of the resultant force of the secondary compressive stress caused by magma flow;

[0115] If the magma flow direction is stable, the principal stress direction is consistent with the direction of earth displacement, and the angle between them is acute; if the flow direction is unstable, the principal stress direction will deviate from the direction of earth displacement.

[0116] Methods for determining the relationship between magma flow and fault structure include:

[0117] Based on the magma flow model, the distribution of shear stress and normal stress in the fault structure area caused by changes in flow direction and velocity is calculated; changes in magma flow velocity lead to shear stress concentration in the plastic layer and fault zone. For example, in the thinning crust area, flow acceleration increases shear stress; in the thickening crust area, due to the deceleration and compression of magma flow, the normal stress increases significantly, resulting in strong deformation in the fault structure area.

[0118] Combined with the fault development conditions, including the fracture surface inclination, shear strength and stress concentration effect, the triggering effect of shear stress and normal stress on fault activity is analyzed; the fracture surface inclination is based on the fracture inclination in the area where the crust thickness changes, and the influence of stress distribution on the fracture extension direction is judged. Shear strength is to evaluate the maximum shear stress on the fracture surface and infer its rupture possibility. The stress concentration effect focuses on analyzing how the shear stress concentration zone affects the intensity of fault activity. For example, the shear concentration in the Kowloon area leads to the development of L-shaped fractures.

[0119] For areas with varying thickness of the crust, identify shear stress concentration zones and normal stress concentration zones, and determine high-risk areas for fault tectonic activity; thrust faults in thickening areas, for example, the crust thickening area from Kangding to Jiulong is characterized by thrust fault concentration zones. Normal faults in thinning areas, for example, the crust thinning area from Wawushan to Leshan is often characterized by normal faults.

[0120] The dynamic coupling relationship between magma flow and fault activity is analyzed to determine the impact of magma flow as a driving source on the fault structural morphology.

[0121] Methods for analyzing the dynamic coupling relationship between magma flow and fault activity include: determining the type of surface ruptures based on shear stress concentration zones and normal stress concentration zones, including compression faults, strike-slip faults and tension faults; compression faults are caused by the increase in normal stress in the thickened crust area, which induces compression faults. Strike-slip faults are caused by magma flow in areas with significant shear stress, such as the central area of ​​the "Y"-shaped structure. Tension faults are caused by stress release and tension effects in areas of thinned crust.

[0122] Among them, in the crust thickening area, the normal stress in the area caused by magma flow is concentrated, and the compressive stress increases; the distribution characteristics of the normal stress are analyzed, the stress concentration zone caused by the magma flow is identified, and the location and direction of the surface compression fracture are determined;

[0123] In the area where the magma flow direction is deflected, the shear stress increases; the driving effect of the magma flow velocity difference and direction change on the horizontal displacement of the fault surface is analyzed in combination with the shear stress, and the active area of ​​the strike-slip fault is determined;

[0124] In the area of ​​crust thinning, the magma flow speed increases, the normal stress decreases, and a tensile stress concentration zone is formed; the driving effect of tensile stress on the tensile cracking activity of the fault surface is analyzed to determine the occurrence area and direction of tensile fracture.

[0125] Embodiment 3

[0126] like Figure 6 and Figure 7 , this embodiment provides a specific example.

[0127] According to the crust thickness contour lines of Liu Yufa et al. ( Figure 6 ), the crust thickness is the largest and island-shaped to the west of Xinlong, with a depth of 70km, and gradually thins to about 40km toward the southeast, and the thickness is uneven in different places:

[0128] (1) Three islands protruding toward the center of the earth appeared in Maoriba to the west of Xiaojin and Maerkang, in the northeast of Maerkang, and between Jiulong County and Shade Township. A belt-like thickening area appeared in Ganluo, Jinyang and Dashanbao Scenic Area, with an increase of about 4 km, 3 km, 5 km, and 12 km respectively. The major axis trends were approximately N22°W, N72°E, S41°E, and SN, and the lengths were approximately 70 km, 130 km, 50 km, and 215 km respectively.

[0129] (2) In the area from Xiaojin to Baoxing and Mofanggou, from the northeast of Daocheng to Aden and Yalongjiang Town, from Mianning southward to Jinhe Township, and from Xichang to Panzhihua, as well as from Wawushan to Leshan, Meishan, Qionglai, and Ya'an, there are 4 crustal thinning areas in the shape of an inverted trough and an inverted dustpan. The thinning thickness values are approximately 8 km, 2 km, 10 km, and 12 km respectively. The directions of the dustpan mouths are S44°E, S55°E turning to S23°E, S7°W, and N47°E turning to N76°E respectively. The ratios of their long axes to short axes are approximately 100 / 56 km, 150 / 52 km, ≥160 / 200 km, and ≥200 / 75 km respectively.

[0130] (3) In the area from Yajiang to Zituoxi Township, Xinlong County, there is a domed crustal thinning area with a scale of approximately 99 km × 86 km and a thinning value of approximately 4 km.

[0131] (4) Northeast of Daofu to Qianning (Huiyuan Temple), a crustal thickening zone appears faintly. The crust is thinning in the areas from Luding to Shimian and from Mianning.

[0132] According to the method of the present invention, combined with Figure 6 the following results can be obtained as Figure 7 shown:

[0133] (1) The crustal thickness gradually thins from the northwest to the southeast. Therefore, the overall flow direction is consistent with this, and most of it is an acceleration area (shown by the dark arrows).

[0134] (2) There is a large-scale resistance line in the NW-SE direction in the region, with a width of approximately 50 - 150 km, forming a "乀"-shaped area where the magma flow rate decreases (shown by the light arrows). The location starts from the northwest of Maoriba, northwest of the region, extends to Daofu, Kangding, and then to the line of Shimian, Yuexi, Jinyang, and Dashanbao. The reason is that there is an oval crustal thickening from Daofu to the northeast of Qianning, and the rate of crustal thinning slows down and the gradient decreases in the areas from Luding to Shimian, Yuexi, and Mianning, and there is a dumbbell-shaped crustal thickening from Yuexi to Zhaojue and from Jinyang to Dashanbao.

[0135] (3) There are small areas with reduced flow rates locally: ① The island-shaped crustal thickening from Shade Township to Jiulong forms a resistance line; ② In the areas from Xiaojin to Baoxing and Mofanggou, from the northeast of Daocheng to Aden and Yalongjiang Town, and in the trough zones of the 4 inverted trough-shaped and inverted dustpan-shaped crustal thinning areas from Wawushan to Leshan, Meishan, Qionglai, and Ya'an, the rate of crustal thinning slows down and the gradient decreases, forming a resistance line.

[0136] (4) There are relatively stable areas locally: ① Northwest of the line from Barkam to the northeast of Maoriba, Kangding, Jiulong, Muli, and Yanyuan, the gradient change of the crustal thickness is small, and the magma flow is relatively stable. Southeast of this line, the gradient increases significantly, and the magma flow rate increases significantly; ② The domed area of crustal thinning from Yajiang to Zituoxi Township, Xinlong County, is small in scale and small in thinning value, and is also a relatively stable area for magma activity.

[0137] The relationship between magma flow and regional stress field is determined as follows:

[0138] Depend on Figure 7 It can be seen that the direction of the regional stress field is consistent with the direction of the GPS earth displacement in general, but there are large differences in some parts, while the difference between the direction of magma flow and the direction of GPS earth displacement is much smaller, and the overall pattern is as follows:

[0139] (1) In the area from Maerkang to the northeast of Maoriba, Kangding, Jiulong, Muli, and Yanyuan, where the crust thickness gradient changes little, the direction of the regional stress field and the direction of GPS ground displacement show a high degree of consistency. Only in the northwest of the circular crust thickening zone from Jiulong to Shade Township, their directions show obvious differences in deflection (see Figure 8 of point).

[0140] (2) Although the crust thickness changes greatly in the southeast of the line, the direction of the regional stress field and the direction of GPS earth displacement show a high degree of consistency within the range of uniform gradient changes. There are mainly three small categories that show obvious differences: ① The second-order derivative stationary point range of the crust thickness gradient, that is, the area with small changes in the process of drastic gradient changes → small changes → drastic changes, such as Figure 8 shown ② In the crustal thinning area of ​​inverted trough, inverted dustpan, and wide and gentle dome, the range with small gradient change on the top and both sides, such as Figure 8 shown point; ③ the back side of the island crust thickening area in the direction of magma flow, such as Figure 8 shown Furthermore, if the magma flow direction in the region is stable, the angle between the principal stress direction and the earth displacement direction is acute and consistent with the overall flow direction, such as Figure 8 shown points, etc. If the flow direction is unstable, the angle is unstable, and the angle between the principal stress direction and the earth displacement direction is unstable, such as Figure 8 shown Wait a minute.

[0141] In summary, there is a close relationship between the direction of magma flow and regional stress field and the direction of GPS ground displacement. It is preliminarily inferred that the direction of regional principal stress is the direction of the resultant force of secondary compressive stress generated by flow, and the direction of ground displacement is the direction of the resultant vector of flow direction.

[0142] The relationship between magma flow and fault structure is determined as follows:

[0143] Due to the depth and shape of the earth's crust, the rate and direction of magma movement have certain regularities. Its reflection to the surface causes surface displacement and stress accumulation, which in turn leads to surface ruptures that also have good regularity.

[0144] (1) There is a blocking zone in the north of Maoriba and Luhuo to Daofu and Kangding in the south. Because there is an invisible island-shaped thickening area in front of the flow, it is easy to accumulate high ground stress. The reflection on the surface shows compression and strike-slip characteristics, and the strike-slip is the main one. The mechanical model is compression-shear. There is also a blocking zone in the Shimian, Yuexi, Zhaojue and Dashanbao areas, but they are generally in a resistance reduction area. The crust thickness gradient changes slowly and evenly, which is not conducive to stress accumulation. The reflection on the surface shows compression and strike-slip characteristics, and the compression is the main one. The mechanical model is also compression-shear.

[0145] (2) The entire area from Baoxing, Lushan to Maoxian is in a zone of reduced resistance. However, due to the change in crust thickness gradient and the trend of convergence to Chengdu, Chengdu is a large dome area, which is an invisible blocking area. In addition, the Xiaojin trough-type crust thinning area leads to accelerated flow on both sides. Therefore, the region shows obvious compression, the strike-slip feature is not obvious, which is conducive to the accumulation of high ground stress, and the surface rupture has obvious thrust characteristics; from Baoxing west to Dachuan Town, due to the intersection of magma flow trends, it is slightly extended, and the mechanical model is tension, but it is not conducive to stress accumulation. There is a slight compression from Dachuan Town to Dujiangyan, but the stress accumulation is limited. The section with high stress accumulation and rapid development is located in the northeast area of ​​Dujiangyan.

[0146] (3) The area south of Mianning and Xichang shows obvious extensional and left-lateral strike-slip characteristics, the mechanical mode is shear, and the accumulation of ground stress is limited.

[0147] (4) The Muli area has strong compression characteristics. The Muli to Mianning West and Muli to Daocheng South show shear-slip characteristics. The mechanical mode is compression and compression-shear, which are conducive to the accumulation of higher ground stress. The Litang to Muli area is located at the edge of the Yajiang dome and the Jiulong island-shaped thickening area, with little influence and is not conducive to stress accumulation. The surface rupture shows left-lateral strike-slip characteristics.

[0148] (5) Due to the existence of the Jiulong island-like thickening zone, the flow rate in the northwest decreases and the flow rate in the southeast increases. There is an obvious compression zone in Shade that can accumulate higher stress, and the surface rupture is a thrust. There is an obvious tensile stress accumulation zone in Jiulong County and the northwest. In addition, due to the effects of the Yajiang dome and the Kangding invisible blocking zone, higher stress can be accumulated west of Kangding. The mechanical mode is mainly compression-shear, and the surface rupture is mainly strike-slip with thrust characteristics. The area around Jiulong County is mainly tensile, manifested as a normal fault. The two phases are connected to form a peculiar "L"-shaped fault that developed simultaneously. Similar mechanisms also exist in the fault structures of Muli-Yanyuan and Baoxing.

[0149] (6) The central part of the Y-shaped structure in western Sichuan (Luding to Shimian area) exhibits shear compression characteristics and is also the boundary between the northern strike-slip compression fault and the southern strike-slip fault.

[0150] In summary, magma flow is closely related to regional fault tectonic activities and is the driving force of fault tectonic activities. The surface rupture characteristics and rupture mechanisms of faults can be explained by geomechanical mechanisms.

[0151] Embodiment 4

[0152] A computer-readable storage medium stores a computer program, which, when executed by a processor, implements the above-mentioned analysis method for crustal isopach lines-stress field-geological structure.

[0153] Without loss of generality, computer readable media may include computer storage media and communication media. Computer storage media include volatile and non-volatile, removable and non-removable media implemented in any method or technology for storing information such as computer readable instruction data structures, program modules or other data. Computer storage media include RAM, ROM, EPROM, EEPROM, flash memory or other solid-state storage technology, CD-ROM, DVD or other optical storage, cassettes, magnetic tapes, disk storage or other magnetic storage devices. Of course, those skilled in the art will appreciate that computer storage media are not limited to the above. The above-mentioned system memory and mass storage devices can be collectively referred to as memory.

[0154] A computer program product comprises a computer program / instruction, which, when executed by a processor, implements the above-mentioned analysis method for crustal isopach lines-stress field-geological structure.

[0155] A computer program product includes a computer program or set of instructions for performing specific tasks or implementing specific functions. These programs or instructions are designed to be executed by a processor to implement a series of predefined steps or operations. The program product may be stored in various forms of computer storage media, such as memory, hard disk, solid-state drive, optical disk or other forms of digital storage devices. It may exist in the form of compiled binary code or in the form of scripts or bytecodes that can be executed by an interpreter. The program product uses carefully designed algorithms and logical instructions to enable the processor to process data in a specific order and manner to complete various functions such as data analysis, user interaction, device control, etc.

[0156] In the description of this specification, the description with reference to the terms "one embodiment / method", "some embodiments / methods", "example", "specific example", or "some examples" etc. means that the specific features, structures, materials or characteristics described in conjunction with the embodiment / method or example are included in at least one embodiment / method or example of the present application. In this specification, the schematic representations of the above terms do not necessarily refer to the same embodiment / method or example. Moreover, the specific features, structures, materials or characteristics described may be combined in any one or more embodiments / methods or examples in a suitable manner. In addition, those skilled in the art may combine and combine the different embodiments / methods or examples described in this specification and the features of the different embodiments / methods or examples, unless they are contradictory.

[0157] In addition, the terms "first" and "second" are used for descriptive purposes only and should not be understood as indicating or implying relative importance or implicitly indicating the number of the indicated technical features. Therefore, the features defined as "first" and "second" may explicitly or implicitly include at least one of the features. In the description of this application, the meaning of "plurality" is at least two, such as two, three, etc., unless otherwise clearly and specifically defined.

[0158] It should be understood by those skilled in the art that the above embodiments are only for the purpose of clearly illustrating the present invention, and are not intended to limit the scope of the present invention. For those skilled in the art, other changes or modifications may be made based on the above invention, and these changes or modifications are still within the scope of the present invention.

Claims

1. An analysis method for crustal isopach-stress field-geological structure, characterized in that: include: Determine the layered structure of the crust, plastic layer and magma layer, and establish the physical parameter model of each layer; Based on the change of magma density gradient, a magma layer flow model is constructed to analyze the laminar flow characteristics of magma and its flow velocity distribution in thick and thin crustal regions; Combined with the regional crust thickness contour map, the influence of magma flow on the stress field distribution in different crust thickness regions is analyzed to determine the coupling relationship between magma flow and regional stress field; By utilizing the shear stress and normal stress distribution caused by magma flow and combining it with the fault development conditions, we analyze the driving effect of magma flow on fault tectonic activity and determine the relationship between magma flow and fault structure.

2. The method for analyzing crustal isopach-stress field-geological structure according to claim 1, characterized in that: The establishment of the physical parameter model of each layer includes the following steps: The stratigraphic structure is determined by geophysical detection methods, and three macroscopic layers are divided in the deep area, including the crust layer, plastic layer and magma layer, and a layered model is established; The density gradient model is used to describe the variation of density of each layer with depth, and the Young's modulus, shear modulus and compression modulus of each layer are determined; Analyze the viscous shear force transmission mechanism between the magma layer and the plastic layer, and determine the distribution of shear stress and its influence on the deformation of the plastic layer in combination with laminar flow characteristics; The friction transmission mechanism between the plastic layer and the crust is analyzed, and the interlayer coupling effect is determined by combining the effect of friction on the driving force of horizontal movement of the crust and stress accumulation.

3. The method for analyzing crustal isopach-stress field-geological structure according to claim 1, characterized in that: The method for establishing the magma layer flow model comprises: Based on crust thickness, temperature and pressure data, a distribution model of magma density changing with depth is established to determine the magnitude and direction of density gradient; Based on the spatial distribution of density gradient, the flow area of ​​the magma layer is divided to determine the velocity distribution characteristics of the magma in the area where the thickness of the crust changes, including the flow deceleration behavior in the thickening area and the flow acceleration behavior in the thinning area; Through comprehensive analysis of flow direction, velocity distribution and density change, the shear stress generated by magma flow on the plastic layer and its transmission effect in the plastic layer are calculated.

4. The method for analyzing crustal isopach-stress field-geological structure according to claim 3, characterized in that: Methods for calculating the shear stress caused by magma flow on the plastic layer include: Determine the flow velocity V in the magma layer k , density variation within the layer and viscosity coefficient η k , calculate the viscous shear stress τ in the plastic layer k =f(σ k , V k , η k , ...), σ k is the horizontal stress of the plastic layer; Based on the shear stress distribution model and combined with the physical properties of the plastic layer, including Young's modulus and shear modulus, a stress transfer model in the plastic layer is established; According to the magma flow characteristics in thick and thin regions of the crust, the shear stress concentration area in the plastic layer and its influence on the crustal stress distribution are analyzed; Through the layered analysis method, the transfer effect of shear stress at different depths in the plastic layer is quantified, and its coupling effect on the crust is calculated.

5. The method for analyzing crustal isopach-stress field-geological structure according to claim 1, characterized in that: Methods for determining the coupling relationship between magma flow and regional stress field include: Obtain the crust thickness contour map, divide the crust thickness variation area in the region, and determine the thickening area, thinning area and the thickness rapid change zone; Analyze the velocity distribution characteristics of magma flow in different crustal thickness regions, including the deceleration effect in thickening regions, the acceleration effect in thinning regions, and the flow direction deflection effect in the zone with rapid thickness change; Calculate the shear stress and normal stress distribution caused by magma flow in different regions, and establish a regional stress field distribution model based on the regional crust thickness variation characteristics; By comparing and analyzing the regional stress field distribution model and the magma flow model, the driving effect of magma flow on the stress field and its coupling relationship are determined.

6. The method for analyzing crustal isopach-stress field-geological structure according to claim 5, characterized in that: The direction of magma flow is related to the direction of the principal stress in the regional stress field, which is the direction of the resultant force of the secondary compressive stress caused by magma flow; If the magma flow direction is stable, the principal stress direction is consistent with the direction of earth displacement, and the angle between them is acute; if the flow direction is unstable, the principal stress direction will deviate from the direction of earth displacement.

7. The method for analyzing crustal isopach-stress field-geological structure according to claim 1, characterized in that: Methods for determining the relationship between magma flow and fault structure include: Based on the magma flow model, the distribution of shear stress and normal stress caused by changes in flow direction and velocity in the fault structure area is calculated; Combined with the fault development conditions, including the fault surface inclination, shear strength and stress concentration effect, the triggering effect of shear stress and normal stress on fault activity is analyzed; Targeting areas with varying crust thickness, identify shear stress concentration zones and normal stress concentration zones, and determine high-risk areas for fault tectonic activity; The dynamic coupling relationship between magma flow and fault activity is analyzed to determine the impact of magma flow as a driving source on the fault structural morphology.

8. The method for analyzing crustal isopach-stress field-geological structure according to claim 7, characterized in that: Methods for analyzing the dynamic coupling relationship between magma flow and fault activity include: determining the types of surface ruptures, including compression faults, strike-slip faults, and tension faults, based on shear stress concentration zones and normal stress concentration zones; Among them, in the crust thickening area, the normal stress in the area caused by magma flow is concentrated, and the compressive stress increases; the distribution characteristics of the normal stress are analyzed, the stress concentration zone caused by the magma flow is identified, and the location and direction of the surface compression fracture are determined; In the area where the magma flow direction is deflected, the shear stress increases; the driving effect of the magma flow velocity difference and direction change on the horizontal displacement of the fault surface is analyzed in combination with the shear stress, and the active area of ​​the strike-slip fault is determined; In the area of ​​crust thinning, the magma flow speed increases, the normal stress decreases, and a tensile stress concentration zone is formed; the driving effect of tensile stress on the tensile cracking activity of the fault surface is analyzed to determine the occurrence area and direction of tensile fracture.

9. A computer-readable storage medium storing a computer program, characterized in that: When the computer program is executed by a processor, an analysis method for crustal isopachs-stress field-geological structure as described in any one of claims 1 to 8 is implemented.

10. A computer program product comprising a computer program / instructions, characterized in that When the computer program / instruction is executed by a processor, an analysis method for crustal isopach lines-stress field-geological structure as described in any one of claims 1 to 8 is implemented.

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