阅读说明：本技术 一种地壳三维结构模型融合方法及装置 (Method and device for fusing three-dimensional structure models of earth crust ) 是由 李卫东 赵晨曦 单新建 王亚兵 张定文 董前林 刘甲 吴峥嵘 时春波 于 2020-06-05 设计创作，主要内容包括：本发明提供一种地壳三维结构模型融合方法及装置,属于地球物理领域。该方法包括：在参与融合的多个地壳三维结构模型的重合区域上统一各模型的结构；在深度方向上将重合区域分成多个地层,使每个地层上结构统一后的各模型的物性参数均呈线性关系；结合协同克里金方法,以及每个地层上各模型内部的自协方差函数、各模型间的互协方差函数和各模型的权重比,得到相应地层的融合矩阵；求解每个地层的融合矩阵得到相应地层上结构统一后的各模型对应的最优加权系数矩阵；结合最优加权系数矩阵计算每个地层上所有点融合后的物性参数,得到重合区域上所有点融合后的物性参数,完成模型融合。本发明能消除各模型之间的结构差异和保留各模型原有的地质特征。(The invention provides a method and a device for fusing a three-dimensional structure model of a ground shell, and belongs to the field of geophysical. The method comprises the following steps: unifying the structure of each model on the superposition area of the plurality of crustal three-dimensional structure models participating in fusion; dividing the overlapping area into a plurality of stratums in the depth direction, so that the physical property parameters of the models with unified structures on each stratum are in a linear relation; combining a collaborative kriging method, and an autocovariance function inside each model on each stratum, a cross covariance function among the models and a weight ratio of each model to obtain a fusion matrix of the corresponding stratum; solving the fusion matrix of each stratum to obtain an optimal weighting coefficient matrix corresponding to each model with unified structure on the corresponding stratum; and calculating the physical parameters after all the points on each stratum are fused by combining the optimal weighting coefficient matrix to obtain the physical parameters after all the points on the overlapped area are fused, thereby completing model fusion. The invention can eliminate the structural difference among the models and keep the original geological characteristics of the models.)

1. A method for fusing three-dimensional structure models of the earth crust is characterized by comprising the following steps:

(1) unifying the structure of each model on the overlapped area of the plurality of crustal three-dimensional structure models participating in fusion, including unifying the physical property parameters of each model and the resolution of each model;

(2) dividing the overlapping area into a plurality of stratums in the depth direction, so that physical parameters of all models with unified structures on each stratum are in a linear relation;

(3) the method comprises the following steps of constructing a fusion matrix in a layering mode based on a collaborative kriging method, wherein the process of processing each model with a unified structure on a certain stratum to obtain the fusion matrix of the stratum comprises the following steps:

taking the three-dimensional variation function of each model on the stratum as an autocovariance function inside each model on the stratum;

constructing a cross covariance function between the models on the stratum according to the linear relation of the physical property parameters of the models on the stratum and the auto covariance function inside the models;

determining the weight ratio of each model on the stratum according to the linear relation of the physical property parameters of each model on the stratum;

combining a collaborative kriging method, and an autocovariance function inside each model, a cross covariance function among each model and a weight ratio of each model on the stratum to obtain a fusion matrix of the stratum;

(4) solving the fusion matrix of each stratum to obtain an optimal weighting coefficient matrix corresponding to each model with unified structure on the corresponding stratum; and aiming at any point on each stratum, obtaining the physical parameters after the point fusion according to the physical parameters of different models corresponding to the point, the points in the point neighborhood and the optimal weighting coefficients of different models corresponding to the points in the point neighborhood, thereby obtaining the physical parameters after the point fusion on all the corresponding stratums, further obtaining the physical parameters after the point fusion on all the coincident areas, and finishing the model fusion.

2. The method for fusing the three-dimensional structure model of the earth crust as recited in claim 1, wherein the fusion matrix of a certain stratum is:

in the formula, λ₁，λ₂Respectively are the optimal weighting coefficient matrixes corresponding to the model U and the model V, gamma represents the linear relation between the model U and the model V,

3. The method for fusing the three-dimensional structure models of the earth crust according to claim 1 or 2, characterized in that the power function models are respectively fitted to the three-axis variation functions of the x-axis, the y-axis and the z-axis of each model with unified structure on a certain stratum, and then the three-axis variation functions of each model are registered by adopting an anisotropic registration method to obtain the three-dimensional variation functions of each model on the stratum.

4. The method for fusing the three-dimensional structure model of the earth crust according to claim 3, wherein the three-dimensional variation function is: gamma ray^*(h)＝γ₁(h)+γ₀(|Ah|)-γ₁(| Ah |), where h is the sample point spacing, γ₁(h) As a function of variation in the horizontal direction, gamma₀(|Ah|)-γ₁(| Ah |) is a vertical direction variation function, A is a distance transformation matrix, and gamma^*(h) Is the three-dimensional variation function.

5. The method for fusing the crustal three-dimensional structure model according to claim 1 or 2, wherein the physical parameters of the models after the structures are unified are P-wave velocity or S-wave velocity or density.

6. The method according to claim 5, wherein when the physical property parameter of each model after the structure unification is a P-wave velocity, the physical property parameter of each model is unified into a P-wave velocity by using a transverse-longitudinal-wave empirical relationship and a velocity-density empirical relationship, wherein the transverse-longitudinal-wave empirical relationship is:

the empirical speed-density relationship is:

in the formula, v_pIs P wave velocity, v_sIs the S-wave velocity and ρ is the density.

7. An earth-crust three-dimensional structure model fusion device, characterized in that the device comprises a processor and a memory, wherein the processor executes a computer program stored by the memory to realize the earth-crust three-dimensional structure model fusion method according to any one of claims 1-6.

Technical Field

The invention relates to a method and a device for fusing a three-dimensional structure model of a ground shell, belonging to the technical field of geophysical.

Background

With the increase of research on the three-dimensional structure models of the earth crust in different regions of the world, the construction of the unified earth crust structure model is researched, so that the splicing and integration of the region earth crust structures are realized, the geological interpretation accuracy is further improved, and the three-dimensional physical property structure model with the region integrity is provided for interpreting the deep earth crust structure, and the important significance is achieved. However, each crust three-dimensional structure model is an optimal solution obtained based on a limited constraint condition, the model has a multi-solution problem, and structural difference problems (differences in resolution, depth and attribute among models) exist among different crust three-dimensional structure models obtained by different methods, and the research of the crust structure and the construction of the unified crust structure model are limited by the factors.

At present, the proposal of a multisource heterogeneous gravity and seismic model data fusion research method mainly depends on the research of different physical property empirical relations and the development of a gravity and seismic data joint inversion method.

In The study of density-velocity physical relationship, Birch, Ludwig, Gardner, Von Sharpe and Christensen et al, through theoretical and experimental measurements, proposed a number of density-velocity equations for different conditions (see The following documents: Birch Journal of geographic Research, Vol.66, No. 7, published as The vertical compositional resources in batches to 10 kits, Vol.2, Birch, Del Searesearch & Oceographic extracts, Vol.17, Vol.3, published as The mantle Trench Weluzon Trough travel-III, Seismic-recovery measures; Gardner, Gerdner, Germin, Vol.39, Vol.6, Vol.5, published as The three-dimensional seismic density distribution, Vol.2, published as The seismic density distribution in 1974, Vol.39, Vol.2, published as The seismic density-seismic inversion results, Vol.2, Vol.3, a publication of Poisson's ratio and commercial segregation). Brocher et al comparatively analyze the applicable conditions of various density-Elastic wave velocity relationships and give a formula for the conversion of longitudinal and transverse waves of the Crust suitable for various conditions (see the following literature: Brocher in 2005 Bulletin of the semiconductor Society of America, volume 95, No. 6, published under the name of Empirical Relations between Elastic waves and density in the Earth's Crust), which provides a uniform basis for the properties of model fusion.

In the aspect of joint Inversion, the geophysical Inversion constrained by a Geostatistical method integrates prior knowledge into a collaborative kriging matrix, and can effectively improve the accuracy of Inversion results (for example, an Inversion matrix constructed by Ashi in 2000 Proceedings of the 6th International geostations Congress-geostat2000. Marshall: geostationary Association of South Africa, a document published by Direct of geographic Data by Cokriging; Shamsour in 2010 Geophariscs No. 75 No. 1, a document published by 3D storage investment of geographic Data by Inversion and Cooperation; a document published by geotrichour in geomatics No. 73, a document published by 3D storage investment of geographic Data by Cokriging and Cokriging; a document published by geotrichour in 2010 Geosus No. 4, a document published by 3D storage of geographic Data by geometrics No. 3, a document published by geometrics No. 4, a document published by 3D of geographic Data by Cokriging, a document published by Massach in 2011, a document published by 3D 5, the disclosed document is a document for gravity gradient full-tensor three-dimensional constraint inversion based on a collaborative kriging method; the high-tech cranes, in 2017, volume 47, 2 of the university of Jilin school newspaper (geoscience edition), disclose a document with the name of determining the dip tendency of the dikes through three-dimensional inversion of gravity gradient data and Cokrikin; high-show cranes in 2019, volume 62, 3 of geophysical press, published as literature for joint inversion of gravity and gravity gradient data by the cokriging method based on threshold constraints). However, the construction of these inversion matrices is expected and known as an assumption, and when the problem of uniform expression of the superposition region of the multi-source heterogeneous three-dimensional structure model is solved, the inversion matrices cannot be added with the constraint conditions of the correlations of different models, and cannot be fused with the geological features of different crustal structure models.

In conclusion, when multi-source heterogeneous crustal three-dimensional structure models are fused, how to eliminate the structural difference among the models and simultaneously keep the original geological features of the models is still a problem to be solved.

Disclosure of Invention

The invention aims to provide a method and a device for fusing crustal three-dimensional structure models, which are used for solving the problems that structural differences among models cannot be eliminated and original geological features of the models cannot be reserved simultaneously when the crustal three-dimensional structure models are fused at present.

In order to achieve the above object, the present invention provides a method for fusing three-dimensional structural models of the earth crust, which comprises the following steps:

(1) unifying the structure of each model on the overlapped area of the plurality of crustal three-dimensional structure models participating in fusion, including unifying the physical property parameters of each model and the resolution of each model;

(2) dividing the overlapping area into a plurality of stratums in the depth direction, so that physical parameters of all models with unified structures on each stratum are in a linear relation;

(3) the method comprises the following steps of constructing a fusion matrix in a layering mode based on a collaborative kriging method, wherein the process of processing each model with a unified structure on a certain stratum to obtain the fusion matrix of the stratum comprises the following steps:

taking the three-dimensional variation function of each model on the stratum as an autocovariance function inside each model on the stratum;

constructing a cross covariance function between the models on the stratum according to the linear relation of the physical property parameters of the models on the stratum and the auto covariance function inside the models;

determining the weight ratio of each model on the stratum according to the linear relation of the physical property parameters of each model on the stratum;

combining a collaborative kriging method, and an autocovariance function inside each model, a cross covariance function among each model and a weight ratio of each model on the stratum to obtain a fusion matrix of the stratum;

(4) solving the fusion matrix of each stratum to obtain an optimal weighting coefficient matrix corresponding to each model with unified structure on the corresponding stratum; and aiming at any point on each stratum, obtaining the physical parameters after the point fusion according to the physical parameters of different models corresponding to the point, the points in the point neighborhood and the optimal weighting coefficients of different models corresponding to the points in the point neighborhood, thereby obtaining the physical parameters after the point fusion on all the corresponding stratums, further obtaining the physical parameters after the point fusion on all the coincident areas, and finishing the model fusion.

The invention also provides a device for fusing the three-dimensional structure model of the earth crust, which comprises a processor and a memory, wherein the processor executes a computer program stored by the memory to realize the method for fusing the three-dimensional structure model of the earth crust.

The method and the device for fusing the crustal three-dimensional structure model have the advantages that: firstly, unifying the structures of all models in a superposition area to eliminate the structural difference among the models; secondly, dividing the overlapping area into a plurality of stratums in the depth direction, wherein the layering principle is to ensure that physical parameters of all models with unified structures on each stratum are in a linear relation so as to meet the requirement of a second-order stationary hypothesis and improve the reliability of model fusion; then, a fusion matrix is constructed in a layering mode based on a collaborative kriging method, since the autocovariance function inside each model reflects the autocorrelation among data inside each model, the autocovariance function and the obtained linear relation are used for constraining the cross covariance function, the precision of the cross covariance function can be improved while the original priori knowledge of each model is kept, and therefore the autocovariance function inside each model and the cross covariance function among each model are added into the fusion matrix, and the original geological characteristics of each model can be kept; the weight ratio of each model reflects the correlation among the models, so that the correlation among different model geological features can be reflected by adding the weight ratio of each model into the fusion matrix; and finally, solving the physical property parameters after all points on the overlapped area are fused to complete model fusion. In conclusion, the invention can not only eliminate the structural difference among the models, but also keep the original geological characteristics of the models and reflect the correlation among the geological characteristics of different models.

Further, in the above method and apparatus for fusing three-dimensional structure models of the earth crust, the fusion matrix of a certain stratum is:

in the formula, λ₁，λ₂Respectively are the optimal weighting coefficient matrixes corresponding to the model U and the model V, gamma represents the linear relation between the model U and the model V,is the weight ratio of the model U,

weight ratio for model V, cov (u)_k,u_j) As an autocovariance function of model U, cov (v)_k,v_j) Autocovariance function for model V, cov (u)_k,v_j) As a cross-covariance function between model U and model V, cov (V_k,u_j) As a cross-covariance function between model V and model U,

u_kphysical property parameter U of model U corresponding to point k_jRepresenting the physical property parameters of the model U corresponding to the j point in the neighborhood of the point k, n representing the total number of the points in the neighborhood of the point k, v_kA physical property parameter, V, of a model V corresponding to a point k_jWithin the neighborhood of the representation point kThe physical property parameter u of the model V corresponding to the j-th point of (1)_oA physical property parameter v representing the model U corresponding to the point o_oThe physical property parameter, μ, of the model V corresponding to the point o₁、μ₂Is the lagrangian parameter for constructing the fusion matrix.

Further, in the method and the device for fusing the three-dimensional structure models of the earth crust, the variation functions of the models with unified structures in the three axial directions of the x axis, the y axis and the z axis are respectively fitted on a certain stratum by using the power function model, and then the variation functions of the models in the three axial directions are registered by adopting an anisotropic registration method to obtain the three-dimensional variation functions of the models on the stratum.

Further, in the above method and apparatus for fusing crustal three-dimensional structure models, the three-dimensional variation function is: gamma ray^*(h)＝γ₁(h)+γ₀(|Ah|)-γ₁(| Ah |), where h is the sample point spacing, γ₁(h) As a function of variation in the horizontal direction, gamma₀(|Ah|)-γ₁(| Ah |) is a vertical direction variation function, A is a distance transformation matrix, and gamma^*(h) Is the three-dimensional variation function.

Further, in the method and the apparatus for fusing three-dimensional structure models of the earth crust, the physical parameters of the models with unified structures are P-wave velocity or S-wave velocity or density.

Further, in the above method and apparatus for fusing three-dimensional structure models of the earth crust, when the physical property parameter of each model after the structure unification is a P-wave velocity, the physical property parameter of each model is unified into the P-wave velocity by using a transverse-longitudinal wave empirical relation and a velocity-density empirical relation, the transverse-longitudinal wave empirical relation being:

the empirical speed-density relationship is:

in the formula, v_pIs P wave velocity, v_sIs the S-wave velocity and ρ is the density.

Drawings

FIG. 1 is a flow chart of a method for fusing three-dimensional earth crust structural models according to an embodiment of the method of the present invention;

FIG. 2 is a plot of a Shanxi fault zone in the middle of the Claritong section of North China in an embodiment of the method of the present invention;

FIG. 3-a is a linear relationship diagram of east and west models obtained by performing linear relationship fitting at a depth of 0km to 1.4km in the method embodiment of the present invention;

FIG. 3-b is a linear relationship diagram of east and west models obtained by performing linear relationship fitting at a depth of 1.4km to 15km in the method embodiment of the present invention;

FIG. 3-c is a linear relationship diagram of east and west models obtained by performing linear relationship fitting at a depth of 15km to 39km in the method embodiment of the present invention;

FIG. 3d is a linear relationship diagram of east and west models obtained by fitting linear relationships at a depth of 39km to 50km in the method embodiment of the present invention;

FIG. 4-a is a model diagram of the three-dimensional P-wave velocity structure of the earth's crust at the coincidence region of the east model in an embodiment of the method of the present invention;

FIG. 4-b is a diagram of a three-dimensional structure of P-wave velocity of the crust of the western model in the coincidence region according to an embodiment of the method of the present invention;

FIG. 4-c is a structural model diagram of the three-dimensional P-wave velocity of the crust of the Krige model in the coincidence region in the embodiment of the method of the invention;

FIG. 4-d is a diagram of a three-dimensional P-wave velocity structure of the earth's crust at the coincidence region of the G model in an embodiment of the method of the present invention;

FIG. 5-a is a diagram of a Western model of the location of the section of NCISP4 in an embodiment of the method of the invention;

FIG. 5-b is a diagram of an east model of the cross-sectional location of NCISP4 in a method embodiment of the invention;

FIG. 5-c is a Krige model of the cross-sectional position of NCISP4 in an embodiment of the method of the present invention;

FIG. 5-d is a G-model diagram of the cross-sectional location of NCISP4 in an embodiment of the method of the invention;

FIG. 6-a is a diagram of an east model of a Wednen-Alaran cross-sectional position in an embodiment of the method of the invention;

FIG. 6-b is a diagram of a western model of the location of the West Denton-Alaran section in an embodiment of the method of the invention;

FIG. 6-c is a Krige model of the location of the Wednen-Alaran section in an embodiment of the method of the present invention;

FIG. 6-d is a G-model of the location of the Wednen-Alaran profile in an embodiment of the method of the invention;

FIG. 7-a is a diagram of an east model of the Yancheng-Baotou cross-sectional location in an embodiment of the method of the present invention;

FIG. 7-b is a diagram of a Western model of the saline town-toe cut location in an embodiment of the method of the present invention;

FIG. 7-c is a Krige model of the location of the halochen-baotou cross-section in an embodiment of the method of the invention;

FIG. 7-d is a G-model of the salt city-toe cross-sectional position in an embodiment of the method of the present invention;

FIG. 8-a is a diagram of an east model with the east model cut away at the position of section BB' in an embodiment of the method of the present invention;

FIG. 8-b is a diagram of a western model with the east model cut away at the position of section BB' in accordance with an embodiment of the method of the present invention;

FIG. 8-c is a Krige model of the east model taken at the position of section BB' in accordance with an embodiment of the method of the present invention;

FIG. 8-d is a G model view of the east model at the position of cut-away section BB' in an embodiment of the method of the present invention;

FIG. 9 is a block diagram of a device for fusing three-dimensional earth crust models in an embodiment of the device of the present invention.

Detailed Description

Method embodiment

The method for fusing three-dimensional structure models of the crust according to this embodiment is shown in fig. 1, and the following describes in detail the process of fusing three-dimensional structure models of the crust using this method, taking 2 three-dimensional structure models of the crust (hereinafter referred to as a model U and a model V) participating in the fusion as an example, and specifically as follows:

step 1, unifying the structures of the model U and the model V in the overlapped area of the model U and the model V, including unifying the physical parameters and the resolution of the model U and the model V.

Because the structural difference problem exists between different crustal three-dimensional structure models obtained by different methods, the structural difference between the models can be eliminated by using the step, and a foundation is laid for the later model fusion.

The crust three-dimensional structure model obtained and constructed based on the forward and inverse methods mainly comprises structure models of P-wave velocity, S-wave velocity and density, and some models already give converted P-wave velocity structure models in the inverse result, so in the embodiment, the P-wave velocity is selected as a unified physical property parameter, the physical property parameters of the model U and the model V are unified into the P-wave velocity by using a transverse-longitudinal wave empirical relation and a velocity-density empirical relation, and the resolutions of the model U and the model V are unified by using an interpolation method.

The transverse and longitudinal wave empirical relation is as follows:

the empirical speed-density relationship is:

in the formula, v_pIs P wave velocity, v_sIs the S-wave velocity and ρ is the density.

In another embodiment, the physical property parameters may be unified into S-wave velocity or density by selecting a physical property relationship empirical formula.

And 2, dividing a superposed region of the model U and the model V into a plurality of strata in the depth direction, so that the P wave velocities of the model U and the model V on each stratum are in a linear relationship.

Because the geophysical field of the overlapped region has homology, in order to meet the second-order stationary assumption, the overlapped regions of different models are subjected to deep layering treatment, so that each model on each stratum meets the normal distribution assumption, and the reliability of model fusion can be improved.

Theoretically, the same stratum in the crust structure has spatial consistency, so that the difference existing at the same position of different crust three-dimensional structure models can be expressed by using a linear relation:

u＝γ·v (3)

in the formula, U is the P-wave velocity of the model U, V is the P-wave velocity of the model V, and γ represents the linear relationship between the model U and the model V.

And 3, constructing a fusion matrix in a layering manner based on a collaborative kriging method.

The process of obtaining the fusion matrix of the stratum by processing the model U and the model V with unified structures on a certain stratum is as follows:

(1) respectively constructing autocovariance functions inside the model U and the model V on the stratum;

in this embodiment, considering that the three-dimensional structure model of the earth crust has anisotropy, determining three main axis directions (i.e., three axial directions of an x axis, a y axis, and a z axis) of the earth crust based on the strike of the earth crust, then fitting the three axial variation functions of the x axis, the y axis, and the z axis of the model U with a power function model, respectively, and finally fitting the three axial variation functions of the model U with an anisotropic fit method to obtain a three-dimensional variation function of the model U on the earth crust, and taking the three-dimensional variation function of the model U on the earth crust as an autocovariance function inside the model U; similarly, the three-dimensional variation function of the model V on the formation can be obtained similarly, and the three-dimensional variation function of the model V on the formation is used as the autocovariance function inside the model V.

The calculation method of the variation function in each axial direction and the three-dimensional variation function is as follows:

because the size of the area occupied by the crust structure model is large, the crust fusion takes the seismic wave P wave velocity as an attribute, and the change of the stratum velocity difference is generally less than 0.2km/s, a power function model (formula A1) is adopted as a unified model for calculating the variation function in the embodiment, a least square method is adopted for fitting the variation function model, and the precision of the fitting function is verified by the verification of the variation coefficient.

γ(h)＝scale*h^exponet+nugget (A1)

In the formula, scale is a coefficient of proportionality of the variation function, exponet is a coefficient of exponential of the variation function, nugget is a value of the block gold of the variation function, and h is a distance between two sample points.

The method for registering the x, y and z triaxial variogram adopts anisotropic registration, and the method characterizes the variogram in the horizontal directionAs isotropic features gamma in three-dimensional space₁(| h |), fitting a variation function γ in the entire three-dimensional space^*(h) Is in the vertical direction at gamma₂(h_z) And (4) nesting in each horizontal direction. The three-dimensional variation function obtained after the registration is shown as formula A2:

γ^*(h)＝γ₁(h)+γ₀(|Ah|)-γ₁(|Ah|) (A2)

where h is the sample point spacing, γ₁(h) As a function of variation in the horizontal direction, gamma₀(|Ah|)-γ₁(| Ah |) is a vertical direction variation function, A is a distance transformation matrix, and gamma^*(h) Is a three-dimensional variation function obtained after registration.

Because the variation function can quantitatively express and analyze the spatial autocorrelation of the sample data, the autocorrelation among the data in the model can be embodied by taking the three-dimensional variation function as the autocovariance function in the model, so that the original geological characteristics of the model can be embodied.

(2) Constructing a cross covariance function between the model U and the model V on the stratum;

and constructing a cross covariance function between the model U and the model V according to the linear relation of the P wave velocities of the model U and the model V on the stratum and the autocovariance functions inside the model U and the model V, wherein the method specifically comprises the following steps:

if the P-wave velocities of the model U and the model V have a linear relationship as shown in equation (3), the auto-covariance function and the cross-covariance function have the following relationship:

cov(u_k,v_j)＝γ·cov(u_k,u_j) (4)

wherein, cov (u)_k,u_j) Is a dieAutocovariance function of type U, cov (U)_k,v_j) Is a cross covariance function between model U and model V.

In this embodiment, when calculating the cross-covariance function between model U and model V at point o on the formation, the cross-covariance function cov at point o is calculated (U)_o,v_k) And cov (v)_o,u_k) The deformation is performed, adding model U, model V auto-covariance function cov at point o (U₀,u_k) And cov (v)₀,v_k) Therefore, the prior knowledge of the original model is utilized to constrain the cross covariance function between the models so as to retain the original geological characteristics of each model and improve the precision of the cross covariance function. The deformation is as follows:

(3) determining the weight ratio of the model U and the model V on the stratum;

in the embodiment, the weight ratio of the model U to the model V is determined according to the linear relation of the P wave velocities of the model U and the model V on the stratum; if the P wave velocities of the model U and the model V on the stratum have a linear relationship as shown in formula (3), the weight ratio of the model U is

The weight ratio of the model V is

(4) And combining a collaborative kriging method, and an autocovariance function inside the model U and the model V, a cross covariance function of the model U and the model V and a weight ratio of the model U and the model V on the stratum to obtain a fusion matrix of the stratum.

In the embodiment, the difference of the earth crust structure models obtained by different forward and inverse methods on the three-dimensional space distribution of the stratum depth and the geological features is consideredAdding an autocovariance function inside the model U and the model V and a cross-covariance function between the model U and the model V into a fusion matrix in order to keep original geological characteristics of the model U and the model V after the models are fused; in addition, in order to reflect the correlation between the model U and the model V after the models are fused, the weight ratio of the model U and the model V is taken as a constraint condition and added into a fusion matrix, and on the basis, the fusion matrix of a certain stratum finally obtained by combining a collaborative kriging method is as follows:

in the formula, λ₁，λ₂Respectively are the optimal weighting coefficient matrixes corresponding to the model U and the model V, gamma represents the linear relation between the model U and the model V,is the weight ratio of the model U,weight ratio for model V, cov (u)_k,u_j) As an autocovariance function of model U, cov (v)_k,v_j) Autocovariance function for model V, cov (u)_k,v_j) As a cross-covariance function between model U and model V, cov (V_k,u_j) As a cross-covariance function between model V and model U,

u_kp-wave velocity, U, of model U corresponding to point k_jRepresenting the P wave velocity of the model U corresponding to the j point in the neighborhood of the point k, n representing the total number of points in the neighborhood of the point k, v_kP-wave velocity, V, of model V representing point k_jRepresents the P-wave velocity, u, of the model V corresponding to the j-th point in the neighborhood of point k_oP-wave velocity, v, of model U corresponding to point o_oP-wave velocity, μ, of model V corresponding to point o₁、μ₂Is the lagrangian parameter for constructing the fusion matrix.

Step 4, solving the fusion matrix of each stratum to obtain an optimal weighting coefficient matrix corresponding to each model with unified structure on the corresponding stratum; and aiming at any point on each stratum, obtaining the P wave velocity after point fusion according to the P wave velocity of the point, different models corresponding to the points in the point neighborhood and the optimal weighting coefficient of the different models corresponding to the points in the point neighborhood, thus obtaining the P wave velocity after the point fusion on all the corresponding stratums, further obtaining the P wave velocity after the point fusion on all the coincident areas, and finishing model fusion (namely obtaining a final fusion model).

For example, the calculation process of the P-wave velocity after the point o fusion on a certain stratum is as follows:

solving the fusion matrix of the stratum to obtain the optimal weighting coefficient matrix corresponding to each model with unified structure on the stratum, namely the optimal weighting coefficient matrix lambda corresponding to the model U and the model V₁、λ₂；

And obtaining the P wave velocity after the point o is fused according to the P wave velocities of the different models (namely, the model U and the model V) corresponding to the points in the neighborhood of the point o and the optimal weighting coefficients of the different models (namely, the model U and the model V) corresponding to the points in the neighborhood of the point o.

When 3 models participate in the fusion, two models are randomly selected to be fused according to the method of the embodiment to obtain a new model, and then the obtained new model and the rest models are fused according to the method of the embodiment to obtain the final fusion model. When the number of models participating in the fusion is greater than 3, the fusion process is similar to the above and is not described in detail.

Next, an experiment is performed based on actual data, and the validity of the three-dimensional structure model fusion method of the crust (hereinafter referred to as the method of the present embodiment) of the present embodiment is verified by using a statistical evaluation method and an actually measured profile evaluation method, respectively.

Validation experiment based on statistical evaluation method:

taking the Shanxi fault band region in the middle of the Claritong in North China as shown in FIG. 2 as an example, a unified crustal three-dimensional P-wave velocity structure model of a research area is constructed by using the method of the embodiment, and a simple fusion model is constructed by introducing a weighted average method as a comparison model. The verification method uses the root mean square error and pearson correlation coefficient.

The method is characterized in that a model fusion experiment is carried out on two crustal three-dimensional structure models obtained from Shanxi fault trap areas in the middle of the Ke Tong in North China, and the three-dimensional crustal speed structure models participating in model fusion comprise: constructing a three-dimensional P-wave velocity structure model of the east crusta of the North China Claritong by using a Krige interpolation method; and obtaining a three-dimensional S-wave velocity structure model of the western crust of North China Claton by using a receiving function method, wherein the S-wave velocity structure model gives the converted P-wave velocity. In practical inspection, because the three-dimensional earth crust structure model has a large scale and contains a large number of geological structure characteristics, the problem that the data of the superposed region is difficult to conform to the second-order stationary assumption and the problem that the variation function is difficult to fit are solved by directly extracting and fusing the data of the superposed region, so that the superposed region needs to be partitioned according to the main geological structure of the superposed region, and the Shanxi fault band is taken as the main geological structure characteristic of the region to extract the data to be fused of the corresponding model.

The three-dimensional P-wave velocity structure model of east crust in Karitong province of North China (hereinafter referred to as east model) has a resolution of 0.25 DEG.times.0.25 DEG.times.1 km at a depth of 10km and a resolution of 0.25 DEG.times.0.25 DEG.times.2 km at a depth of 10km to 50 km. The resolution of the western hull three-dimensional S-wave velocity structure model (hereinafter referred to as the western model) of north China caranton is 0.2 ° × 0.2 ° × 0.2km at a depth of 7km, and 0.2 ° × 0.2 ° × 1km at a depth of 7km to 50 km. The P-wave velocity structure hierarchy given by the East Model and the West Model is shown in Table 1, wherein East Model is the East Model, West Model is the West Model, and the main strata comprise sedimentary deposit (segment), Upper Crust (Upper Crust), Middle Crust (Middle Crust), lower Crust (Lowercrust), Crust transition zone (Crust-mantle transition zone) and rock ring Crust (lithosphere).

TABLE 1 east and west models for each principal formation P-wave velocity

In the embodiment, the longitude range of 112 degrees to 113 degrees and the latitude range of 36 degrees to 42 degrees are selected as the region to be fused (see the dashed-line frame region in fig. 2), and the main geologic structure characteristics of the region are mainly the Shanxi fault zone. And taking the western model grid with higher resolution as a model grid to be fused, interpolating the east model by using an IDW (inverse distance weighted interpolation) method, unifying the resolution of each model, and finally obtaining the layered speed structure of the east model and the western model.

To satisfy the second order stationary assumption, the model was layered with a depth of 0km to 1.4km, a depth of 1.4km to 15km, a depth of 15km to 39km, and a depth of 39km to 50km, respectively. And selecting main P wave velocity characteristics of each layer to perform normal test to obtain the maximum number of sample points, and uniformly extracting the coordinates of the sample points containing the P wave velocity attribute of each layer. As the geological features of the basin and the earth in the region are in the northeast direction, the variable feature direction of the region is defined as [1,1,1], the three main axis directions of a region coordinate system are [1,0,0], [0,1,0], [0,0,1] respectively, the x, y and z triaxial variation functions are fitted by a power function model, and the final three-dimensional variation function is obtained by using a registration method.

When defining the relation of the fusion model, hierarchically fitting the linear relation of the stratum corresponding to each model, calculating a cross covariance function, finally constructing a fusion matrix based on a collaborative kriging method, performing neighborhood point search and matrix solution on each point, and acquiring a unified crustal three-dimensional P-wave velocity structure model (namely, the fusion model obtained by the method of the embodiment) of the research area. Wherein, the east and west model linear relations obtained by fitting the linear relations according to the depths of 0km-1.4km, 1.4km-15km, 15km-39km and 39km-50km are respectively shown in figure 3-a, figure 3-b, figure 3-c and figure 3-d.

At the time of analytical verification, a G model is added for comparative analysis. The G model takes the linear relation between the east model and the west model as a weight coefficient, the velocities of all points are weighted and summed, and the proportion of the east model and the west model is

And

fig. 4-a to 4-d are comparison diagrams of the three-dimensional crustal P-wave velocity structure model of the model participating in fusion and the fusion model in the overlapping region, wherein the east model and the west model are the models participating in fusion, the Krige model represents the fusion model obtained by the method of the present embodiment, and the G model represents the fusion model obtained by the weighting method. As can be seen from fig. 4-a to 4-d, the P-wave velocities of the east and west models have peaks at 5.5km/s or less, 6km/s, 6.5km/s and 7.5km/s, so that the east and west models can be divided into four stratal structures conforming to the second-order stationary assumption, i.e., a sedimentary layer, an upper crust, a lower crust and an upper mantle, and the final Krige model and G model obtained by the method of the present embodiment and the weighting method also conform to the four-layer structure.

The model accuracy evaluation employed Root Mean Square Error (RMSE)) and Pearson correlation coefficient as evaluation indexes, and tables 2 and 3 are the values of RMSE and Pearson coefficient between the comparative analysis results and the respective models.

TABLE 2 respective stratum RMSE

The east model and the west model are different models of the crustal velocity structure of the overlapping region obtained by different methods, and as can be seen from table 2, the root mean square error of the models is 0.342, and the error is large. The root mean square error of the fused Krige model is less than 0.3 for both east and west models, and only rises in depth error of 16km-39km, so that the Krige model can approximately meet the expression of east and west models, the root mean square error of the G model is less than 0.2, and the accuracy degree is higher than that of the Krige model.

TABLE 3 Pearson coefficients for the various strata

The Pearson correlation coefficient in table 3 is the correlation analysis of each model after layering. Before the fusion, the correlation between the east and west models was greater than 0.7 only at 39km-50 km. After fusion, the correlation between the Krige model and the east model is remarkably improved, and the correlation of the G model, which is a fusion model obtained by the east model and the west model by using a weighted average method, is higher than that of the Krige model.

In summary, the evaluation results based on the statistical evaluation method are: the accuracy of the fusion model (i.e., the Krige model) constructed by the method of the present embodiment on the root mean square error and the Pearson correlation coefficient is lower than that of the fusion model (i.e., the G model) constructed by the weighted average method.

However, when the multi-source heterogeneous crustal models are fused, the fused models are expected to keep original crustal structure characteristics and geological body characteristics of a plurality of different models, so that selected evaluation indexes can reflect whether the fused models can reflect the original geological characteristics of the models participating in the fusion, the root mean square error and the Pearson correlation coefficient are general evaluation indexes in statistics, the indexes can be generally applied to any field and cannot reflect the fusion specificity of the multi-source heterogeneous crustal models, and whether the fused models realize the fusion expression of the geological characteristics of the multi-source heterogeneous crustal models or not can not be truly reflected according to the indexes. Therefore, a new evaluation index needs to be selected for further verification.

Verification experiment based on the actually measured profile evaluation method:

three actually measured profiles (respectively shown as NN ', YY' and WW 'in figure 2) and an east crust structure model intercepting profile (shown as BB' in figure 2) are adopted to analyze the geological features of the Krige model, and the G model obtained by a weighting method is used as a comparison verification model to determine the final feasibility of the method.

In fig. 2, BB 'represents an east crust model cut-out section, NN' represents an NCISP4 section obtained by a passive source reception function method, YY 'represents a salt city-toe section obtained by a deep seismic method, and WW' represents a wden-alashan section obtained by a deep seismic method.

(1) NCISP4 profile comparison verification result obtained by passive source receiving function method

NCISP4 is a structure image of the crustal S-wave velocity acquired using the receive function method. The stratum of the imaging area fluctuates, an inclined and horizontally-distributed low-speed layer is arranged in the crust, the Moho surface reaches 45km deepest, the structural trace left by evolution of the North China Claton is reserved, and the thinning structural characteristic of the crust from the west to the east of the North China Claton is revealed. The region is mainly characterized by a low-speed stratum L2 in the lower crustal, which is a residual body of the paleo-ocean shells brought to the top of the rock circle and folded back to the lower crustal.

Fig. 5-a to 5-d are comparison graphs of models of the cross-sectional position of the NCISP4, and it can be seen from fig. 5-a to 5-d that the west model and the east model differ in depth and morphology of the sedimentary layer and the conrads plane. The west model has a low speed layer L2 with a P wave velocity of less than 6.2km/s near a depth of 30km on the west side of the cross section, and the east model has a depression with a P wave velocity of 6.45km/s below the Karad.

The deposition layer of the Krige model is similar to the east model, the conradd surface is between the conradd surfaces of the east and west models, a low-speed anomaly L2' exists at a depth of 25km-40km, the P wave speed is lower than 6.2km/s, and the P wave speed can correspond to a low-speed zone L2 in the west model.

The G model deposition layer is similar to the Western model, the conrads surface is the isoline with the P wave velocity of 6.3km/s, the east model is similar, and no description of the low velocity layer L2 exists. For the expression of the morphology and depth of the Mohuo surface, the east and west models are similar, and the Krige and G fusion model is between the east and west models.

(2) Wendeng-Alaran profile comparison verification result obtained by deep seismic method

The Wendeng-Alalashan velocity structure profile in the east model is a two-dimensional deep seismic depth-finding profile obtained by modeling refracted waves and reflected waves by a two-dimensional ray tracing method. At the junction of the Shanxi area of collapse and Taihang mountain ridge, the sedimentary layer, the upper crust, the middle crust, the lower crust and the upper mantle are layered by G, C1, C3 and M interfaces, while the C2 interface is layered again on the middle crust. The thickness of the deposition layer is 0.5 km-2 km, the thickness of the crust is 39km, and the thickness of the crust is 15 km-19 km. The depth of Moho increased from west to east to over 40 km. The inner structure of the earth crust is extremely complex and changeable, and the middle and upper earth crust has obvious high and low speed abnormal structures.

Fig. 6-a to 6-d are comparative graphs of the model of the location of the wden-alagin profile, and it can be seen from fig. 6-a to 6-d that the east and west models have similar features of depth and morphology only at the interface between the deposition layer and the mojow surface, the deposition layer is located near 1.4km in depth and the interface is smooth, the mojow surface is located near 40km in depth and gradually rises from west to east. The east model has an upper crustal interface C1 at a depth of 15km, a middle and lower crustal interface C2 at a depth of 23km, and a lower crustal interior C3 at a depth of 30 km. High-speed anomalies with P-wave velocity greater than 6.2km/s exist in the upper crust, and low-speed anomalies with P-wave velocity less than 6.15km/s exist in the middle crust. In the western model, an upper crustal interface C1 is positioned at a depth of 10km, a middle and lower crustal interface C2 is positioned at a depth of 20km, a C3 interface is positioned between 30km and 40km in depth, a low-speed layer with the P wave speed lower than 6.49km/s exists in the lower crustal of the east side of the section, and a C3 interface consists of an isoline of the top of the low-speed layer with the west side P wave speed of 6.5km/s and the east side P wave speed of 6.7 km/s.

The interface of the Krige model deposition layer is higher than the interfaces of the east and west model deposition layers, and the Mohol surface is similar to that of the east model. The interfaces of C1 and C2 are similar to those of the east model in structure, and the depths of the interfaces of C2 and C3 are slightly lower than those of the east model. The C1 and C2 interfaces are equal surface of P wave velocity of 6.15km/s, so that the P wave velocity is between the C1 and C2 interfaces, the stratum with the depth of 5km-15km is a high-speed layer, and the stratum with the depth of 15km-30km is a low-speed layer, and the P wave velocity is corresponding to the middle and upper crustal high and low-speed abnormal structures of the east model Wenden-Arabian profile in a staggered mode. And below the C3 interface, there is a low speed anomaly corresponding to the western model.

The sedimentary layers and the mojo surface of the G model are similar to the east and west models. The C1 interface is lower than the depth of the C1 interface of the east and west models, the C2 interface is similar to the C2 interface of the Krige model, and the C3 interface is the same as the C3 interface of the west model with the P wave speed of 6.7km/s in shape and depth. However, the P-wave velocity at the interfaces of G models C1 and C2 increases from top to bottom, and only low-velocity anomalies exist below the isoline with the P-wave velocity of 6.2km/s, and the high-velocity and low-velocity anomaly characteristics of the upper crust in the east model are not retained. The low-speed layer with the cross section west-side P wave speed lower than 6.5km/s is positioned above the C3 interface and does not correspond to the position of the west model low-speed layer.

(3) Salt city-Baotou section comparison verification result obtained by deep seismic method

The salt city-Baotou P-wave velocity structural section in the east model is a rock ring two-dimensional P-wave velocity structural section obtained by inverting high-resolution refraction and wide-angle reflection/refraction combined detection section data by adopting a ray tracing method. The profile layered structure is consistent with Wen-Den-Ara, the Shanxi fault zone in the profile is subjected to strong geological structure deformation, the crust structure is broken, and an obvious low-speed depressed area exists in the upper crust. There is a low velocity body between the upper mesochite C1 interface and the C2 interface.

Fig. 7-a to 7-d are comparative graphs of the model of the cross-sectional position of the halocheng shell, and it can be seen from fig. 7-a to 7-d that the depth of the mohohedral surface of the east and west models is 45km and the morphology difference is not large, and the depth of the deposition layer in the middle of the cross-section is slightly increased. The east model deposition depth is around 1.4km, the depth of the C1 interface is between 15km and 20km, the C2 interface is at20 km depth, and the C3 interface is at 30km depth. The upper crust has a remarkable low-speed depression area, the middle crust is a low-speed zone with the P wave speed lower than 6.15km/s, and a low-speed layer with the P wave speed lower than 6.6km/s exists below a C3 interface. The depth of the western model sedimentary deposit is between 0km and 5km, the C1 interface is between 5km and 15km, the C2 interface is between 20km and 30km, and the speed difference of the upper interface and the lower interface is more than 0.2 km/s. The depth of the C3 interface is 35km, and the crust structure below the C3 interface is a low-speed band with the P wave speed less than 6.55 km/s.

The Krige model deposition layer is only provided with a depression in the middle, the depth is less than 5km, the Krige model deposition layer is thinned from the middle of the section to two ends, the upper crust is exposed, the difference between the Krige model deposition layer and the east model and the west model is large, the depth of the Mohuo surface is 45km, and the form is similar to that of the east model. The depth of the C1 interface is between 10km and 15km, the depth of the C2 interface gradually decreases from the west to the east, the depth is between 20km and 30km, the depth of the C3 interface is 30km, and the east side is close to the C2 interface. The low-speed zone located between the interfaces of C1 and C2 corresponds to the east model, while the high-speed zone of 20km to 30km raises the C2 interface, but corresponds to the crust structure between the interfaces of the west models C2 and C3, and a low-speed layer is present at a depth of 40km below the C3 interface, and can correspond to the low-speed notch of the east model and the low-speed zone of the west model.

The depth and morphology of the major discontinuities of the G model (sediment layer, C1, C2, C3, mojohn) are similar to those of the western model, with low velocity layers below the C3 interface with P-wave velocities less than 6.53km/s, but the mid-upper crust structure lacks a description of the low velocity bands in the eastern model.

(4) BB' section comparison verification result of east China Claritong three-dimensional speed structure model interception

The BB' section in the east model is a longitudinal section in an east crustal three-dimensional speed structure model HBCrust1.0 in North China Claton. The profile intersects with NCISP4, and the model is divided into sediment layer, upper crust, lower crust and upper mantle by G, C and M three-layer discontinuities. Part of the crust in the section is exposed to the ground, and the Shanxi fault zone low-speed layer extends from 16km to 30km in depth.

Fig. 8-a to 8-d are comparative diagrams of models at the east model cut-away section BB', and as can be seen from fig. 8-a to 8-d, the mohoh planes of the east and west models are similar to the conradd planes in morphology, with the conradd plane depth being between 20km and 30km, and the mohoh planes gradually rising from west to east and having a depth near 45 km. The deposited layer of the east model BB' profile is positioned near the depth of 5km, the upper crusta is exposed, and the lower crusta is gradually thinned from west to east and is positioned between the depths of 35km and 39 km. The contour line of the P-wave velocity of 6.55km/s in the lower crust ascends from west to east, and the presence of a dip in the west region of the lower crust can be seen in comparison to the Conrads surface. The depth of the deposition layer of the west model is about 5km, and the difference with the east model is large. At depths of 20km to 30km, there is a low velocity layer in the lower crust below the conrads surface.

The Krige model deposition layer keeps the exposed characteristics of the crust on the east side of the section, the depth and the morphological characteristics of the east model deposition layer are met, the low-speed abnormity with the P-wave speed of 6.0km/s exists in the upper crust, and the sunken characteristics of the east model Conrads surface on the west side of the section are met. The crust has a concave shape with low speed which is abnormally approximately expressed at the same position with the speed of the east model P wave of 6.55km/s and a low speed layer with the speed of the west model P wave of 6.25km/s below the Karad surface in the depth of 25km to 40 km.

The depth and the shape of the G model conradd surface and the Mohuo surface are similar to those of the east model and the west model, and the depth and the shape of a deposition layer conform to the characteristics of the west model. The presence of the characteristic P-wave velocity of 6.15km/s in the crust on the east side of the section is only consistent with the description of the western model. Below the contour line with a P-wave velocity of 6.4km/s, there are no velocity anomalies in the G-model crust at depths below 30 km.

In summary, the evaluation results based on the actually measured profile evaluation method are: comparing two deep seismic sounding profiles of the east model, one intercepting profile and one receiving function imaging profile of the west model can find that the Krige model and the G model can well keep the characteristics of the original model section at the position of the Mohuo surface and the Kancki surface where the east model and the west model have little difference. When the east and west models are different, the main discontinuity form retained by the Krige model is similar to that of the east model, and the main discontinuity form retained by the G model is similar to that of the west model. In terms of expression of east-west high-speed anomalies and low-speed anomalies, the G model can only retain the structural features of the lower hull of the west model, and the Krige model can simultaneously retain the high-speed anomalies and the low-speed anomalies of the east-west model by correcting the main discontinuous morphology and the P-wave velocity difference, so that the fusion model obtained by the method of the embodiment has higher reliability.

By integrating the statistical evaluation method and the actually measured profile evaluation method, it can be found that although the precision of the fusion model constructed by the method of the present embodiment on the root mean square error and the correlation coefficient is lower than that of the fusion model constructed by the weighted average method, when the actually measured profile is compared, the method of the present embodiment can retain the geological features of a plurality of crustal three-dimensional structure models in the research area, and overcome the problem that the geological feature difference is difficult to fuse in the model fusion, so that the method of the present embodiment has feasibility and reliability.

The method for fusing the three-dimensional structure model of the crust of the embodiment combines the geostatistics principle with the geophysical method, and solves the difficult problem of unified construction of the model fusion and the crust structure of the multi-source heterogeneous three-dimensional structure model of the crust. Aiming at the differences of the resolution, depth and attribute of the crust three-dimensional structure models obtained by different geophysical methods, the method obtains crust three-dimensional P-wave velocity structure models with the same resolution, depth and attribute by using an empirical formula of seismic wave velocity and density and a related interpolation method, and when a unified crust three-dimensional structure model retaining multi-model geological features is constructed, the geological features can be fused into a fusion matrix by using a model fusion method based on a collaborative kriging method to obtain a unified crust structure containing the multi-model geological features.

The method mainly solves the multiple solution problem of inverting the crust structure model and the difference integration problem of multiple crust three-dimensional structure models obtained by seismic wave, gravity and joint inversion of the seismic wave and the gravity. With the intensive research on the crustal structure, more and more crustal three-dimensional structure models are obtained by different methods, and the characteristics of the models are difficult to fuse to carry out numerical simulation and geological interpretation. The method for fusing the three-dimensional structure model of the crust aims to provide a set of model fusion solution for the research of the crust structure by the methods of unified attribute, fusion modeling and joint simulation for the cross fusion of various geophysical methods.

Device embodiment

As shown in fig. 9, the device for fusing three-dimensional earth crust structural models of this embodiment includes a processor and a memory, where a computer program operable on the processor is stored in the memory, and the processor implements the method of the above method embodiment when executing the computer program.

That is, the method in the above method embodiment is understood as a flow of the method for fusing the three-dimensional structure model of the earth's crust, which can be realized by computer program instructions. These computer program instructions may be provided to a processor such that execution of the instructions by the processor results in the implementation of the functions specified in the method flow described above.

The processor referred to in this embodiment refers to a processing device such as a microprocessor MCU or a programmable logic device FPGA.

The memory referred to in this embodiment includes a physical device for storing information, and generally, information is digitized and then stored in a medium using an electric, magnetic, optical, or the like. For example: various memories for storing information by using an electric energy mode, such as RAM, ROM and the like; various memories for storing information by magnetic energy, such as hard disk, floppy disk, magnetic tape, magnetic core memory, bubble memory, and U disk; various types of memory, CD or DVD, that store information optically. Of course, there are other ways of memory, such as quantum memory, graphene memory, and so forth.

The apparatus comprising the memory, the processor and the computer program is realized by the processor executing corresponding program instructions in the computer, and the processor can be loaded with various operating systems, such as windows operating system, linux system, android, iOS system, and the like.