Method for Inverting Amplitude of Internal Solitary Waves in the Ocean, Electronic Device, and Readable Storage Medium

Abstract

The present application proposes a method for inverting the amplitude of internal solitary waves in the ocean, an electronic device, and a readable storage medium. By combining the SWOT satellite observation data with the observation data of other remote sensing means at adjacent times to form a two-temporal remote sensing image, the amplitude of the observed internal solitary waves in the target sea area is obtained. Based on the fact that radar interferometry can provide high-resolution and high-precision large-area two-dimensional sea surface height observation data, when the sea surface height anomaly caused by internal solitary waves in the ocean can be captured, the amplitude of internal solitary waves is obtained by combining other remote sensing observation data, thereby simplifying the calculation process and improving the inversion accuracy.

Description

Technical Field

[0001] The present invention belongs to the technical field of predicting the amplitude of internal solitary waves in the ocean, and in particular relates to a method for inverting the amplitude of internal solitary waves in the ocean, an electronic device, and a readable storage medium. Background Art

[0002] Internal waves in the ocean are a wave phenomenon that occurs inside the stably stratified ocean and has a frequency between the inertial frequency and the buoyancy frequency, and their maximum amplitude appears inside the ocean. When the seawater density is stably stratified and there is a disturbance source, it is possible to cause the generation of internal waves. The internal waves that are often observed are a special type called internal solitary waves, which are usually generated by the non-linear steepening of the internal tide waves generated by the interaction between the barotropic tide and the topography during the propagation process, and then fission into internal solitary waves.

[0003] In the techniques of predicting and inverting internal solitary waves in the ocean, at the present stage, there are many documents publicly available for predicting the internal wave speed, such as papers like "Construction and Evaluation of the Internal Solitary Wave Speed - Gaussian Function Model", "Computer Algebra Research on Internal Solitary Waves", "Propagation and Evolution Characteristics of Weak Nonlinear Internal Solitary Waves on Slopes", etc., as well as patent documents such as CN115859021B and CN118114030B, which all disclose techniques for obtaining the propagation speed of internal solitary waves through remote sensing means. However, in the field of remote sensing detection of the amplitude of internal solitary waves, there is relatively no simple solution at the present stage, and most of the internal solitary wave amplitude inversion schemes have defects such as poor accuracy and high error. Summary of the Invention

[0004] In order to make up for the above-mentioned defects in the internal solitary wave amplitude inversion technology, the present application proposes a method for inverting the amplitude of internal solitary waves in the ocean, an electronic device, and a readable storage medium. Based on the fact that radar interferometry can provide high-resolution and high-precision large-area two-dimensional sea surface height observation data, when the sea surface height anomaly caused by internal solitary waves in the ocean can be captured, and then combined with other remote sensing observation data to obtain the internal solitary wave amplitude data, thereby simplifying the calculation process and improving the inversion accuracy.

[0005] The technical solution of the method includes: A method for inverting the amplitude of internal solitary waves in the ocean, characterized in that a dual-temporal remote sensing image is formed by combining SWOT satellite observation data with observation data from other remote sensing means at a nearby time, and then the amplitude of the observed internal solitary wave in the target sea area is obtained.

[0006] The steps include:

[0007] Obtain the sea surface height anomaly ζ of the target sea area from the remote sensing image of the internal solitary wave observed by the SWOT satellite in the target sea area;

[0008] According to the chart of the target sea area and the data of the ocean numerical model, obtain the water depth data and the temperature-salinity profile data of the target sea area, and calculate the seawater buoyancy frequency N of the target sea area;

[0009] Based on the water depth data and the seawater buoyancy frequency, and according to the vertical structure function of the internal solitary wave, solve for the linear phase velocity c0 of the internal solitary wave in the target sea area;

[0010] Collect other remote sensing images near the time of SWOT satellite observation in the range of the target sea area to form a two-temporal remote sensing image of the internal solitary wave, and obtain the propagation velocity v of the internal solitary wave according to the two-temporal remote sensing image;

[0011] According to the strongly nonlinear Miyata–Choi–Camassa (MCC) model under the free surface boundary condition, obtain the relationship between the sea surface height anomaly in the target sea area, the vertical displacement of the interface between the two-layer fluid, and the data of the upper and lower layers of the two-layer fluid. Furthermore, combine the relationship between the propagation velocity v of the internal solitary wave, the linear phase velocity c0 of the internal solitary wave, the data of the upper and lower layers of the two-layer fluid, and the vertical displacement of the interface between the two-layer fluid, and jointly solve through the above relationship to obtain the vertical displacement data η;

[0012] Obtain the amplitude of the observed internal solitary wave in the target sea area according to the vertical displacement.

[0013] Furthermore, the other remote sensing images include one or more of synthetic aperture radar (SAR) satellite remote sensing images, visible light satellite remote sensing images, shipborne X-band radar remote sensing images, and aerial remote sensing images.

[0014] Furthermore, the steps for obtaining the seawater buoyancy frequency N include:

[0015]

[0016] where ρ is the seawater density, z is the water depth, and g is the acceleration due to gravity.

[0017] Furthermore, the linear phase velocity c0 of the internal solitary wave propagation is obtained through the vertical structure function of the internal solitary wave where is the eigenfunction of the first mode of the internal solitary wave.

[0018] Furthermore, the steps for obtaining the vertical displacement η of the interface between the two-layer fluid include:

[0019] Obtain the relationship between the sea surface height anomaly ζ in the target sea area, the vertical displacement η of the interface between the two-layer fluid, and the data of the upper and lower layers of the two-layer fluid, which is abbreviated as the vertical displacement relationship:

[0020]

[0021] Obtain the relationship between the propagation velocity v of the internal solitary wave, the linear phase velocity c0 of the internal solitary wave, the vertical displacement η of the interface between the two-layer fluid, and the data of the upper and lower layers of the two-layer fluid, which is abbreviated as the propagation velocity relationship:

[0022]

[0023] Obtain the relationship between the linear phase velocity c0 of the internal solitary wave and the data of the upper and lower layers of the two-layer fluid, which is abbreviated as the linear phase velocity relationship:

[0024]

[0025] According to the above vertical displacement relationship, propagation velocity relationship, and linear phase velocity relationship, through the combined solution of the above three relational expressions, obtain the vertical displacement η of the interface between the two-layer fluid;

[0026] Among them, Δ between the upper layer and the lower layer of the two-layer fluid is the density difference, and its value H is the total water depth of the target sea area, H = h1 + h2, ρ1 and h1 are the density and thickness of the upper layer fluid of the two-layer fluid system respectively, ρ2 and h2 are the density and thickness of the lower layer fluid respectively; g is the acceleration due to gravity.

[0027] Further, the adjacent time is an interval value greater than 0 and not greater than the generation period of the internal solitary wave in this sea area.

[0028] Further, the process of obtaining the amplitude of the observed internal solitary wave in the target sea area according to the vertical displacement of the interface between the two-layer fluid includes using the absolute value η0 of the vertical displacement η of the interface between the two-layer fluid as the amplitude of the observed internal solitary wave in the target sea area.

[0029] This application also proposes an electronic device, which includes a processor and a memory. The memory stores a program or instruction that can run on the processor, and when the program or instruction is executed by the processor, it realizes the steps of the method described in any one of the above.

[0030] This application also proposes a readable storage medium, on which a program or instruction is stored, and when the program or instruction is executed by a processor, it realizes the steps of the method described in any one of the above.

[0031] Compared with the traditional remote sensing inversion method for the amplitude of internal solitary waves, the present application avoids the error in the inversion of the amplitude of internal solitary waves introduced by the calculation errors of the upper layer thickness h1 and the density difference Δ during the traditional remote sensing inversion process of the amplitude of internal solitary waves, and improves the accuracy of the satellite remote sensing inversion of the amplitude of ocean internal solitary waves. It makes full use of the sea surface height anomaly of ocean internal solitary waves observed by the SWOT satellite, which is more accurate than the bright and dark stripe feature information observed from SAR, visible light or shipborne X-band radar remote sensing images, and avoids the amplitude inversion error introduced by the error in extracting the bright and dark stripe feature information, thus improving the accuracy of the satellite remote sensing inversion of the amplitude of ocean internal solitary waves. It only needs to directly obtain the sea surface height anomaly and the propagation speed of internal solitary waves respectively through the dual-temporal remote sensing images based on the SWOT satellite, directly obtain the total water depth through the nautical chart, solve for the linear phase velocity of internal solitary waves, and then the amplitude of the ocean internal solitary waves observed by remote sensing can be obtained by jointly solving multiple relational expressions, which simplifies the dependence of the satellite remote sensing inversion technology for the amplitude of ocean internal solitary waves on the dynamic process of internal waves. By collecting remote sensing data such as SAR, visible light or shipborne X-band radar, a dual-temporal remote sensing image based on the SWOT satellite is formed. Using the advantages of the dual-temporal remote sensing image, not only can a more accurate propagation speed of ocean internal solitary waves be obtained, improving the accuracy of the satellite remote sensing inversion of the amplitude of ocean internal solitary waves, but also the advantages of multi-source and multi-temporal remote sensing images of ocean internal solitary waves can be fully utilized. BRIEF DESCRIPTION OF THE DRAWINGS

[0032] In order to more clearly illustrate the technical solutions in the embodiments of the present invention or the prior art, the following will briefly introduce the drawings required for the description of the embodiments or the prior art. Obviously, the drawings in the following description are only some embodiments of the present invention. For those of ordinary skill in the art, other drawings can be obtained based on these drawings without creative efforts.

[0033] Figure 1 It is a schematic flowchart of an implementation manner of the method of the present invention. DETAILED DESCRIPTION OF THE EMBODIMENTS

[0034] The following will clearly and completely describe the technical solutions of the present application with reference to the drawings. Obviously, the described embodiments are some, but not all, of the embodiments of the present application. All other embodiments obtained by those of ordinary skill in the art based on the embodiments in the present application without creative efforts shall fall within the scope of protection of the present application.

[0035] In the description of the present application, it should be noted that the orientation or positional relationship indicated by the terms "center", "upper", "lower", "left", "right", "vertical", "horizontal", "inner", "outer", etc. is based on the orientation or positional relationship shown in the drawings. It is only for the convenience of describing the present application and simplifying the description, rather than indicating or implying that the device or element referred to must have a specific orientation, be constructed and operated in a specific orientation, and therefore should not be construed as a limitation to the present application. In addition, the terms "first", "second", "third" are only used for descriptive purposes and cannot be construed as indicating or implying relative importance.

[0036] In the description of the present application, it should be noted that unless otherwise clearly specified and defined, the terms "installed", "connected", "coupled" should be understood in a broad sense. For example, it can be a fixed connection, a detachable connection, or an integral connection; it can be a mechanical connection or an electrical connection; it can be directly connected or indirectly connected through an intermediate medium, and it can be the communication inside two elements. For those of ordinary skill in the art, the specific meanings of the above terms in the present application can be understood according to specific circumstances.

[0037] The present invention will be further described in detail below with reference to the drawings.

[0038] Combined with Figure 1 , an embodiment of the present application.

[0039] A method for retrieving the amplitude of internal solitary waves in the ocean constructs a two - temporal - phase remote - sensing image by combining SWOT satellite observation data with observation data from other remote - sensing means at adjacent times, and then obtains the amplitude of the observed internal solitary waves in the target sea area. The steps include: obtaining the sea - surface height anomaly ζ of the target sea area from the remote - sensing image data of internal solitary waves observed by the SWOT satellite in the target sea area; obtaining the water depth data and temperature - salinity profile data of the target sea area according to the nautical chart and ocean numerical model data of the target sea area, and calculating the buoyancy frequency N of the sea water in the target sea area; solving for the linear phase velocity c0 of the internal solitary waves in the target sea area according to the vertical structure function of internal solitary waves through the water depth data and the buoyancy frequency of sea water; collecting other remote - sensing images adjacent in time to the SWOT satellite observations within the scope of the target sea area to form a two - temporal - phase remote - sensing image of internal solitary waves, and obtaining the propagation velocity v of the internal solitary waves according to the two - temporal - phase remote - sensing image; obtaining the relationship between the sea - surface height anomaly of the target sea area, the vertical displacement of the interface between the two - layer fluid, and the data of the upper and lower layers of the two - layer fluid according to the strongly non - linear Miyata–Choi–Camassa (MCC) model under the free - surface boundary condition, and then combining the relationship between the propagation velocity v of the internal solitary waves, the linear phase velocity c0 of the internal solitary waves, the data of the upper and lower layers of the two - layer fluid, and the vertical displacement of the interface between the two - layer fluid, and jointly solving through the above relationships to obtain the vertical displacement data η; obtaining the amplitude of the observed internal solitary waves in the target sea area according to the vertical displacement. In this embodiment, when there are internal solitary waves in the ocean, both the sea - surface height and the sea - surface roughness will change. Compared with traditional altimeters, the SWOT (Surface Water and Ocean Topography) satellite can provide high - resolution and high - precision large - area two - dimensional sea - surface height observation data through radar interferometry, so as to capture the sea - surface height anomaly caused by internal solitary waves on the sea surface. At the same time, due to the strong non - linear characteristics of internal solitary waves, the phenomenon of convergence and divergence occurs on the sea surface, causing changes in sea - surface roughness, which thus presents striped features of bright and dark intervals in SAR, visible - light, or ship - borne X - band radar remote - sensing images. Based on the remote - sensing image of internal solitary waves observed by the SWOT satellite in a certain sea area, combined with SAR, visible - light, or ship - borne X - band radar remote - sensing images of internal solitary waves in the adjacent remote - sensing observation time (the adjacent time interval value is greater than 0 and not greater than the generation period of internal solitary waves in this sea area, and usually the smaller the adjacent time interval value, the better) within the same observed sea - area scope of the SWOT satellite, a two - temporal - phase remote - sensing image can be formed, and the propagation velocity v of the internal solitary waves in the ocean can be calculated. On the basis of the above - mentioned embodiment, further, the other remote - sensing images include one or several of SAR remote - sensing images, visible - light satellite remote - sensing images, ship - borne X - band radar images, and aerial remote - sensing images.The satellites at different times of the dual-temporal remote sensing images composed with the SWOT satellite are usually satellite remote sensing data such as SAR or visible light satellites, and can also be remote sensing images of internal solitary waves in the ocean obtained by other means such as shipborne X-band radars and aerial remote sensing, and it is not necessarily required to be satellite remote sensing images.

[0040] Based on one or more of the above embodiments, further, the step of obtaining the seawater buoyancy frequency N includes:

[0041]

[0042] where ρ is the seawater density, z is the water depth at that place, and g is the acceleration due to gravity.

[0043] Based on one or more of the above embodiments, further, the linear phase velocity c0 of the internal solitary wave propagation is obtained through the vertical structure function of the internal solitary wave obtained, where is the eigenfunction of the first mode of the internal solitary wave.

[0044] Based on one or more of the above embodiments, further, the step of obtaining the vertical displacement η of the interface between the two-layer fluid includes:

[0045] Obtain the relationship between the sea surface height anomaly ζ of the target sea area, the vertical displacement η of the interface between the two-layer fluid, and the data of the upper and lower layers of the two-layer fluid, which is abbreviated as the vertical displacement relationship:

[0046]

[0047] Obtain the relationship between the propagation velocity v of the internal solitary wave, the linear phase velocity c0 of the internal solitary wave, the vertical displacement η of the interface between the two-layer fluid, and the data of the upper and lower layers of the two-layer fluid, which is abbreviated as the propagation velocity relationship:

[0048]

[0049] Obtain the relationship between the linear phase velocity c0 of the internal solitary wave and the data of the upper and lower layers of the two-layer fluid, which is abbreviated as the linear phase velocity relationship:

[0050]

[0051] According to the above three relational expressions of the vertical displacement relationship, the propagation velocity relationship, and the linear phase velocity relationship, through the joint solution of the above three relational expressions, obtain the vertical displacement η of the interface between the two-layer fluid;

[0052] where Δ between the upper fluid and the lower fluid of the two-layer fluid is the density difference, and its value Let \(H\) be the total water depth of the target sea area, \(H = h_1+h_2\), where \(\rho_1\) and \(h_1\) are the density and thickness of the upper fluid in the two - layer fluid system respectively, and \(\rho_2\) and \(h_2\) are the density and thickness of the lower fluid respectively; \(g\) is the acceleration due to gravity.

[0053] In this embodiment, according to the strongly nonlinear Miyata–Choi–Camassa (MCC) model under the free - surface boundary condition, the following relationship exists between the sea - surface height anomaly \(\zeta\), the vertical displacement \(\eta\) of the interface between the two - layer fluids, and the data of the upper and lower fluids in the two - layer fluids: In the formula, \(\zeta\) is the sea - surface height anomaly of the ocean internal solitary wave observed by the SWOT satellite; \(\eta\) is the vertical displacement of the interface between the two - layer fluids, and its absolute value is the amplitude \(\eta_0\) of the ocean internal solitary wave observed by the SWOT satellite; when the ocean internal solitary wave is a descending - type internal solitary wave, \(\zeta>0\) and \(\eta < 0\); when the ocean internal solitary wave is an ascending - type internal solitary wave, \(\zeta < 0\) and \(\eta>0\).

[0054]

[0055]

[0056] \(H = h_1+h_2\)

[0057] \(c_0\) is the linear phase velocity of the internal solitary wave, which can be obtained from the vertical structure function of the internal solitary wave obtained

[0058] In the formula, is the eigen - function of the first mode of the internal solitary wave, \(N\) is the buoyancy frequency of seawater, \(\rho\) is the density of seawater, \(z\) is the water depth, and the density of seawater can be obtained from the temperature - salinity profile data of the SWOT satellite - observed sea area range and the observation period provided by the ocean numerical model. Among the three relationships of the above vertical displacement relationship, propagation velocity relationship, and linear phase velocity relationship, there are 7 variables. Among them, the vertical displacement \(\eta\) of the interface between the two - layer fluids, the density difference \(\Delta\), and the upper - layer thickness \(h_1\) are 3 unknown variables; the sea - surface height anomaly \(\zeta\) of the ocean internal solitary wave, the seawater depth \(H\), the linear phase velocity \(c_0\) of the internal solitary wave, and the propagation velocity \(v\) of the internal solitary wave are the 4 known variables. At this time, the 3 unknowns exactly correspond to the 3 relationships of the vertical displacement relationship, propagation velocity relationship, and linear phase velocity relationship. Therefore, the vertical displacement \(\eta\) of the interface between the two - layer fluids, the density difference \(\Delta\), and the upper - layer thickness \(h_1\) can be obtained by joint solution. Taking the absolute value \(\eta_0\) of the vertical displacement \(\eta\) of the interface between the two - layer fluids, the amplitude \(\eta_0\) of the ocean internal solitary wave observed by the SWOT satellite can be obtained.

[0059] Based on one or more of the above - mentioned embodiments, further, the adjacent time is an interval value greater than 0 and not greater than the generation period of the internal solitary wave in this sea area.

[0060] Based on one or more of the above embodiments, further, the process of obtaining the amplitude of the observed internal solitary wave in the target sea area according to the vertical displacement includes using the absolute value η0 of the vertical displacement η of the inner interface of the two-layer fluid as the amplitude data of the observed internal solitary wave in the target sea area.

[0061] The present invention also provides an electronic device, which includes a processor and a memory. The memory stores a program or instructions that can run on the processor. When the program or instructions are executed by the processor, the steps of the method described in any one of the above embodiments are implemented.

[0062] The present invention also provides a readable storage medium, on which a program or instructions are stored. When the program or instructions are executed by a processor, the steps of the method described in any one of the above embodiments are implemented.

[0063] Compared with the traditional remote sensing inversion method for the amplitude of internal solitary waves, this application avoids the error in the amplitude inversion of internal solitary waves introduced by the calculation errors of the upper layer thickness h1 and density difference Δ in the traditional remote sensing inversion process of the amplitude of internal solitary waves, and improves the accuracy of satellite remote sensing inversion of the amplitude of ocean internal solitary waves. It makes full use of the sea surface height anomaly of ocean internal solitary waves observed by the SWOT satellite, which is more accurate than the bright and dark stripe feature information observed from SAR, visible light or shipborne X-band radar remote sensing images, and avoids the amplitude inversion error introduced by the error in extracting the bright and dark stripe feature information, thus improving the accuracy of satellite remote sensing inversion of the amplitude of ocean internal solitary waves. Only by directly obtaining the sea surface height anomaly and the propagation speed of internal solitary waves from the dual-temporal remote sensing images based on the SWOT satellite respectively, directly obtaining the total water depth through a nautical chart, obtaining the linear phase speed by solving the vertical structure function of internal solitary waves, and then the amplitude of the ocean internal solitary waves observed by remote sensing can be calculated, which simplifies the dependence of the satellite remote sensing inversion technology of the amplitude of ocean internal solitary waves on the dynamic process of internal waves in the ocean. By collecting remote sensing data such as SAR, visible light or shipborne X-band radar, a dual-temporal remote sensing image based on the SWOT satellite is formed. By using the advantages of the dual-temporal remote sensing image, not only can a more accurate propagation speed of ocean internal solitary waves be obtained, improving the accuracy of satellite remote sensing inversion of the amplitude of ocean internal solitary waves, but also the advantages of multi-source and multi-temporal remote sensing images of ocean internal solitary waves can be fully utilized.

[0064] The above technical solutions only reflect the preferred technical solutions of the technical solutions of the present invention. Some changes that may be made by those skilled in the art to some parts thereof all reflect the principles of the present invention and fall within the protection scope of the present invention.

Claims

1. An amplitude inversion method for internal solitary waves in the ocean, characterized in that, By combining the SWOT satellite observation data with the observation data of other remote sensing means at adjacent times to form a two-phase remote sensing image, and then obtaining the amplitude of the observed internal solitary wave in the target sea area. The steps include: Obtaining the sea surface height anomaly ζ of the target sea area from the remote sensing image of the internal solitary wave observed by the SWOT satellite in the target sea area. Obtaining the water depth data and temperature-salinity profile data of the target sea area according to the nautical chart and ocean numerical model data of the target sea area, and calculating the seawater buoyancy frequency N of the target sea area. According to the water depth data and the seawater buoyancy frequency, and based on the vertical structure function of the internal solitary wave, solving to obtain the linear phase velocity c0 of the internal solitary wave in the target sea area. Collecting other remote sensing images of the SWOT satellite observation at adjacent times within the scope of the target sea area to form a two-phase remote sensing image of the internal solitary wave, and obtaining the propagation velocity v of the internal solitary wave according to the two-phase remote sensing image. According to the strongly nonlinear Miyata–Choi–Camassa (MCC) model under the free surface boundary condition, obtaining the relationship between the sea surface height anomaly ζ of the target sea area, the vertical displacement of the interface between the two-layer fluid, and the data of the upper and lower layers of the two-layer fluid. Then, combining the relationship between the propagation velocity v of the internal solitary wave, the linear phase velocity c0 of the internal solitary wave, the data of the upper and lower layers of the two-layer fluid, and the vertical displacement of the interface between the two-layer fluid, and jointly solving through the above relationship to obtain the vertical displacement data η. Obtaining the amplitude of the observed internal solitary wave in the target sea area according to the vertical displacement.

2. The method according to claim 1, characterized in that The other remote sensing images include one or several of synthetic aperture radar (SAR) satellite remote sensing images, visible light satellite remote sensing images, shipborne X-band radar remote sensing images, and aerial remote sensing images.

3. The method according to claim 1, wherein The steps for obtaining the seawater buoyancy frequency N include: where ρ is the seawater density, z is the water depth, and g is the acceleration due to gravity.

4. The method according to claim 3, characterized in that, The linear phase velocity \(c_0\) of the internal solitary wave propagation is obtained through the vertical structure function of the internal solitary wave where is the eigenfunction of the first mode of the internal solitary wave 5. The method according to claim 4, wherein The steps for obtaining the vertical displacement η of the interface between the two-layer fluid include: Obtaining the relationship between the sea surface height anomaly ζ of the target sea area, the vertical displacement η of the interface between the two-layer fluid, and the data of the upper and lower layers of the two-layer fluid, which is abbreviated as the vertical displacement relationship. Obtaining the relationship between the propagation velocity v of the internal solitary wave, the linear phase velocity c0 of the internal solitary wave, the vertical displacement η of the interface between the two-layer fluid, and the data of the upper and lower layers of the two-layer fluid, which is abbreviated as the propagation velocity relationship. Obtaining the relationship between the linear phase velocity c0 of the internal solitary wave and the data of the upper and lower layers of the two-layer fluid, which is abbreviated as the linear phase velocity relationship. According to the above vertical displacement relationship, propagation velocity relationship, and linear phase velocity relationship, jointly solving through the above three relationships to obtain the vertical displacement η of the interface between the two-layer fluid. where Δ between the upper fluid and the lower fluid of the two-layer fluid is the density difference, and its value H is the total water depth of the target sea area, H = h1 + h2, ρ1 and h1 are the density and thickness of the upper fluid of the two-layer fluid system respectively, ρ2 and h2 are the density and thickness of the lower fluid respectively; g is the acceleration due to gravity.

6. The method according to claim 1, wherein The adjacent time is an interval value greater than 0 and not greater than the generation period of the internal solitary wave in this sea area.

7. The method according to claim 5, characterized in that, The process of obtaining the amplitude of the observed internal solitary wave in the target sea area according to the vertical displacement of the interface between the two-layer fluid includes taking the absolute value η0 of the vertical displacement η of the interface between the two-layer fluid as the amplitude of the observed internal solitary wave in the target sea area.

8. An electronic device, characterized in that, The electronic device includes a processor and a memory. The memory stores programs or instructions that can run on the processor. When the programs or instructions are executed by the processor, the steps of the method according to any one of claims 1 to 7 are implemented.

9. A readable storage medium, characterized in that, The program or instruction is stored on the readable storage medium, and when the program or instruction is executed by the processor, the steps of the method described in any one of claims 1 to 7 are implemented.

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