A method, device and medium for analyzing and processing the activity rate of shallow seabed fluid

Abstract

The present invention discloses a method, device, and medium for analyzing and processing the activity rate of shallow seabed fluids. Guided by the basic theories of fluid kinematics and thermodynamics, the present invention gives full play to the parameter advantage of the "temperature" factor. By establishing a heat convection conduction model, relying on the measured geothermal data of near-seabed strata with relatively low acquisition costs, and combining the geothermal data of the hydrate stability zone obtained by hydrate phase equilibrium simulation and quasi-seabed reflector inversion, the average geothermal gradient within the hydrate stability zone near-seabed strata and below the seabed is calculated. Finally, the vertical migration rate of shallow seabed fluids is calculated using the Berkeley (Pe) equation, providing a basis for revealing the activity behavior of shallow seabed fluids and assessing the potential ecological environment and geological disaster impacts. The embodiments of the present invention can conveniently and accurately analyze and process the activity rate of shallow seabed fluids, and the present invention can be widely applied to the field of data processing technology.

Description

Technical Field

[0001] The present invention relates to the field of data processing technology, and in particular to a method, device and medium for analyzing and processing the activity rate of shallow seabed fluid. Background Art

[0002] In nature, driven by regional tectonic and sedimentary activity, deep-seated fluids migrate toward shallower layers under overpressure along fluid pathways such as gas chimneys and tectonic faults, causing deep-seated matter and energy to circulate in the shallow seafloor. Intense gas-bearing fluid activity at continental margins can sometimes directly impact the seafloor, playing a crucial role in controlling the ocean's carbon cycle and ecosystem evolution. Furthermore, gas-bearing fluid activity often indicates an ample gas supply in the underlying sediments, making relevant geological exploration crucial for offshore oil and gas exploration, particularly for shallow seafloor natural gas hydrates.

[0003] As an important parameter characterizing the characteristics of fluid activity, the fluid migration rate is often obtained through two methods: survey observation or numerical simulation calculation. Among them, survey observation is direct and can be further divided into geophysical survey, geochemical survey and seabed in situ observation according to the survey method. In geophysical survey, the deep fluid activity rate is qualitatively inferred based on the seismic wave reflection intensity, distribution range, amplitude shape and the degree of deformation of the overlying strata caused; in geochemical survey, the fluid activity rate is inferred based on the characteristics of typical ions (such as sulfate ions) in the pore water of the sedimentary strata below the seabed collected with depth; in seabed in situ observation, in situ monitoring equipment deployed on the seabed is often used to directly monitor the leakage of seabed fluids.

[0004] Numerical simulation is an effective method for indirectly estimating fluid migration rates and is widely used in geological exploration. Specifically, numerical simulation is primarily based on the principles of fluid kinematics and seepage mechanics. By numerically modeling and programmatically calculating specific geological parameters such as formation pressure, pressure gradient, rock permeability, and rock density, it can simulate and predict the intensity and direction of fluid activity.

[0005] Although the method of obtaining fluid migration rate based on direct survey and observation means is highly reliable, it does not have realistic conditions for large-scale promotion and application due to the huge cost of offshore implementation operations and high geological, engineering and environmental risk hazards. Most existing technical solutions are guided by the basic principles of fluid mechanics, relying on existing survey data, and indirectly estimating fluid activity intensity and fluid migration rate through numerical simulation methods to provide key scientific parameters for guiding deep oil and gas exploration. The fluid migration rate is mainly obtained through two methods: "direct" survey and observation or "indirect" numerical simulation calculation. Although the use of survey and observation means to obtain fluid migration rate is highly reliable, its significant disadvantages are high economic cost, long observation period and certain geological, engineering and environmental risk hazards, and it does not have the prospect of widespread promotion and application. Existing numerical simulation technology methods also have certain shortcomings or application limitations in actual application scenarios. Summary of the Invention

[0006] The present invention aims to address, at least to a certain extent, the limitations of related technologies. To this end, the present invention proposes a method, device, and medium for analyzing and processing the flow rate of shallow seabed fluids, which can conveniently and accurately analyze and process the flow rate of shallow seabed fluids.

[0007] In one aspect, an embodiment of the present invention provides a method for analyzing and processing the flow rate of shallow seabed fluid, comprising the following steps:

[0008] Obtaining seismic reflection times at target locations in a seismic profile of the target area, and establishing a fluid seepage geological model based on the seismic reflection times; the target locations include the seabed, a quasi-seabed reflection layer, and the root of the fluid seepage channel; the top boundary of the fluid seepage geological model is the seabed, and the bottom boundary is the root of the fluid seepage channel;

[0009] Based on the fluid leakage geological model and the temperature data of the target location, a heat convection conduction model is established;

[0010] Based on the heat convection conduction model, the formation temperature field function is transformed to obtain the function of the geothermal gradient changing with the burial depth;

[0011] Acquire formation temperature measurement data, and obtain the top boundary temperature gradient value of the near-seabed formation based on the formation temperature measurement data processing; the near-seabed formation represents the top boundary of the fluid leakage geological model;

[0012] Obtain the formation pressure of the seabed-like reflector layer, and based on the formation pressure, solve the hydrate phase equilibrium equation to obtain the phase equilibrium temperature at the bottom of the hydrate stability zone. Then, combine it with the measured seabed temperature to obtain the average geothermal gradient of the hydrate stability zone.

[0013] The average geothermal gradient is substituted into the variation function and then combined with the Berkeley equation to derive the vertical fluid migration rate.

[0014] Optionally, the seismic reflection time includes a first reflection time at the seabed, a second reflection time at a seabed-like reflection layer, and a third reflection time at the root of the fluid leakage channel; and establishing a fluid leakage geological model based on the seismic reflection time includes the following steps:

[0015] Obtaining the seabed depth of the seabed position according to half the product of the first reflection time and the first velocity; the first velocity represents the propagation speed of the seismic wave in the seawater;

[0016] The first depth is obtained according to half of the product of the difference between the second reflection time and the first reflection time and the second velocity; the second velocity represents the propagation speed of the seismic wave in the shallow seabed; the first depth represents the depth of the seabed-like reflection layer below the seabed position;

[0017] A second depth is obtained based on half of the product of the difference between the third reflection time and the first reflection time and the second velocity; the second depth represents the depth of the root position of the fluid leakage channel below the seabed position;

[0018] A fluid seepage geological model is established based on the seabed depth, the first depth, and the second depth;

[0019] Among them, the top boundary of the fluid leakage geological model is the seabed position, and the bottom boundary of the fluid leakage geological model is the root position of the fluid leakage channel; the vertical distance of the fluid leakage geological model is equal to the second depth.

[0020] Optionally, the temperature data includes a top boundary temperature of the top boundary and a bottom boundary temperature of the bottom boundary; and establishing a heat convection conduction model based on the fluid leakage geological model and the temperature data of the target location includes the following steps:

[0021] Based on the top boundary temperature and the bottom boundary temperature, the heat convection conduction model is established in combination with the Berkeley number and the vertical distance of the fluid leakage geological model; the vertical distance represents the depth distance between the top boundary and the bottom boundary;

[0022] The heat convection conduction model represents the data relationship between the burial depth and the corresponding depth temperature; the expression of the heat convection conduction model is:

[0023]

[0024] Where, T z represents the depth temperature corresponding to the burial depth z; T0 represents the top temperature; T L represents the bottom temperature; L represents the vertical distance; e is a mathematical constant; β represents the Berkeley number.

[0025] Optionally, performing formation temperature field function transformation based on a heat convection conduction model to obtain a function of geothermal gradient varying with burial depth comprises the following steps:

[0026] Based on the heat convection conduction model, the partial derivative function of the formation temperature field with respect to the burial depth is calculated, and the functional relationship between the geothermal gradient and the burial depth in the heat convection conduction model is established;

[0027] Among them, the expression of the functional relationship is:

[0028]

[0029] Where, The symbol representing the partial derivative function; T represents the symbol for temperature;

[0030] Based on the functional relationship, the burial depth is approximately 0 as a constraint condition to obtain the temperature function of the near-seabed stratum;

[0031] The expression of the temperature function is:

[0032]

[0033] Substitute the temperature function into the functional relationship and obtain the change function through functional transformation;

[0034] The expression of the change function is:

[0035]

[0036] Optionally, obtaining formation temperature measurement data and obtaining a top boundary temperature gradient value of a near-seabed formation based on the formation temperature measurement data may include the following steps:

[0037] Obtain in-situ temperature data and location information of temperature probes in the shallow seabed to obtain formation temperature measurement data;

[0038] The temperature probe is placed on the shallow surface of the seabed by a gravity column carrying multiple temperature probes; the shallow surface of the seabed represents a shallow layer within a preset depth below the seabed position;

[0039] The least squares method is used to perform linear fitting on the in-situ temperature data corresponding to different location information to obtain the apparent geothermal gradient value of the near-seabed stratum, which is used as the top boundary temperature gradient value.

[0040] Optionally, obtaining the formation pressure of the quasi-seafloor reflector layer, solving the hydrate phase equilibrium equation based on the formation pressure to obtain the phase equilibrium temperature at the bottom boundary of the hydrate stability zone, and then combining the measured seafloor temperature at the seafloor location to obtain the average geothermal gradient of the hydrate stability zone, comprises the following steps:

[0041] The underwater depth of the quasi-seafloor reflector is determined based on the fluid seepage geological model, and then the hydrostatic pressure of the quasi-seafloor reflector is calculated based on the pore fluid density of the sedimentary formation. The hydrostatic pressure is used as the formation pressure.

[0042] The fluid seepage geological model includes the seabed depth at the seabed location and the first depth of the seabed-like reflective layer below the seabed location; the underwater depth is obtained based on the sum of the seabed depth and the first depth; and the hydrostatic pressure is obtained by multiplying the underwater depth, the pore fluid density, and the gravitational acceleration.

[0043] The hydrate phase equilibrium simulation function is constructed using the preset phase equilibrium simulation software. The formation pressure is substituted into the hydrate phase equilibrium simulation function to solve and obtain the phase equilibrium temperature at the bottom boundary of the hydrate stability domain.

[0044] Based on the phase equilibrium temperature at the bottom of the hydrate stability zone and the measured seabed temperature at the seabed, the average geothermal gradient of the hydrate stability zone is obtained by partial derivative calculation.

[0045] The expression of the average geothermal gradient is:

[0046]

[0047] Where, represents the symbol of the partial derivative function; T represents the symbol of temperature; z represents the burial depth; T BSR represents the phase equilibrium temperature; T0 represents the measured seabed temperature; Z BSR Indicates the first depth.

[0048] Optionally, the average geothermal gradient is substituted into the variation function, and then the vertical migration rate of the fluid is derived in combination with the Berkeley equation, which includes the following steps:

[0049] Substitute the average effect position point corresponding to the average geothermal gradient into the variation function to obtain the first function;

[0050] The expression of the change function is:

[0051]

[0052] Where, represents the symbol of the partial derivative function; T represents the symbol of temperature; z represents the burial depth; L represents the vertical distance of the heat convection conduction model; e is a mathematical constant; β represents the Berkeley number;

[0053] The expression of the average geothermal gradient is:

[0054]

[0055] Where, T BSR represents the phase equilibrium temperature; T0 represents the measured seabed temperature; ZBSR Indicates the first depth of the seabed-like reflector below the seabed;

[0056] The expression of the first function is:

[0057]

[0058] Where, 0.5Z BSR is the average effect location point;

[0059] Substituting Berkeley's equation into the first function yields the second function;

[0060] The expression of Berkeley's equation is:

[0061]

[0062] Where φ represents the formation porosity; ρ w represents the density of sediment pore fluid; C w represents the heat capacity of sediment pore fluid; V z represents the vertical migration rate of fluid; λ represents the average thermal conductivity of formation sediment;

[0063] The expression of the second function is:

[0064]

[0065] The measured parameters are introduced into the second function to derive the vertical migration rate of the fluid; the measured parameters include the measured values ​​of formation porosity, sediment pore fluid density, sediment pore fluid heat capacity and average thermal conductivity of formation sediments.

[0066] On the other hand, an embodiment of the present invention provides an analysis and processing device for the flow rate of shallow seabed fluid, comprising:

[0067] The first module is used to obtain the seismic reflection time of the target location in the seismic profile of the target area and establish a fluid leakage geological model based on the seismic reflection time; the target location includes the seabed location, the seabed-like reflection layer and the root location of the fluid leakage channel; the top boundary of the fluid leakage geological model is the seabed location, and the bottom boundary of the fluid leakage geological model is the root location of the fluid leakage channel;

[0068] The second module is used to establish a heat convection conduction model based on the fluid leakage geological model and the temperature data of the target location;

[0069] The third module is used to transform the formation temperature field function based on the heat convection conduction model to obtain the function of the change of geothermal gradient with burial depth;

[0070] The fourth module is used to obtain formation temperature measurement data, and obtain the top boundary temperature gradient value of the near-seabed formation based on the formation temperature measurement data; the near-seabed formation represents the top boundary of the fluid leakage geological model;

[0071] The fifth module is used to obtain the formation pressure of the seabed-like reflector layer. Based on the formation pressure, the hydrate phase equilibrium equation is solved to obtain the phase equilibrium temperature at the bottom boundary of the hydrate stability zone. This is then combined with the measured seabed temperature to obtain the average geothermal gradient of the hydrate stability zone.

[0072] The sixth module is used to substitute the average geothermal gradient into the variation function, and then combine it with the Berkeley equation to derive the vertical migration rate of the fluid.

[0073] On the other hand, an embodiment of the present invention provides an electronic device, comprising: a processor and a memory; the memory is used to store programs; the processor executes the program to implement the above-mentioned method for analyzing and processing the activity rate of shallow seabed fluid.

[0074] On the other hand, an embodiment of the present invention provides a computer storage medium storing a program executable by a processor. When the program is executed by the processor, it is used to implement the above-mentioned method for analyzing and processing the activity rate of shallow seabed fluid.

[0075] The embodiment of the present invention obtains seismic reflection times at target locations in a seismic profile of a target area and establishes a fluid seepage geological model based on the seismic reflection times. The target locations include the seafloor, a quasi-seafloor reflector, and the root of the fluid seepage channel. The top boundary of the fluid seepage geological model is the seafloor, and the bottom boundary of the fluid seepage geological model is the root of the fluid seepage channel. A heat convection conduction model is established based on the fluid seepage geological model and temperature data of the target location. A formation temperature field function is transformed based on the heat convection conduction model to obtain a function of geothermal gradient variation with burial depth. Formation temperature measurement data is obtained and, based on the formation temperature measurement data, a temperature gradient value at the top boundary of the near-seafloor formation is obtained. The near-seafloor formation represents the top boundary of the fluid seepage geological model. The formation pressure of the quasi-seafloor reflector is obtained and, based on the formation pressure, the hydrate phase equilibrium equation is solved to obtain the phase equilibrium temperature at the bottom boundary of the hydrate stability zone. This is then combined with the measured seafloor temperature at the seafloor to obtain the average geothermal gradient of the hydrate stability zone. The average geothermal gradient is substituted into the variation function and, combined with the Berkeley equation, the vertical migration rate of the fluid is derived. The present invention is guided by the basic theories of fluid kinematics and thermodynamics, fully leveraging the parameter advantage of the "temperature" factor. By establishing a heat convection conduction model, relying on the measured geothermal data of near-seabed strata with low acquisition costs, and combining the geothermal data of the hydrate stability zone obtained by hydrate phase equilibrium simulation and quasi-seabed reflector inversion, the average geothermal gradient in the hydrate stability zone near the seabed strata and below the seabed is calculated. Finally, the vertical migration rate of shallow seabed fluid is calculated using the Berkeley (Pe) equation, providing a basis for revealing the activity behavior of shallow seabed fluids and assessing the potential ecological environment and geological disaster impacts. The embodiments of the present invention can conveniently and accurately analyze and process the activity rate of shallow seabed fluids. BRIEF DESCRIPTION OF THE DRAWINGS

[0076] The accompanying drawings are used to provide a further understanding of the technical solution of the present invention and constitute a part of the specification. Together with the embodiments of the present invention, they are used to explain the technical solution of the present invention and do not constitute a limitation to the technical solution of the present invention.

[0077] Figure 1 This is a schematic diagram of an implementation environment for analyzing and processing the flow rate of shallow seabed fluids provided by an embodiment of the present invention;

[0078] Figure 2 This is a flow chart of a method for analyzing and processing the flow rate of shallow seabed fluid provided by an embodiment of the present invention;

[0079] Figure 3 A schematic diagram of a fluid flow geological model established based on seismic profile characteristics provided by an embodiment of the present invention;

[0080] Figure 4 A schematic diagram of the expanded flow of step S400 provided in an embodiment of the present invention;

[0081] Figure 5 A schematic diagram of a data relationship curve for calculating the phase equilibrium temperature at the bottom boundary of the hydrate stability region through phase equilibrium simulation provided in an embodiment of the present invention;

[0082] Figure 6 A schematic diagram of a data relationship curve for calculating the boundary geothermal gradient of a fluid leakage model provided in an embodiment of the present invention;

[0083] Figure 7 A schematic diagram of a data relationship curve for calculating the vertical migration rate of formation fluids using the Pe (Berkeley) equation provided in an embodiment of the present invention;

[0084] Figure 8 A schematic diagram of the overall process of a method for analyzing and processing the flow rate of shallow seabed fluid provided by an embodiment of the present invention;

[0085] Figure 9 A schematic structural diagram of a device for analyzing and processing the flow rate of shallow seabed fluids provided by an embodiment of the present invention;

[0086] Figure 10 A schematic structural diagram of an electronic device provided by an embodiment of the present invention. DETAILED DESCRIPTION

[0087] In order to make the purpose, technical solutions and advantages of the present invention more clearly understood, the present invention will be further described in detail below with reference to the accompanying drawings and embodiments. It should be understood that the specific embodiments described herein are only used to explain the present invention and are not intended to limit the present invention.

[0088] It should be noted that although the system diagrams illustrate functional module divisions and the flowcharts illustrate a logical sequence, in certain circumstances, the steps shown or described may be performed in a sequence that differs from the module divisions in the system or the sequence in the flowcharts. The terms "first / S100," "second / S200," and the like in the specification, claims, and drawings are used to distinguish similar objects and are not necessarily intended to describe a specific sequence or precedence.

[0089] References herein to "embodiments" mean that a particular feature, structure, or characteristic described in connection with the embodiments may be included in at least one embodiment of the present invention. The appearance of this phrase in various places in the specification does not necessarily refer to the same embodiment, nor does it constitute a separate or alternative embodiment that is mutually exclusive of other embodiments. It is understood, both explicitly and implicitly, by those skilled in the art that the embodiments described herein may be combined with other embodiments.

[0090] To facilitate understanding of the technical solutions of the present invention, the meanings of the parameters that may be cited in the embodiments of the present invention and their technical principles are first explained:

[0091] Hydrate: A mineral crystal formed by the combination of water molecules and gas molecules under low temperature and high pressure conditions. It is often found in marine environments or terrestrial permafrost zones and is a potential clean energy source with huge energy (hydrates in this invention specifically refer to hydrates in marine environments).

[0092] BSR: Bottom Simulation Reflection, representing the reflective interface between hydrate-bearing sediments and the underlying hydrate-free layer. The BSR is an important indicator of hydrate occurrence in geophysical exploration and also serves as a thermodynamic interface. It is generally believed that the area above the BSR lies within the hydrate stability zone, where hydrates can stably exist. The area below the BSR is beyond the hydrate stability zone and cannot stably exist.

[0093] Hydrate phase equilibrium curve: usually expressed in the form of a pressure (P)-temperature (T) diagram, it refers to the equilibrium state of coexistence of hydrate (solid phase), liquid water and free gas under specific temperature and pressure conditions. The hydrate phase equilibrium curve is the equilibrium boundary between the hydrate stable zone and the unstable zone.

[0094] The hydrate stability zone refers to a specific area below the seafloor where the temperature and pressure conditions are within the thermodynamically stable range for hydrate formation. The bottom of the hydrate stability zone is numerically equal to the intersection of the geothermal gradient line and the hydrate phase equilibrium curve. The hydrate stability zone is primarily controlled by geological factors such as seawater depth, seafloor temperature and pressure, geothermal gradient, pore fluid salinity, and natural gas alkane composition.

[0095] Gas chimneys: A geophysical manifestation of gas in sedimentary strata, resembling a chimney. Gas chimneys are important pathways for the migration of gaseous fluids from deep layers to shallower layers. This migration is accompanied by significant heat transfer, leading to changes in the shallow seabed geothermal field. The shape and size of gas chimneys can be used to qualitatively infer the intensity of gaseous fluid activity and the degree of disturbance to the geothermal field.

[0096] Geothermal Field: The geothermal field is the manifestation of Earth's internal heat energy through rocks of varying thermal conductivity, reflected in the Earth's crust. Beneath the Earth's surface, the ground temperature increases regularly with depth, meaning that each increase in depth results in a corresponding increase in ground temperature.

[0097] Geothermal gradient: A parameter that measures the vertical transfer rate of stratum temperature, usually expressed as the degree of temperature drop per kilometer (℃ / km).

[0098] Thermal conductivity, also known as thermal conductivity or thermal conductivity, is the amount of heat transferred per unit temperature gradient through a unit heat conducting surface per unit time, expressed in W / (m·K). Sediment thermal conductivity is directly or indirectly related to lithology, geological age, burial depth, and compaction. Deep-sea sediment thermal conductivity is primarily related to hydrostatic pressure, sediment compaction, and the resulting changes in porosity.

[0099] Heat transfer refers to the physical phenomenon of the transfer of thermal energy due to temperature differences. There are three basic forms of heat transfer: conduction, radiation, and convection. Conduction occurs when there is no macroscopic motion within a medium and can occur in solids, liquids, and gases. Strictly speaking, pure conduction occurs only in solids; convection is the process by which energy is transferred from a higher temperature area to a lower temperature area through the flow of liquids or gases. In shallow seabed geology, energy transfer in deep strata occurs primarily through conduction and convection.

[0100] The Peclet Number (Pe) represents the ratio of convection to diffusion in a fluid gradient. In fluid theory, the larger the Pe, the more significant the role of convection in fluid migration.

[0101] It is understandable that the analysis and processing method for the shallow seabed fluid activity rate provided by the embodiment of the present invention can be applied to any computer device with data processing and computing capabilities, and this computer device can be various terminals or servers. When the computer device in the embodiment is a server, the server is an independent physical server, or a server cluster or distributed system composed of multiple physical servers, or a cloud server that provides basic cloud computing services such as cloud services, cloud databases, cloud computing, cloud functions, cloud storage, network services, cloud communications, middleware services, domain name services, security services, CDN (Content Delivery Network), and big data and artificial intelligence platforms. Optionally, the terminal is a smart phone, tablet computer, laptop computer, desktop computer, etc., but is not limited to this.

[0102] To facilitate understanding of the technical solutions of the present invention, the following are first explained regarding the technical features that may appear in the embodiments of the present invention:

[0103] like Figure 1 FIG. 1 is a schematic diagram of an implementation environment provided by an embodiment of the invention. Figure 1 , the implementation environment includes at least one terminal 102 and a server 101. The terminal 102 and the server 101 can be connected to the network in a wireless or wired manner to complete data transmission and exchange.

[0104] Server 101 can be an independent physical server, or a server cluster or distributed system composed of multiple physical servers. It can also be a cloud server that provides basic cloud computing services such as cloud services, cloud databases, cloud computing, cloud functions, cloud storage, network services, cloud communications, middleware services, domain name services, security services, CDN (Content Delivery Network), as well as big data and artificial intelligence platforms.

[0105] In addition, server 101 can also be a node server in a blockchain network. Blockchain is a new application model of computer technologies such as distributed data storage, peer-to-peer transmission, consensus mechanism, and encryption algorithm.

[0106] The terminal 102 may be a smart phone, tablet computer, laptop computer, desktop computer, smart speaker, smart watch, etc., but is not limited thereto. The terminal 102 and the server 101 may be connected directly or indirectly via wired or wireless communication, which is not limited in this embodiment of the present invention.

[0107] Based on the example Figure 1 In the implementation environment shown, an embodiment of the present invention provides a method for analyzing and processing the activity rate of shallow seabed fluid. The following is explained using the example of applying the analysis and processing method of the activity rate of shallow seabed fluid in server 101. It can be understood that the analysis and processing method of the activity rate of shallow seabed fluid can also be applied to terminal 102.

[0108] Reference Figure 2 , Figure 2 The flowchart of the method for analyzing and processing the rate of shallow seabed fluid activity applied to the server provided in the embodiment of the present invention, the execution subject of the method for analyzing and processing the rate of shallow seabed fluid activity can be any of the aforementioned computer devices (including servers or terminals). Figure 2 , the method comprises the following steps:

[0109] S100, obtaining the seismic reflection time of the target position in the seismic profile of the target area, and establishing a fluid leakage geological model based on the seismic reflection time;

[0110] The target locations include the seabed, the quasi-seabed reflector, and the root of the fluid leakage channel. The top boundary of the fluid leakage geological model is the seabed, and the bottom boundary of the fluid leakage geological model is the root of the fluid leakage channel.

[0111] It should be noted that the seismic reflection time includes the first reflection time of the seabed position, the second reflection time of the seabed-like reflection layer, and the third reflection time of the root position of the fluid leakage channel; in some embodiments, establishing a fluid leakage geological model based on the seismic reflection time may include the following steps: obtaining the seabed depth of the seabed position according to half of the product of the first reflection time and the first velocity; the first velocity represents the propagation speed of seismic waves in seawater; obtaining the first depth according to half of the product of the difference between the second reflection time and the first reflection time and the second velocity; the second velocity represents the propagation speed of seismic waves in the shallow seabed; the first depth represents the depth of the seabed-like reflection layer below the seabed position; the second depth is obtained according to half of the product of the difference between the third reflection time and the first reflection time and the second velocity; the second depth represents the depth of the root position of the fluid leakage channel below the seabed position; establishing a fluid leakage geological model based on the seabed depth, the first depth, and the second depth; wherein, the top boundary of the fluid leakage geological model is the seabed position, and the bottom boundary of the fluid leakage geological model is the root position of the fluid leakage channel; the vertical distance of the fluid leakage geological model is equal to the second depth.

[0112] For example, in some specific implementations, taking a specific embodiment with typical fluid leakage characteristics as an example:

[0113] In the seismic profile, read the seismic reflection time corresponding to the seismic reflection event axis at the seabed position, recorded as t0, unit s;

[0114] In the seismic profile, read the seismic reflection time corresponding to the BSR position, which is recorded as t BSR , unit s;

[0115] In the seismic profile, the seismic reflection time corresponding to the root position of the fluid leakage channel (such as gas chimney, tubular channel, mud diapir / mud volcano) (i.e., the position where the fluid begins to leak or diffuse) is read and recorded as t L , unit s;

[0116] In a specific embodiment, the propagation speed of seismic waves in seawater is v=1500 m / s; the propagation speed of seismic waves in the shallow seabed is v=1600 m / s.

[0117] Specifically, the seabed depth D sea (i.e. water depth), BSR burial depth Z below the seabed BSR , the depth L of the root of the fluid leakage channel is recorded as:

[0118] D sea =(1500* t0) / 2 (1)

[0119] Z BSR =1600*(t BSR - t0) / 2, (2)

[0120] L=1600*(t L -t0) / 2, (3)

[0121] Based on the above parameters, a gas-bearing fluid leakage geological model is established. The geological model environment is set as a stratum that is permeable to both heat and fluid, and the heat and fluid migration directions are both vertical. The seabed is used as the top boundary of the fluid leakage geological model, and the root position of the fluid leakage channel is used as the bottom boundary of the fluid leakage geological model. The model height, that is, the vertical distance between the "top boundary" and the "bottom boundary", is L (e.g. Figure 3 shown).

[0122] S200, establishing a heat convection conduction model based on the fluid leakage geological model and temperature data of the target location;

[0123] It should be noted that the temperature data includes the top boundary temperature of the top boundary and the bottom boundary temperature of the bottom boundary; in some embodiments, step S200 may include the following steps: based on the top boundary temperature and the bottom boundary temperature, combined with the Berkeley number and the vertical distance of the fluid leakage geological model, a heat convection conduction model is established; the vertical distance represents the depth distance between the top boundary and the bottom boundary; wherein the heat convection conduction model represents the data relationship between the burial depth and the corresponding depth temperature; the expression of the heat convection conduction model is:

[0124]

[0125] Where, T z represents the depth temperature corresponding to the burial depth z; T0 represents the top temperature; T L represents the bottom temperature; L represents the vertical distance; e is a mathematical constant; β represents the Berkeley number.

[0126] For example, in some specific implementations, a one-dimensional thermal convection conduction numerical model of the temperature field is established based on the geological model, which is expressed as:

[0127]

[0128] In formula 4:

[0129] L: height of the heat convection conduction model, m;

[0130] z: Depth at any position z in the heat convection conduction model (z≤L), m;

[0131] T0: seafloor temperature, i.e., the top temperature of the heat convection conduction model;

[0132] T L : bottom temperature of the heat convection conduction model, °C;

[0133] T Z: temperature at depth z in the heat convection conduction model, °C;

[0134] β: Pe (Berkeley number).

[0135] Specifically, the seabed temperature T0 is measured by carrying a temperature probe on a gravity column, and the data is recorded and stored in the form of electronic documents. The data can be directly retrieved for numerical calculations.

[0136] S300, performing formation temperature field function transformation based on a heat convection conduction model to obtain a function of geothermal gradient varying with burial depth;

[0137] It should be noted that, in some embodiments, step S300 may include the following steps:

[0138] Based on the heat convection conduction model, the partial derivative function of the formation temperature field with respect to the burial depth is calculated, and the functional relationship between the geothermal gradient and the burial depth in the heat convection conduction model is established;

[0139] Among them, the expression of the functional relationship is:

[0140]

[0141] Where, The symbol representing the partial derivative function; T represents the symbol for temperature;

[0142] Based on the functional relationship, the burial depth is approximately 0 as a constraint condition to obtain the temperature function of the near-seabed stratum;

[0143] The expression of the temperature function is:

[0144]

[0145] Substitute the temperature function into the functional relationship and obtain the change function through functional transformation;

[0146] The expression of the change function is:

[0147]

[0148] For example, in some specific implementations, the partial derivative function of the formation temperature field with respect to the burial depth is calculated, and the functional relationship between the geothermal gradient and the burial depth of the heat convection conduction model is established, which is expressed as:

[0149]

[0150] For the near-seafloor strata (i.e., the top boundary of the geological model, when the burial depth z≈0), Formula 5 is expressed as:

[0151]

[0152] Substituting formula 6 into formula 5 and replacing some constant terms on the right side of the equation, we get:

[0153]

[0154] Further functional transformation of Formula 7 yields Formula 8:

[0155]

[0156] S400, obtaining formation temperature measurement data, and obtaining a top boundary temperature gradient value of a near-seabed formation based on the formation temperature measurement data;

[0157] Among them, the near-seafloor strata represent the top boundary of the fluid seepage geological model;

[0158] It should be noted that, in some embodiments, Figure 4 As shown, step S400 may include the following steps: S401, obtaining in-situ temperature data and position information of a temperature probe of the shallow layer of the seabed to obtain formation temperature measurement data; wherein, the temperature probe is carried and placed in the shallow layer of the seabed by a gravity column, and the gravity column carries multiple temperature probes; the shallow layer of the seabed represents the shallow stratum within a preset depth below the seabed position; S402, using the least squares method to perform linear fitting on the in-situ temperature data corresponding to different position information to obtain the apparent geothermal gradient value of the near-seabed stratum, and the apparent geothermal gradient value is used as the top boundary temperature gradient value.

[0159] For example, in some specific embodiments, the geothermal gradient of the near-seabed formation, that is, the geothermal gradient of the top boundary of the model, is expressed as express.

[0160] Specifically, the geothermal gradient of the near-seabed formation is obtained by collecting in-situ temperature data of the shallow seabed layer (generally the shallow layer within 5m below the seabed) through a gravity column carrying a temperature probe. Combined with the position information of the temperature probe, the least squares method is used to perform a linear fit on the in-situ formation temperature at different burial depths of the near-seabed formation to obtain the apparent geothermal gradient value of the near-seabed formation, which is recorded as:

[0161]

[0162] Where, T i , T k are the measured formation temperatures of the near-seafloor strata recorded by the i-th and k-th temperature probes carried by the gravity column, respectively;

[0163] Where, X i , X k are the depths below the seabed where the i-th and k-th temperature probes carried by the gravity column are located.

[0164] Specifically, i,k is generally less than 6, that is, the number of temperature probes carried by the gravity column is generally less than 6;

[0165] Specifically, X i , X k Generally less than 5m, that is, the temperature probe carried by the gravity column penetrates into the seabed to a depth of less than 5m;

[0166] Specifically, during the temperature measurement of near-seabed formations, temperature probes are installed on gravity sampling tubes at different angles and fixed spacing values. The relative distances between the temperature probes are measured before and after entering the water to ensure that the temperature probes do not shift.

[0167] Specifically, since the temperature measurement probe may not be completely upright when penetrating into the sediment, but may be at a certain angle to the vertical direction, it is necessary to perform inclination correction of the temperature measurement probe in order to calculate the actual geothermal gradient value.

[0168] Specifically, the temperature measurement probe position information, the measured in-situ temperature information, and the temperature measurement probe inclination information all come from field measurement records and are stored in the form of electronic documents. The data information can be directly retrieved for numerical calculations.

[0169] S500, obtaining the formation pressure of the seabed-like reflector layer, solving the hydrate phase equilibrium equation based on the formation pressure to obtain the phase equilibrium temperature of the bottom boundary of the hydrate stability zone, and then combining it with the measured seabed temperature at the seabed location to obtain the average geothermal gradient of the hydrate stability zone;

[0170] It should be noted that, in some embodiments, step S500 may include the following steps: determining the underwater depth of the seabed-like reflective layer based on the fluid seepage geological model, and then calculating the hydrostatic pressure of the seabed-like reflective layer in combination with the pore fluid density of the sedimentary formation; and using the hydrostatic pressure as the formation pressure;

[0171] The fluid seepage geological model includes the seabed depth at the seabed location and the first depth of the seabed-like reflective layer below the seabed location; the underwater depth is obtained based on the sum of the seabed depth and the first depth; and the hydrostatic pressure is obtained by multiplying the underwater depth, the pore fluid density, and the gravitational acceleration.

[0172] The hydrate phase equilibrium simulation function is constructed using the preset phase equilibrium simulation software. The formation pressure is substituted into the hydrate phase equilibrium simulation function to solve and obtain the phase equilibrium temperature at the bottom boundary of the hydrate stability domain.

[0173] Based on the phase equilibrium temperature at the bottom of the hydrate stability zone and the measured seabed temperature at the seabed, the average geothermal gradient of the hydrate stability zone is obtained by partial derivative calculation.

[0174] The expression of the average geothermal gradient is:

[0175]

[0176] Where, represents the symbol of the partial derivative function; T represents the symbol of temperature; z represents the burial depth; T BSR represents the phase equilibrium temperature; T0 represents the measured seabed temperature; Z BSR Indicates the first depth.

[0177] For example, in some specific embodiments, the formation pressure at the BSR position is calculated, and then the bottom boundary phase equilibrium temperature of the hydrate stability domain is calculated by solving the hydrate phase equilibrium equation (i.e., the PT equation).

[0178] Specifically, the formation pressure at the BSR position is approximately equal to the hydrostatic pressure at that position, which is expressed as:

[0179] P BSR =ρ*g*H=ρ*g*(D sea +Z BSR ) (10)

[0180] Where, ρ: pore fluid density of sedimentary formation, 1035 kg / m 3 ;

[0181] g: acceleration due to gravity, 9.8 m / s 2 ;

[0182] D sea : depth of overlying seawater, m;

[0183] Z BSR : burial depth of the BSR below the seabed, m.

[0184] Specifically, the phase equilibrium simulation software CSMGEM was used to carry out numerical simulation calculations on the bottom boundary of the hydrate stability region. By inputting parameters such as the alkane gas composition of the hydrate decomposition gas and the salinity of the pore water, a hydrate phase equilibrium simulation function was constructed. The formation pressure P at the BSR position obtained based on Formula 10 was converted to BSR Substitute into the hydrate phase equilibrium simulation function to obtain the formation temperature at the BSR position, that is, the phase equilibrium temperature T at the bottom boundary of the hydrate stability region BSR (like Figure 5 shown).

[0185] Specifically, the alkane gas composition of hydrate decomposition gas and pore water salinity testing work are completed on-site during the hydrate drilling voyage. The corresponding test data are stored in the form of electronic documents, and the data can be directly retrieved for numerical simulation calculations.

[0186] Specifically, according to the measured seabed temperature T0 and the bottom phase equilibrium temperature of the hydrate stability zone T BSR, calculate the average geothermal gradient of the hydrate stability zone (such as Figure 6 As shown), recorded as:

[0187]

[0188] S600. Substitute the average geothermal gradient into the variation function and then combine it with the Berkeley equation to derive the vertical migration rate of the fluid.

[0189] It should be noted that, in some embodiments, step S600 may include the following steps: substituting the average effect position point corresponding to the average geothermal gradient into the variation function to obtain a first function; wherein the variation function is expressed as:

[0190]

[0191] Where, represents the symbol of the partial derivative function; T represents the symbol of temperature; z represents the burial depth; L represents the vertical distance of the heat convection conduction model; e is a mathematical constant; β represents the Berkeley number;

[0192] The expression of the average geothermal gradient is:

[0193]

[0194] Where, T BSR represents the phase equilibrium temperature; T0 represents the measured seabed temperature; Z BSR Indicates the first depth of the seabed-like reflector below the seabed;

[0195] The expression of the first function is:

[0196]

[0197] Where, 0.5Z BSR is the average effect location point;

[0198] Substituting Berkeley's equation into the first function yields the second function;

[0199] The expression of Berkeley's equation is:

[0200]

[0201] Where φ represents the formation porosity; ρ w represents the density of sediment pore fluid; C w represents the heat capacity of sediment pore fluid; V z represents the vertical migration rate of fluid; λ represents the average thermal conductivity of formation sediment;

[0202] The expression of the second function is:

[0203]

[0204] The measured parameters are introduced into the second function to derive the vertical migration rate of the fluid; the measured parameters include the measured values ​​of formation porosity, sediment pore fluid density, sediment pore fluid heat capacity and average thermal conductivity of formation sediments.

[0205] For example, in some specific embodiments, the geothermal gradient derived from Formula 11 is is the average geothermal gradient value of the hydrate stability zone, and its value is half of the hydrate stability zone, that is, the average effect position point is 0.5Z BSR .

[0206] In a specific embodiment, according to the model boundary conditions, Formula 8 is expressed as:

[0207]

[0208] Combined with the definition formula of Pe (Berkeley) equation:

[0209]

[0210] The specific expression of formula 12 is as follows:

[0211]

[0212] In formula 14:

[0213] The geothermal gradient value of the near-seabed stratum, °C / km, is calculated using Formula 9;

[0214] The average geothermal gradient in the hydrate stability zone, °C / km, is calculated using Equation 11;

[0215] Z BSR : Depth of the BSR below the seabed, m, calculated by Equation 2;

[0216] ρ w : Sediment pore fluid density, 1035kg / m 3 ;

[0217] C w : Sediment pore fluid heat capacity, 4186 J·kg -1 ·K -1 ;

[0218] φ: formation porosity, dimension is 1;

[0219] λ: average thermal conductivity of stratum sediments, W·m -1 ·K -1 ;

[0220] V z : vertical migration rate of fluid in the heat convection conduction model, m / s;

[0221] Specifically, the formation porosity φ can be calculated using sonic logging, density logging, or neutron porosity logging curves obtained by hydrate logging while drilling.

[0222] Specifically, the average thermal conductivity λ of the sediment can be obtained by conducting thermal conductivity tests on sediment samples obtained by gravity piston sampling and hydrate drilling.

[0223] V z As the only variable to be solved, the vertical migration rate of the fluid is obtained by numerical calculation using formula 14 (e.g. Figure 7 shown).

[0224] In order to explain the principle of the technical solution of the present invention in detail, the overall process of the present invention is described below in combination with some specific embodiments. It is easy to understand that the following is an explanation of the technical principle of the present invention and cannot be regarded as a limitation of the present invention.

[0225] First, it's important to note that while direct survey and observation methods for determining fluid migration rates are highly reliable, they are not practical for large-scale deployment due to the substantial costs of offshore operations and the high geological, engineering, and environmental risks. Existing technical solutions (such as the following example) are often guided by fundamental principles of fluid mechanics. Relying on existing survey data, they indirectly estimate fluid activity intensity and migration rates through numerical simulations, providing key scientific parameters for guiding deep oil and gas exploration.

[0226] Fluid migration rates are primarily determined through direct survey observations or indirect numerical simulations. While highly reliable, survey observations have significant drawbacks, including high costs, long observation cycles, and potential geological, engineering, and environmental risks, hindering their widespread application. However, existing numerical simulation techniques also have drawbacks and limitations, primarily in the following three areas:

[0227] (1) The existing technical solutions are mainly targeted at deep strata (usually buried at a depth of several thousand meters below the seabed), and focus on the "secondary migration" of liquid petroleum hydrocarbons in consolidated rocks and the accumulation process in the dominant reservoir. Compared with the fluid activity behavior of shallow seabed strata with the characteristics of "shallow burial depth" (usually buried less than 200m below the seabed), "loose and unconsolidated", "developed pore structure" and "active fluid microleakage", the two have obvious differences in fluid migration conditions, driving mechanisms and numerical simulation methods, resulting in the limitations of the existing technical solutions when applied to the study of shallow seabed fluid activity.

[0228] (2) Existing technical solutions usually use formation "pressure" factors, especially fluid overpressure factors, as key control variables for geological modeling and fluid migration rate calculations. However, for shallow seabed sediments, the pore fluid pressure is almost the same as the hydrostatic pressure, and there is no significant formation overpressure effect. In addition, shallow seabed fluid activity is mostly micro-seepage, and the intensity of fluid activity is significantly weaker than that of deep fluids. Therefore, the existing solutions based on formation pressure factors for modeling and estimating the direction of formation fluid activity and migration rate through "overpressure" anomalies are no longer applicable.

[0229] (3) Existing technical solutions and numerical simulation methods involve many types of parameters, and key geological parameters such as "formation pressure", "deep rock permeability", "rock density", etc. need to be obtained through deep well drilling, coring testing, etc. Due to the difficulty of collection and the high cost of parameter acquisition, they are not suitable for large-scale application.

[0230] Taking into account the limitations of existing technical methods in terms of application conditions, the present invention focuses on the leakage behavior of gas-bearing fluids in shallow submarine strata (generally less than 200 meters below the seabed, generally located within the hydrate stability zone). Based on the fact that the migration of gas-bearing hot fluids causes deep material energy migration and disturbance of the shallow submarine geothermal field, guided by the basic theories of fluid kinematics and thermodynamics, the parameter advantages of the "temperature" factor are fully utilized. By establishing a one-dimensional heat convection conduction model of the temperature field, relying on the measured geothermal data of near-seabed strata with low acquisition cost, and combining the geothermal data of the hydrate stability zone obtained by hydrate phase equilibrium simulation and BSR inversion, the average geothermal gradient in the near-seabed strata and the hydrate stability zone below the seabed is calculated. Finally, the Berkeley (Pe) equation is used to calculate the vertical migration rate of shallow submarine fluids, providing a basis for revealing the activity behavior of shallow submarine fluids and assessing the potential impact of ecological environment and geological disasters.

[0231] In some specific application scenarios, such as Figure 8 As shown, the technical solution of the present invention can be implemented as follows:

[0232] Step 1: Establish a geological model of gas-bearing fluid leakage and determine the model boundary conditions based on seismic reflection characteristics.

[0233] In this embodiment, a typical fluid leakage activity area in a certain sea area is taken as the research object.

[0234] Specifically, in a specific embodiment of developing deep gas chimney activity, exemplary,

[0235] In the seismic profile, the seismic reflection time t0 at the seabed position is read: 2.56s;

[0236] In the seismic profile, read the seismic reflection time t at the BSR position BSR: 2.75s;

[0237] In the seismic profile, read the seismic reflection time t at the root of the gas chimney L : 3.5s.

[0238] According to the propagation speed of seismic waves in seawater v = 1500m / s and the propagation speed of seismic waves in the shallow seabed v = 1600m / s, the seabed depth (i.e., water depth), the burial depth of BSR below the seabed, and the root depth of the fluid leakage channel are calculated respectively:

[0239] D sea =(1500*t0) / 2=(1500*2.56) / 2=1920m (1)

[0240] Z BSR =1600*(t BSR -t0) / 2=1600*(2.75-2.56) / 2=152m (2)

[0241] L=1600*(t L -t0) / 2=1600*(3.5-2.56) / 2=752m (3)

[0242] According to the calculated D sea , Z BSR , L and other parameter values ​​are used to establish a gas-bearing fluid leakage geological model. The geological model environment is a formation that is permeable to both heat and fluid, and the directions of heat and fluid migration are both vertical.

[0243] The height L of the established geological model is 752m, and the BSR is located 152m below the top boundary of the geological model.

[0244] Step 2: Based on the geological model, establish a one-dimensional thermal convection conduction numerical model of the temperature field.

[0245] In a specific embodiment of deep gas chimney activity, a one-dimensional thermal convection conduction numerical model of the temperature field is established based on the geological model, which is expressed as:

[0246]

[0247] Substituting the geological model parameters calculated based on step 1 into formula 4, the numerical model expression of the one-dimensional thermal convection conduction temperature field is obtained as follows:

[0248]

[0249] In formula 4-1,

[0250] L: height of one-dimensional heat convection conduction model, 752m;

[0251] z: Depth of any position z in the heat convection conduction model (z≤752m), m;

[0252] T0: seafloor temperature, i.e., the top temperature of the heat convection conduction model, 2.64°C;

[0253] T L : bottom temperature of the heat convection conduction model, °C;

[0254] T z : formation temperature at depth z in the heat convection conduction model, °C;

[0255] β is the value of Pe (Berkeley number), and its dimension can be 1.

[0256] Specifically, in this embodiment, the seabed temperature T0 is measured by a temperature probe carried by a gravity column, and the data is recorded and stored in the form of an electronic document, and the data is directly retrieved for numerical calculation.

[0257] Step 3: Carry out geothermal field function transformation to obtain the function of geothermal gradient changing with burial depth.

[0258] In this embodiment, by calculating the partial derivative function of the formation temperature field with respect to the burial depth, a functional relationship between the geothermal gradient and the burial depth in the heat convection conduction model is established, which is as follows:

[0259]

[0260] Substituting the geological model parameters calculated based on step 1 into formula 5, the functional relationship between the geothermal gradient and the burial depth of the heat convection conduction model is obtained as follows:

[0261]

[0262] For the near-seafloor strata (i.e., the top boundary of the geological model, when the burial depth z≈0), Formula 5-1 is expressed as

[0263]

[0264] Substituting formula 6 into formula 5-1 and replacing some constant terms on the right side of the equation, we get:

[0265]

[0266] Further functional transformation of formula 7 gives formula 8

[0267]

[0268] Step 4: Calculate the geothermal gradient value of the near-seabed formation based on the formation temperature measurement data.

[0269] In this embodiment, the geothermal gradient of the near-seabed formation, i.e., the geothermal gradient of the top boundary of the model, is expressed as express.

[0270] Specifically, the geothermal gradient of the near-seabed stratum is obtained by collecting in-situ temperature data of the shallow seabed layer (generally the stratum shallower than 5m below the seabed) through a gravity column carrying a temperature probe. Combined with the position information of the temperature probe, the least squares method is used to perform linear fitting on the in-situ stratum temperature at different burial depths of the near-seabed stratum to obtain the geothermal gradient of the near-seabed stratum.

[0271]

[0272] In this embodiment, the in-situ temperature information of the near-seabed formation recorded by the temperature probe carried by the gravity column is: T1: 2.809°C; T2: 2.893°C; T3: 2.986°C; T4: 3.064°C; T5: 3.154°C; and T6: 3.248°C. T1, T2, T3, T4, T5, and T6 are the measured formation temperatures of the near-seabed formation recorded by the 1st, 2nd, 3rd, 4th, 5th, and 6th temperature probes carried by the gravity column, respectively.

[0273] In this example, the burial depth information recorded by the temperature probes carried by the gravity column is: X1: 1.025m; X2: 1.825m; X3: 2.625m; X4: 3.425m; X5: 4.225m; X6: 5.025m. X1, X2, X3, X4, X5, and X6 are the depths below the seabed where the first, second, third, fourth, fifth, and sixth temperature probes carried by the gravity column are located, respectively.

[0274] Based on formula 9, the apparent geothermal gradient of the near-seabed formation is obtained by linear fitting.

[0275] Specifically, during the near-seafloor formation temperature measurement process, temperature probes were installed on the gravity sampling tube at various angles and fixed spacings, secured with screws. The relative distances between the temperature probes were measured before and after immersion in the water to ensure that the probes had not shifted.

[0276] Specifically, since the temperature measuring probe has a certain angle with the vertical direction when it penetrates the seabed sediment, the actual geothermal gradient of the near-seabed stratum is obtained after the temperature measuring probe inclination angle is corrected.

[0277] Specifically, the temperature measurement probe position information, the measured in-situ temperature information, and the temperature measurement probe inclination information all come from field measurement records and are stored in the form of electronic documents. The data information can be directly retrieved for numerical calculations.

[0278] Step 5: Estimate the equilibrium temperature of the hydrate bottom phase based on the BSR burial depth and calculate the average geothermal gradient value of the hydrate stability zone.

[0279] In this embodiment, the formation pressure at the BSR position in the model is calculated, and the hydrate phase equilibrium equation (ie, the PT equation) is solved to calculate the bottom boundary phase equilibrium temperature of the hydrate stability region.

[0280] In this embodiment, the formation pressure at the BSR position is approximately equal to the hydrostatic pressure at that position, which is expressed as:

[0281] P BSR =ρ*g*H=ρ*g*(D sea +Z BSR ) (10)

[0282] Specifically, the model parameter calculation results in step 1 are substituted into formula 10 to calculate the formation pressure at the BSR position:

[0283] P BSR =ρ*g*H=ρ*g*(D sea +Z BSR )=1035*9.8*(1920+152)=21.02Mpa(10-1)

[0284] In formula 10-1:

[0285] ρ: density of pore fluid in sedimentary formation, 1035 kg / m 3 ;

[0286] g: acceleration due to gravity, 9.8 m / s 2 ;

[0287] D sea : Sea depth, 1920m;

[0288] Z BSR : The burial depth of the BSR below the seabed is 152m.

[0289] Specifically, the alkane gas composition of the hydrate decomposition gas in this embodiment is:

[0290] CH4: 97.5%; C2H6: 2.49%; C3H8: 0.01%; pore water salinity: 35‰.

[0291] In this embodiment, the test contents related to the composition of hydrate decomposition gas and pore water salinity are all completed on-site during the hydrate drilling voyage. The test results are stored in the form of electronic documents, and the data can be directly retrieved for numerical simulation calculations.

[0292] In this embodiment, the hydrate decomposition gas alkane gas composition and pore water salinity parameter information are input into the phase equilibrium simulation software CSMGEM to carry out hydrate phase equilibrium simulation, that is, to construct a hydrate phase equilibrium function.

[0293] Furthermore, the BSR position obtained based on formula 10-1 is placed on the ground layer pressure P BSR Substituting into the hydrate phase equilibrium simulation function, the formation temperature at the BSR position is calculated, that is, the bottom boundary phase equilibrium temperature T of the hydrate stability region BSR :17.93℃.

[0294] In this embodiment, according to the measured seabed temperature T0 and the bottom phase equilibrium temperature of the hydrate stability region T BSR , calculate the average geothermal gradient of the hydrate stability zone, which is expressed as:

[0295]

[0296] Step 6: Calculate the vertical migration rate of the formation fluid using the Pe (Berkeley) equation and the geothermal gradient value at the model boundary.

[0297] In this embodiment, the geothermal gradient derived from formula 11 is is the average geothermal gradient value of the hydrate stability zone, and its value is half of the hydrate stability zone, that is, the average effect position point is 0.5Z BSR .

[0298] In a specific embodiment, according to the model boundary conditions, Formula 8 is expressed as:

[0299]

[0300] The result calculated by formula 2, formula 9 and formula 11 is Substituting into formula 12, the specific expression is as follows:

[0301] 100.59 / 114.1=e β(76 / L) (12-1)

[0302] Combined with the definition formula of Pe (Berkeley number):

[0303]

[0304] Formula 12-1 can be expressed as:

[0305]

[0306] In this embodiment, the specific information of each parameter in Formula 14 is as follows:

[0307] ρ w: Sediment pore fluid density, 1035kg / m 3 ;

[0308] C w : Sediment pore fluid heat capacity, 4186 J·kg -1 ·K -1 ;

[0309] φ: porosity of shallow seabed sedimentary strata, 0.4;

[0310] Specifically, in this embodiment, the φ value is calculated using hydrate while drilling acoustic logging information;

[0311] λ: Average thermal conductivity of shallow seabed sedimentary strata, 1.2 W·m -1 ·K -1 .

[0312] Specifically, in this embodiment, the λ value is obtained based on gravity piston sampling and thermal conductivity testing of hydrate drilling sediment samples.

[0313] In this embodiment, V z is the only variable to be solved in formula 14. Through numerical calculation, the vertical migration rate of the fluid is obtained as V z : 3.62cm / year.

[0314] In this example, the calculated fluid leakage activity rate is comparable to the fluid activity rate in the hydrate drilling area on the northeastern slope of the South China Sea that has been confirmed by drilling. This result suggests that the study area may also have the potential for hydrate development.

[0315] In summary, the present invention aims to solve scientific and technological problems existing in the process of marine geological exploration, such as "high cost of deep-sea in-situ data acquisition and observation", "difficulty in predicting the activity rate of shallow seabed fluids", and "uncertain potential engineering geological risks". Based on the basic theories of fluid kinematics and thermodynamics, the present invention gives full play to the parameter advantages of the "temperature" element of the formation. Relying on the near-seabed measured geothermal data with low acquisition cost and combining the hydrate stability zone geothermal data obtained by hydrate phase equilibrium simulation and BSR inversion, a one-dimensional thermal convection conduction model of the temperature field is established, and the average geothermal gradient of the near-seabed formation and the hydrate stability zone below the seabed is obtained. Finally, the Berkeley (Pe) equation is used to complete the calculation of the vertical migration rate of the shallow seabed fluid.

[0316] The embodiment of the present invention is based on the principles of fluid kinematics and thermodynamics, giving full play to the parameter advantages of the "temperature" factor, relying on the near-seabed measured formation temperature data with relatively low acquisition costs, and combining the hydrate stability zone geothermal data obtained by phase equilibrium simulation and BSR inversion. By establishing a one-dimensional heat convection conduction model and carrying out the calculation of the average geothermal gradient in the near-seabed formation and the hydrate stability zone below the seabed, the Berkeley (Pe) equation is finally used to realize the vertical migration rate of the shallow seabed fluid, providing a basis for clarifying the behavior of the shallow seabed fluid activity and evaluating the potential ecological environment and geological disaster impacts. Specifically, the technical solution of the present invention includes at least the following innovations:

[0317] Innovation 1: Based on the concepts of fluid kinematics and thermodynamics, this invention estimates the vertical migration rate of shallow seabed fluid by constructing a one-dimensional heat convection conduction model of the temperature field, thus making up for the deficiency that traditional technology cannot directly monitor the fluid activity patterns in the formations below the seabed.

[0318] The present invention first establishes a fluid leakage geological model based on a comprehensive analysis of geological elements, and on this basis proposes a one-dimensional heat convection conduction model and forms a vertical temperature field function of the formation. Afterwards, the vertical spatial geothermal field disturbance of the shallow seabed is used as a breakthrough point. By calculating the in-situ geothermal gradient of the near-seabed formation, the bottom boundary equilibrium temperature of the hydrate stability domain and the average geothermal gradient in the stable domain are calculated in combination with the hydrate phase equilibrium equation, and finally the vertical migration rate of the shallow seabed fluid is calculated using the Berkeley equation. The entire technical process is based on the basic principles of fluid kinematics and thermodynamics, and uses measured data such as the average geothermal gradient of the near-seabed formation and the hydrate stability domain below the seabed as boundary conditions to carry out model numerical calculations. The method is highly scientific. In addition, this method effectively overcomes the limitation that traditional observation (monitoring) means cannot directly obtain the characteristics of fluid activity in the formation below the seabed.

[0319] Key Point 2: This invention constructs the shallow seabed fluid field based on the formation "temperature" factor, breaking through the traditional technical paradigm of previous technical solutions that mostly use the formation "pressure" factor as the basis to infer the laws of deep fluid activity. It is innovative in the basic modeling theory and application scenarios.

[0320] Existing technologies mostly focus on deep oil and gas systems and the influence of formation "pressure," especially formation "overpressure" on the fluid migration and accumulation process. However, formation "overpressure" is almost non-existent in shallow seabed formations. However, the thermal convection generated during the migration of deep high-temperature gas-bearing fluids and their disturbance of the shallow seabed geothermal field can form an effective geological record. This provides a theoretical basis and technical advantages for this embodiment to use the "temperature" factor as the starting point to establish a one-dimensional thermal convection conduction numerical model of the temperature field to determine the shallow seabed fluid activity rate. In practical applications, the shallow seabed temperature field is relatively easy to obtain through seabed geothermal measurements; the important geophysical indicator (BSR) of hydrate occurrence is also more significant in the study area, which provides a reliable basis for constructing the hydrate phase equilibrium equation, determining the equilibrium temperature, and calculating the average geothermal gradient in the hydrate stability zone. Based on the "temperature" factor, the present invention realizes the effective integration of geothermal field information, geochemical information, and geophysical information under the constraints of fluid thermodynamics theory, thereby improving the accuracy of numerical simulation results. This technical method is highly applicable in studying shallow seabed strata, especially in studying the laws of fluid activity in the absence of fluid "overpressure".

[0321] Key point 3: The present invention is mainly based on seismic survey data and near-seabed temperature measurement data with relatively low acquisition cost, which effectively reduces the cost of obtaining in-situ formation parameters of deep formations. The technical method is cost-effective and has spatial scalability.

[0322] Traditional methods mainly rely on deploying in-situ observation equipment for fluid leakage activity on the seabed or obtaining key geological parameters of fluid activity based on hydrate drilling and related downhole detection equipment. The outstanding features of the above technical methods are high construction costs, long acquisition cycles for key geological scientific parameters, and certain geological, engineering, and environmental risks, which do not meet the conditions for large-scale implementation and application. The present invention is mainly based on shallow seabed geothermal measurement data and hydrate seismic survey data with low acquisition costs. By constructing a one-dimensional thermal convection conduction model of the temperature field, it realizes the quantitative calculation of fluid activity rate, effectively reducing the cost of obtaining key geothermal parameter information in deep layers, especially hydrate layers. The present invention and technical process effectively make up for the technical limitations of traditional methods that can only obtain fluid activity information through high-cost hydrate drilling, long-term seabed in-situ observation, etc. The technical method has high economic benefits and expanded applicability.

[0323] In view of this, compared with the existing technology, the present invention includes at least the following beneficial effects: Based on the basic principles of fluid kinematics and thermodynamics, the present invention establishes a fluid heat convection conduction model based on the "temperature" factor through the organic combination and information mining of seismic survey data (mainly BSR reflection characteristics) and near-seabed geothermal measurement data. The technical advantage of this method is to carry out numerical simulations under the constraints of actual geological models and boundary conditions, avoiding errors in understanding the laws of fluid activity that may be caused by the scarcity of deep formation drilling test data, and providing a basis for revealing the shallow fluid activity behavior on the seabed and then evaluating the potential ecological environment and geological disaster impacts. In addition, the present invention and technical process get rid of the path dependence of traditional technical methods that rely solely on high-cost drilling, long-term seabed in-situ observations, etc. to obtain fluid activity information, reducing the cost of obtaining formation science parameter information, and has good prospects for expanding applications.

[0324] It should also be noted that gas-bearing fluid seepage is widespread in continental margins and plays an important role in indicating energy accumulation, ocean carbon cycles, and ecosystem evolution. Research on this topic is of great scientific significance and economic value. This invention breaks through the traditional technical paradigm and key parameter acquisition limitations of previous technical solutions that rely on formation "pressure" to infer deep fluid activity. Based on the actual operating conditions and application scenarios of shallow submarine strata, and in accordance with the basic theories of fluid kinematics and thermodynamics, it fully utilizes the special advantages of the "temperature" factor. Relying on low-cost shallow submarine geothermal data and combining hydrate phase equilibrium simulation and BSR inversion to obtain the equilibrium temperature of the hydrate stability zone, a one-dimensional heat convection conduction model is established, and the average geothermal gradient within the hydrate stability zone near the submarine strata and below the submarine is calculated. Finally, the vertical migration rate of shallow submarine fluids is calculated using the Berkeley equation, providing a basis for elucidating the behavior of shallow submarine fluid activity and assessing potential ecological and geological disaster impacts. The present invention and technical process effectively make up for the technical limitations of previous technical solutions that can only obtain fluid activity information through high-cost hydrate drilling and long-term seabed in-situ observation. It has high economy and expanded applicability, and provides new ideas and methods for serving hydrate energy resource exploration and geological disaster assessment.

[0325] On the other hand, Figure 9 As shown, an embodiment of the present invention provides an analysis and processing device 900 for analyzing the flow rate of shallow seabed fluid, which may include:

[0326] The first module 901 is configured to obtain seismic reflection times of target locations in a seismic profile of a target area and establish a fluid leakage geological model based on the seismic reflection times; the target locations include the seabed, a quasi-seabed reflection layer, and the root of a fluid leakage channel; the top boundary of the fluid leakage geological model is the seabed, and the bottom boundary of the fluid leakage geological model is the root of the fluid leakage channel;

[0327] The second module 902 is used to establish a heat convection conduction model based on the fluid leakage geological model and the temperature data of the target location;

[0328] The third module 903 is used to transform the formation temperature field function based on the heat convection conduction model to obtain the function of the change of the geothermal gradient with the burial depth;

[0329] The fourth module 904 is used to obtain formation temperature measurement data, and obtain a temperature gradient value of a top boundary of a near-seabed formation based on the formation temperature measurement data; the near-seabed formation represents the top boundary of a fluid leakage geological model;

[0330] The fifth module 905 is used to obtain the formation pressure of the seabed-like reflector layer, and solve the hydrate phase equilibrium equation based on the formation pressure to obtain the phase equilibrium temperature of the bottom boundary of the hydrate stability zone. Then, combined with the measured seabed temperature at the seabed location, the average geothermal gradient of the hydrate stability zone is obtained.

[0331] The sixth module 906 is used to substitute the average geothermal gradient into the variation function, and then derive the vertical migration rate of the fluid in combination with the Berkeley equation.

[0332] The contents of the method embodiments of the present invention are all applicable to the device embodiments. The functions specifically implemented by the device embodiments are the same as those of the above method embodiments, and the beneficial effects achieved are also the same as those achieved by the above method embodiments.

[0333] In another aspect, an embodiment of the present invention further provides an electronic device comprising a memory and a processor. The memory stores a computer program, and the processor, when executing the computer program, implements the aforementioned method for analyzing and processing the rate of shallow seafloor fluid activity. The electronic device can be any smart terminal, including a tablet computer and an in-vehicle computer.

[0334] It can be understood that the contents of the above method embodiments are applicable to the present device embodiments, the functions specifically implemented by the present device embodiments are the same as those of the above method embodiments, and the beneficial effects achieved are also the same as those achieved by the above method embodiments.

[0335] like Figure 10 As shown, Figure 10 The hardware structure of an electronic device 1000 according to another embodiment is shown. The electronic device 1000 includes:

[0336] The processor 1001 may be implemented as a general-purpose CPU (Central Processing Unit), a microprocessor, an application-specific integrated circuit (ASIC), or one or more integrated circuits, and is configured to execute relevant programs to implement the technical solutions provided by the embodiments of the present invention.

[0337] The memory 1002 can be implemented in the form of a read-only memory (ROM), a static storage device, a dynamic storage device, or a random access memory (RAM). The memory 1002 can store an operating system and other application programs. When the technical solutions provided in the embodiments of this specification are implemented through software or firmware, the relevant program code is stored in the memory 1002 and is called by the processor 1001 to execute the network node population optimization method of the embodiment of the present invention.

[0338] Input / output interface 1003, used to implement information input and output;

[0339] Communication interface 1004, used to implement communication interaction between this device and other devices, which can be achieved through wired means (such as USB, network cable, etc.) or wireless means (such as mobile network, WiFi, Bluetooth, etc.);

[0340] Bus 1005 , which transmits information between various components of the device (e.g., processor 1001 , memory 1002 , input / output interface 1003 , and communication interface 1004 );

[0341] The processor 1001 , the memory 1002 , the input / output interface 1003 and the communication interface 1004 are connected to each other in communication within the device via the bus 1005 .

[0342] The electronic device embodiments described above are merely illustrative. The units described as separate components may or may not be physically separate, i.e., they may be located in one location or distributed across multiple network units. Some or all of these modules may be selected based on actual needs to achieve the objectives of this embodiment.

[0343] The contents of the method embodiments of the present invention are all applicable to the electronic device embodiments. The functions specifically implemented by the electronic device embodiments are the same as those of the above method embodiments, and the beneficial effects achieved are also the same as those achieved by the above method embodiments.

[0344] Another aspect of an embodiment of the present invention further provides a computer-readable storage medium, wherein the storage medium stores a program, and the program is executed by a processor to implement the above method.

[0345] It should be noted that the computer-readable medium shown in the embodiments of the present invention may be a computer-readable signal medium or a computer-readable storage medium, or any combination thereof. The computer-readable storage medium may be, for example, but not limited to, an electrical, magnetic, optical, electromagnetic, infrared, or semiconductor system, device, or component, or any combination thereof. More specific examples of computer-readable storage media may include, but are not limited to: an electrical connection with one or more wires, a portable computer disk, a hard disk, a random access memory (RAM), a read-only memory (ROM), an erasable programmable read-only memory (EPROM), a flash memory, an optical fiber, a portable compact disc read-only memory (CD-ROM), an optical storage device, a magnetic storage device, or any suitable combination thereof. In the present invention, a computer-readable storage medium may be any tangible medium containing or storing a program that can be used by or in conjunction with an instruction execution system, device, or component. In the present invention, a computer-readable signal medium may include a data signal propagated in baseband or as part of a carrier wave, which carries computer-readable program code. Such propagated data signals may take various forms, including but not limited to electromagnetic signals, optical signals, or any suitable combination thereof. A computer-readable signal medium may also be any computer-readable medium other than a computer-readable storage medium that can transmit, propagate, or transport a program for use by or in connection with an instruction execution system, apparatus, or device. Program code embodied on a computer-readable medium may be transmitted using any suitable medium, including but not limited to wireless, wired, or any suitable combination thereof.

[0346] The contents of the method embodiments of the present invention are all applicable to the computer-readable storage medium embodiments. The functions specifically implemented by the computer-readable storage medium embodiments are the same as those of the above method embodiments, and the beneficial effects achieved are also the same as those achieved by the above method embodiments.

[0347] The present invention also discloses a computer program product or computer program, which includes computer instructions stored in a computer-readable storage medium. A processor of a computer device can read the computer instructions from the computer-readable storage medium and execute the computer instructions, causing the computer device to perform the above method.

[0348] The flowcharts and block diagrams in the accompanying drawings illustrate the possible implementation architecture, functions and operations of the systems, methods and computer program products according to various embodiments of the present invention. In this regard, each box in the flowchart or block diagram can represent a module, program segment, or a part of code, and the above-mentioned module, program segment, or a part of code contains one or more executable instructions for implementing the specified logical function. It should also be noted that in some alternative implementations, the functions marked in the box can also occur in an order different from that marked in the accompanying drawings. For example, two boxes represented in succession can actually be executed substantially in parallel, and they can sometimes be executed in the opposite order, depending on the functions involved. It should also be noted that each box in the block diagram or flowchart, and the combination of boxes in the block diagram or flowchart, can be implemented with a dedicated hardware-based system that performs the specified function or operation, or can be implemented with a combination of dedicated hardware and computer instructions.

[0349] It should be noted that although several modules of the device for action execution are mentioned in the above detailed description, this division is not mandatory. In fact, according to an embodiment of the present invention, the features and functions of two or more modules or units described above can be concretized in one module or unit. Conversely, the features and functions of one module or unit described above can be further divided into multiple modules or units to be concretized.

[0350] Through the description of the above embodiments, it is easy for those skilled in the art to understand that the example embodiments described herein can be implemented by software or by combining software with necessary hardware. Therefore, the technical solution according to the embodiments of the present invention can be embodied in the form of a software product, which can be stored in a non-volatile storage medium (which can be a CD to ROM, a USB flash drive, a mobile hard disk, etc.) or on a network, and includes a number of instructions to enable a computing device (which can be a personal computer, a server, a touch terminal, or a network device, etc.) to execute the method according to the embodiments of the present invention.

[0351] In some optional embodiments, the function / operation mentioned in the block diagram may not occur in the order mentioned in the operation diagram. For example, depending on the function / operation involved, the two boxes shown in succession can actually be executed substantially simultaneously or the boxes can sometimes be executed in reverse order. In addition, the embodiment presented and described in the flow chart of the present invention is provided in an exemplary manner for the purpose of providing a more comprehensive understanding of the technology. The disclosed method is not limited to the operation and logic flow presented herein. Optional embodiments are contemplated in which the order of the various operations is changed and the sub-operations described as a part of a larger operation are performed independently.

[0352] In addition, although the present invention is described in the context of functional modules, it should be understood that, unless otherwise stated, one or more of the functions and / or features may be integrated into a single physical device and / or software module, or one or more functions and / or features may be implemented in separate physical devices or software modules. It will also be understood that a detailed discussion of the actual implementation of each module is not necessary for understanding the present invention. More specifically, given the properties, functions, and internal relationships of the various functional modules in the devices disclosed herein, the actual implementation of the module will be understood within the ordinary skill of an engineer. Therefore, a person skilled in the art will be able to implement the present invention as set forth in the claims using ordinary skill without undue experimentation. It will also be understood that the specific concepts disclosed are merely illustrative and are not intended to limit the scope of the present invention, which is determined by the full scope of the appended claims and their equivalents.

[0353] If the function is implemented in the form of a software functional unit and sold or used as an independent product, it can be stored in a computer-readable storage medium. Based on this understanding, the technical solution of the present invention, or the part that contributes to the prior art, or the part of the technical solution, can be embodied in the form of a software product. The computer software product is stored in a storage medium and includes several instructions for enabling a computer device (which can be a personal computer, server, or network device, etc.) to execute all or part of the steps of the methods of each embodiment of the present invention. The aforementioned storage medium includes: U disk, mobile hard disk, read-only memory (ROM, Read Only Memory), random access memory (RAM, Random Access Memory), disk or optical disk, and other media that can store program code.

[0354] The logic and / or steps represented in the flowcharts or otherwise described herein, for example, can be considered as an ordered list of executable instructions for implementing the logical functions, and can be embodied in any computer-readable medium for use by, or in conjunction with, an instruction execution apparatus, device, or apparatus (e.g., a computer-based apparatus, a device including a processor, or other apparatus that can fetch instructions from and execute instructions on an instruction execution apparatus, device, or apparatus). For purposes of this specification, a "computer-readable medium" can be any device that can contain, store, communicate, propagate, or transport a program for use by, or in conjunction with, an instruction execution apparatus, device, or apparatus.

[0355] More specific examples (a non-exhaustive list) of computer-readable media include the following: an electrical connection with one or more wires (electronic devices), a portable computer disk cartridge (magnetic devices), a random access memory (RAM), a read-only memory (ROM), an erasable and programmable read-only memory (EPROM or flash memory), a fiber optic device, and a portable compact disc read-only memory (CDROM). In addition, the computer-readable medium may even be paper or other suitable medium on which the program is printed, since the program may be obtained electronically, for example, by optically scanning the paper or other medium, followed by editing, deciphering, or processing in another suitable manner as necessary, and then stored in a computer memory.

[0356] It should be understood that various parts of the present invention can be implemented using hardware, software, firmware, or a combination thereof. In the above-described embodiments, multiple steps or methods can be implemented using software or firmware stored in a memory and executed by a suitable instruction execution device. For example, if implemented using hardware, as in another embodiment, any one of the following technologies known in the art or a combination thereof can be used: a discrete logic circuit having a logic gate circuit for implementing a logic function on a data signal, an application-specific integrated circuit having a suitable combination of logic gate circuits, a programmable gate array (PGA), a field programmable gate array (FPGA), etc.

[0357] Throughout this specification, reference to terms such as "one embodiment," "some embodiments," "examples," "specific examples," or "some examples" means that a specific feature, structure, material, or characteristic described in conjunction with that embodiment or example is included in at least one embodiment or example of the present invention. In this specification, schematic representations of the above terms do not necessarily refer to the same embodiment or example. Furthermore, the specific features, structures, materials, or characteristics described may be combined in any suitable manner in any one or more embodiments or examples.

[0358] While embodiments of the present invention have been shown and described, it will be appreciated by those skilled in the art that various changes, modifications, substitutions, and variations may be made to the embodiments without departing from the principles and spirit of the invention, and that the scope of the invention is defined by the claims and their equivalents.

[0359] The above is a specific description of the preferred implementation of the present invention, but the present invention is not limited to the embodiments. Those skilled in the art can make various equivalent modifications or substitutions without violating the spirit of the present invention. These equivalent modifications or substitutions are all included in the scope defined by the claims of the present invention.

Claims

1. A method for analyzing and processing the flow rate of shallow seabed fluid, characterized in that: The following steps are involved: Acquire seismic reflection times of a target position in a seismic profile of a target area, and establish a fluid leakage geological model based on the seismic reflection times; the target position includes a seabed position, a seabed-like reflection layer, and a root position of a fluid leakage channel; the top boundary of the fluid leakage geological model is the seabed position, and the bottom boundary of the fluid leakage geological model is the root position of the fluid leakage channel; the seismic reflection times include a first reflection time of the seabed position, a second reflection time of the seabed-like reflection layer, and a third reflection time of the root position of the fluid leakage channel; establishing the fluid leakage geological model based on the seismic reflection times comprises the following steps: Obtaining the seabed depth of the seabed position according to half of the product of the first reflection time and a first velocity; the first velocity represents the propagation speed of seismic waves in seawater; A first depth is obtained based on half of the product of a difference between the second reflection time and the first reflection time and a second velocity; the second velocity represents a propagation velocity of seismic waves in a shallow seabed; and the first depth represents a depth of the seabed-like reflective layer below the seabed position; A second depth is obtained based on half of the product of the difference between the third reflection time and the first reflection time and the second velocity; the second depth represents the depth of the root position of the fluid leakage channel below the seabed position; Establishing the fluid leakage geological model based on the seabed depth, the first depth, and the second depth; The top boundary of the fluid leakage geological model is the seabed position, and the bottom boundary of the fluid leakage geological model is the root position of the fluid leakage channel; the vertical distance of the fluid leakage geological model is equal to the second depth; Establishing a heat convection conduction model based on the fluid leakage geological model and the temperature data of the target location; Performing formation temperature field function transformation based on the heat convection conduction model to obtain a function of geothermal gradient varying with burial depth; Acquiring formation temperature measurement data, and processing the formation temperature measurement data to obtain a top boundary temperature gradient value of a near-seabed formation; the near-seabed formation represents the top boundary of the fluid leakage geological model; Obtaining the formation pressure of the seabed-like reflective layer, and obtaining the phase equilibrium temperature of the bottom boundary of the hydrate stability zone by solving the hydrate phase equilibrium equation based on the formation pressure, and then combining it with the measured seabed temperature at the seabed location to obtain the average geothermal gradient of the hydrate stability zone; The average geothermal gradient is substituted into the variation function, and then the vertical migration rate of the fluid is derived in combination with the Berkeley equation.

2. The method for analyzing and processing the flow rate of shallow seabed fluid according to claim 1, characterized in that: The temperature data includes the top boundary temperature of the top boundary and the bottom boundary temperature of the bottom boundary; the heat convection conduction model is established based on the fluid leakage geological model and the temperature data of the target location, including the following steps: The heat convection conduction model is established based on the top boundary temperature and the bottom boundary temperature in combination with the Berkeley number and the vertical distance of the fluid leakage geological model; the vertical distance represents the depth distance between the top boundary and the bottom boundary; The heat convection conduction model represents the data relationship between the burial depth and the corresponding depth temperature; the expression of the heat convection conduction model is: Where, T z represents the depth temperature corresponding to the burial depth z; T0 represents the top temperature; T L represents the bottom temperature; L represents the vertical distance; e is a mathematical constant; β represents the Berkeley number.

3. The method for analyzing and processing the flow rate of shallow seabed fluid according to claim 2, characterized in that: The method of performing formation temperature field function transformation based on the heat convection conduction model to obtain a function of geothermal gradient varying with burial depth comprises the following steps: Calculating the partial derivative function of the formation temperature field with respect to the burial depth based on the heat convection conduction model, and establishing a functional relationship between the geothermal gradient and the burial depth in the heat convection conduction model; The expression of the functional relationship is: Where, The symbol representing the partial derivative function; T represents the symbol for temperature; Based on the functional relationship, the temperature function of the near-seabed stratum is obtained by taking the burial depth as approximately 0 as a constraint condition; Wherein, the expression of the temperature function is: Substituting the temperature function into the functional relationship, and obtaining the change function through functional transformation; Wherein, the expression of the change function is:

4. The method for analyzing and processing the flow rate of shallow seabed fluid according to claim 1, characterized in that: The step of obtaining formation temperature measurement data and obtaining a top boundary temperature gradient value of a near-seabed formation based on the formation temperature measurement data includes the following steps: Acquiring in-situ temperature data and position information of a temperature probe in a shallow seabed layer to obtain the formation temperature measurement data; The temperature probe is carried by a gravity column and placed at the shallow surface layer of the seabed, and the gravity column carries a plurality of the temperature probes; the shallow surface layer of the seabed represents a shallow layer within a preset depth below the seabed position; The in-situ temperature data corresponding to the different position information are linearly fitted using the least squares method to obtain the apparent geothermal gradient value of the near-seabed stratum, and the apparent geothermal gradient value is used as the top boundary temperature gradient value.

5. The method for analyzing and processing the flow rate of shallow seabed fluid according to claim 1, characterized in that: The step of obtaining the formation pressure of the quasi-seafloor reflector layer, obtaining the phase equilibrium temperature of the bottom boundary of the hydrate stability zone by solving the hydrate phase equilibrium equation based on the formation pressure, and then obtaining the average geothermal gradient of the hydrate stability zone in combination with the measured seafloor temperature at the seafloor location comprises the following steps: Determining the underwater depth of the seabed-like reflective layer based on a fluid seepage geological model, and then calculating the hydrostatic pressure of the seabed-like reflective layer in combination with the pore fluid density of the sedimentary formation; and using the hydrostatic pressure as the formation pressure; The fluid seepage geological model includes the seabed depth of the seabed location and a first depth of the seabed-like reflective layer below the seabed location; the underwater depth is obtained based on the sum of the seabed depth and the first depth; and the hydrostatic pressure is obtained by multiplying the underwater depth, the pore fluid density, and the gravitational acceleration. A hydrate phase equilibrium simulation function is constructed using preset phase equilibrium simulation software, and the formation pressure is substituted into the hydrate phase equilibrium simulation function to solve and obtain the phase equilibrium temperature at the bottom boundary of the hydrate stability domain; Based on the phase equilibrium temperature at the bottom boundary of the hydrate stability zone and the measured seabed temperature at the seabed location, the average geothermal gradient of the hydrate stability zone is obtained by partial derivative calculation; The expression of the average geothermal gradient is: Where, represents the symbol of the partial derivative function; T represents the symbol of temperature; z represents the burial depth; T BSR represents the phase equilibrium temperature; T0 represents the measured seabed temperature; Z BSR Indicates the first depth.

6. The method for analyzing and processing the flow rate of shallow seabed fluid according to claim 1, characterized in that: Substituting the average geothermal gradient into the variation function and then deriving the vertical migration rate of the fluid in combination with the Berkeley equation includes the following steps: Substituting the average effect position point corresponding to the average geothermal gradient into the variation function to obtain a first function; Wherein, the expression of the change function is: Where, represents the symbol of the partial derivative function; T represents the symbol of temperature; z represents the burial depth; L represents the vertical distance of the heat convection conduction model; e is a mathematical constant; β represents the Berkeley number; The expression of the average geothermal gradient is: Where, T BSR represents the phase equilibrium temperature; T0 represents the measured seabed temperature; Z BSR Indicates the first depth of the seabed-like reflector below the seabed; The expression of the first function is: Where, 0.5Z BSR is the average effect location point; Substituting the Berkeley equation into the first function to obtain a second function; The expression of the Berkeley equation is: Where φ represents the formation porosity; ρ w represents the density of sediment pore fluid; C w represents the heat capacity of sediment pore fluid; V z represents the vertical migration rate of fluid; λ represents the average thermal conductivity of formation sediment; The expression of the second function is: The measured parameters are introduced into the second function to derive the vertical migration rate of the fluid; the measured parameters include the measured values ​​of the formation porosity, the sediment pore fluid density, the sediment pore fluid heat capacity and the average thermal conductivity of the formation sediment.

7. An analytical and processing device for the flow rate of shallow seabed fluid, characterized in that: include: The first module is configured to obtain seismic reflection times of a target position in a seismic profile of a target area, and establish a fluid leakage geological model based on the seismic reflection times; the target position includes a seabed position, a seabed-like reflection layer, and a root position of a fluid leakage channel; the top boundary of the fluid leakage geological model is the seabed position, and the bottom boundary of the fluid leakage geological model is the root position of the fluid leakage channel; the seismic reflection times include a first reflection time of the seabed position, a second reflection time of the seabed-like reflection layer, and a third reflection time of the root position of the fluid leakage channel; establishing the fluid leakage geological model based on the seismic reflection times comprises the following steps: Obtaining the seabed depth of the seabed position according to half of the product of the first reflection time and a first velocity; the first velocity represents the propagation speed of seismic waves in seawater; A first depth is obtained based on half of the product of a difference between the second reflection time and the first reflection time and a second velocity; the second velocity represents a propagation velocity of seismic waves in a shallow seabed; and the first depth represents a depth of the seabed-like reflective layer below the seabed position; A second depth is obtained based on half of the product of the difference between the third reflection time and the first reflection time and the second velocity; the second depth represents the depth of the root position of the fluid leakage channel below the seabed position; Establishing the fluid leakage geological model based on the seabed depth, the first depth, and the second depth; The top boundary of the fluid leakage geological model is the seabed position, and the bottom boundary of the fluid leakage geological model is the root position of the fluid leakage channel; the vertical distance of the fluid leakage geological model is equal to the second depth; The second module is used to establish a heat convection conduction model based on the fluid leakage geological model and the temperature data of the target location; The third module is used to transform the formation temperature field function based on the heat convection conduction model to obtain the function of the change of geothermal gradient with burial depth; A fourth module is configured to obtain formation temperature measurement data, and obtain a top boundary temperature gradient value of a near-seabed formation based on the formation temperature measurement data; the near-seabed formation represents the top boundary of the fluid leakage geological model; A fifth module is configured to obtain the formation pressure of the quasi-seafloor reflector layer, obtain the phase equilibrium temperature of the bottom boundary of the hydrate stability zone by solving the hydrate phase equilibrium equation based on the formation pressure, and then obtain the average geothermal gradient of the hydrate stability zone in combination with the measured seafloor temperature at the seafloor location; The sixth module is used to substitute the average geothermal gradient into the variation function, and then derive the vertical migration rate of the fluid in combination with the Berkeley equation.

8. An electronic device, characterized in that: including a processor and a memory; The memory is used to store programs; The processor executes the program to implement the method according to any one of claims 1 to 6.

9. A computer storage medium storing a program executable by a processor, characterized in that: The program executable by the processor is used to implement the method according to any one of claims 1 to 6 when executed by the processor.

Images