Method and device for recovering ancient landform of broken basin, medium and equipment

Abstract

The invention relates to a method, a device, a medium and equipment for recovering the ancient landform of a broken basin. The method comprises the following steps: acquiring seismic profile data of a target basin; identifying top and bottom reflection interfaces of the magma bottoming body according to the seismic profile data; determining a seismic two-way travel time based on the top and bottom reflective interfaces of the magmatic bottoming body; on the basis of the earthquake two-way travel time, calculation is carried out by combining magma bottom dager body data and adopting a heave amount calculation model, and R values of all positions are obtained; constructing a section based on the R value to obtain a plurality of section lines; determining a ratio function; identifying an abnormal upheaval region according to a ratio function; and according to the R value of each section line, carrying out backstepping and correcting the abnormal upheaval area, and recovering the ancient landform of the broken basin. According to the method, the magma bottom can be quantitatively eliminated, the bottleneck problem that a disturbance area cannot be quantified and recovered in a traditional method is solved, and the real spatial form of an original stratigraphic system is accurately recovered.

Description

Technical Field

[0001] This invention relates to the field of oil and gas geological exploration technology, and more specifically, to a method, apparatus, medium, and equipment for restoring paleomorphology in rift basins. Background Technology

[0002] During the tectonic evolution of sedimentary basins, magmatic activity often intrudes into sedimentary strata in the form of diapirs. These magmatic diapirs often exhibit upward-arching intrusive structures. Their high-density and high-velocity physical properties can lead to abnormal seismic wave propagation paths, resulting in distorted seismic profile images and chaotic reflection characteristics. This, in turn, leads to misjudgments of stratigraphic structures and severely interferes with the paleogeographic reconstruction of rift basins.

[0003] Existing paleogeographic reconstruction methods largely rely on seismic stratigraphic interpretation and interpolation algorithms, or empirical models based on stratigraphic thickness backfilling and erosion compensation. However, for areas heavily influenced by magmatic diapiric intrusions, these methods primarily remain at the stage of qualitative analysis or semi-quantitative processing, lacking a systematic quantitative restoration mechanism for diapiric disturbance zones. For example, for uplifted landforms caused by strong diapiric intrusions, existing methods cannot accurately determine the true spatial morphology of the original stratigraphic system, leading to significant errors in subsequent structural interpretation and hydrocarbon prediction results. Summary of the Invention

[0004] The technical problem to be solved by the present invention is to provide a method, apparatus, medium and equipment for restoring ancient landforms in rift basins, addressing the problems existing in the prior art.

[0005] The technical solution adopted by this invention to solve its technical problem is: to construct a method for restoring the paleogeography of a fault basin, comprising the following steps: Obtain seismic profile data of the target basin; Identify the top and bottom reflection interfaces of the magma diapiric body based on the seismic profile data; The two-way travel time of the earthquake is determined based on the top and bottom reflection interfaces of the magma diapir. Based on the earthquake two-way travel time, combined with magma diapiric data and using the uplift calculation model, the R value at each location was obtained. Based on the R value, a profile is constructed to obtain multiple profile lines; Determine the ratio function; Abnormal bulging areas are identified based on the ratio function; The paleogeography of the fault basin is reconstructed by inferring the R value of each profile line and combining it with the abnormal uplift area.

[0006] In the method for restoring paleogeography of rift basins described in this invention, the step of identifying the top and bottom reflection interfaces of a magma diapiric body based on the seismic profile data includes: Based on the seismic profile data, determine the profile amplitude anomaly data and the changes in reflected energy; Based on the abnormal amplitude data and reflection energy changes in the profile, and combined with well-controlled formation data, the top and bottom reflection interfaces of the magmatic diapiric body are identified on the profile.

[0007] In the method for restoring paleogeography of rift basins described in this invention, determining the two-way travel time of an earthquake based on the top and bottom reflection interfaces of the magma diapiric body includes: Based on the top and bottom reflection interfaces of the magma diapiric body, the corresponding seismic reflection signals are obtained; The earthquake's two-way travel time is obtained by identifying the earthquake reflection characteristics based on the earthquake reflection signal.

[0008] In the method for restoring paleogeography of rift basins described in this invention, the calculation of R values ​​at each location based on the two-way seismic travel time, combined with magmatic diapiric data and using an uplift calculation model, includes: The thickness of the magma diapiric body was obtained by performing time-depth conversion on the earthquake's two-way travel time. The uplift height difference and original stratum thickness were determined based on the magma diapiric data. The R value at each location is calculated based on the thickness of the magma diapiric body, the uplift height difference, and the thickness of the original strata, using the uplift amount calculation model.

[0009] In the method for restoring the paleogeography of a fault basin described in this invention, the uplift height difference is determined in the following manner: The seismic time interval between the bottom of the magmatic body and the top of the strata deformation is determined based on the magma diapir data. The earthquake time interval is converted to depth to obtain the uplift height difference.

[0010] In the method for restoring paleogeography of rift basins described in this invention, the original stratigraphic thickness is determined in the following manner: Based on the magma diapir data, the time difference and formation velocity from the bottom of the magmatic rock mass to the undeformed stratum are obtained; The thickness of the undeformed stratum is calculated based on the time difference and the formation velocity. Determine the formation thickness below the highest intrusion point; The original formation thickness is obtained by calculating based on the thickness of the undeformed formation and the thickness of the formation below the highest intrusion point.

[0011] In the method for restoring paleogeography of fault basins described in this invention, the uplift calculation model is as follows: ; Where R represents the diapiric uplift; T represents the thickness of the magmatic diapiric body; h represents the uplift height difference; and H represents the thickness of the original strata.

[0012] The present invention also provides a device for restoring paleogeography in a fault basin, comprising: The data acquisition unit is used to acquire seismic profile data of the target basin. Interface recognition unit, used to identify the top and bottom reflection interfaces of the magma diapir based on the seismic profile data; The time analysis unit is used to determine the two-way travel time of the earthquake based on the top and bottom reflection interfaces of the magma diapir. The calculation unit is used to calculate the R value at each location based on the earthquake two-way travel time, combined with magma diapirs data and using a uplift calculation model. A profile construction unit is used to construct a profile based on the R value to obtain multiple profile lines; Function determination unit, used to determine the ratio function; Anomaly identification unit is used to identify abnormal raised areas based on the ratio function; The geomorphological restoration unit is used to back-calculate based on the R value of each profile line and restore the paleomorphology of the rift basin in combination with the abnormal uplift area.

[0013] The present invention also provides a storage medium storing a computer program adapted for loading by a processor to perform the steps of the above-described method for restoring paleogeography in a rift basin.

[0014] The present invention also provides an electronic device, including a memory and a processor, wherein the memory stores a computer program, and the processor executes the steps of the paleogeographic restoration method for rift basins as described in any of the preceding claims by calling the computer program stored in the memory.

[0015] The method, apparatus, medium, and equipment for restoring paleomorphology in rift basins according to the present invention have the following beneficial effects: The method includes the following steps: acquiring seismic profile data of the target basin; identifying the top and bottom reflection interfaces of the magmatic diapirs based on the seismic profile data; determining the two-way travel time (BLT) of the seismic system based on the top and bottom reflection interfaces of the magmatic diapirs; calculating the R-value at each location based on the BLT, combined with the magmatic diapirs data, and using a uplift calculation model; constructing a profile based on the R-values ​​to obtain multiple profile lines; determining a ratio function; identifying anomalous uplift areas based on the ratio function; and back-calculating and correcting the anomalous uplift areas based on the R-value of each profile line to restore the paleomorphology of the rift basin. This invention can quantitatively eliminate magmatic diapirs, solving the bottleneck problem of "inability to quantify and restore" disturbed areas in traditional methods, and accurately restoring the true spatial morphology of the original stratigraphy. Attached Figure Description

[0016] The present invention will be further described below with reference to the accompanying drawings and embodiments. In the accompanying drawings: Figure 1 This is a schematic flowchart of the method for restoring paleogeography in a fault basin provided in an embodiment of the present invention; Figure 2 This is a schematic diagram illustrating the principle of magmatic diapirs disturbing the topography of rift basins, as provided in an embodiment of the present invention. Figure 3 This is a schematic diagram of the boundary identification of a magma diapiric body provided in an embodiment of the present invention; Figure 4 This is a seismic profile of a magma diapiric body provided in an embodiment of the present invention; Figure 5 This is a logic block diagram of the ancient landform restoration device for rift basins provided in an embodiment of the present invention. Detailed Implementation

[0017] The technical solutions of the embodiments of the present invention will be clearly and completely described below with reference to the accompanying drawings. Obviously, the described embodiments are only some embodiments of the present invention, and not all embodiments. Based on the embodiments of the present invention, all other embodiments obtained by those skilled in the art without creative effort are within the scope of protection of the present invention.

[0018] To address the distortion in geomorphological reconstruction caused by magmatic diapirs disturbing sedimentary strata and fundamentally improve the accuracy and reliability of geological and geomorphological reconstruction in rift basins, this invention provides a paleogeomorphological reconstruction method for rift basins. This method enables physical quantitative analysis of the disturbance areas caused by magmatic diapirs. Based on a collaborative approach of profile amplitude anomaly identification, quantitative R-value calculation, ratio boundary discrimination, spatial thickness inversion, and 3D reconstruction, this method overcomes the bottleneck problem of traditional methods being unable to quantify and reconstruct disturbed areas. Magmatic diapirs are diapiric structures driven by magma, referring to special geological structures with dome-shaped or mushroom-shaped morphology formed by deep magma penetrating or arching overlying sedimentary / metamorphic rock layers under the combined action of buoyancy and tectonic stress.

[0019] refer to Figure 1 The method for restoring ancient geomorphology of fault basins provided by the present invention includes the following steps S10, S20, S30, S40, S50, S60, S70 and S80.

[0020] Step S10: Obtain seismic profile data of the target basin.

[0021] In some embodiments, the seismic profile data includes, but is not limited to: high-precision two-dimensional / three-dimensional time-domain or depth-domain seismic data volumes, acquisition spacing of main survey lines and connecting survey lines, seismic sampling rate, average dominant frequency, and vertical resolution.

[0022] Step S20: Identify the top and bottom reflection interfaces of the magma diapirs based on the seismic profile data.

[0023] In some embodiments, identifying the top and bottom reflection interfaces of a magmatic diapir based on seismic profile data includes: determining profile amplitude anomaly data and reflection energy changes based on seismic profile data; and identifying the top and bottom reflection interfaces of the magmatic diapir based on the profile amplitude anomaly data and reflection energy changes, combined with well-controlled stratigraphic data.

[0024] In some embodiments, lithological information from drilling, lithological sampling of relevant depth intervals, or zircon dating can directly identify magmatic rock bodies and thus determine the plausibility of the existence of magmatic diapirs. Moreover, in well logging curve identification, the GR curve usually reflects rich lithological information: low GR values ​​typically represent mafic basic rocks, while high GR values ​​typically represent acidic felsic rocks.

[0025] Specifically, this step involves: First, determining the spatial extent of the magmatic diapir. This includes: loading high-resolution 2D / 3D seismic data (including time-domain / depth-domain data) into seismic interpretation software (such as the commonly used Petrel and Geoframe); matching the acquisition spacing and seismic sampling rate of the master and tie lines; preprocessing the seismic profile based on the average dominant frequency and vertical resolution of the data (including but not limited to noise suppression and amplitude equalization correction); calculating the amplitude and reflection energy properties of the profile; and delineating areas of significant amplitude anomalies or energy abrupt changes that differ significantly from the sedimentary strata of the target basin through attribute plane / profile distribution. These amplitude anomalies or energy abrupt changes represent the spatial extent of the suspected magmatic diapir. Second, identifying the top and bottom reflection interfaces of the magmatic diapir. Specifically, if a magmatic diapir is identified by seismic profiles and is located near a well, the lithology and stratigraphy of the magmatic diapir are confirmed using well core or cuttings descriptions. Well data is projected onto the seismic profile, and the top or bottom boundaries of the identified magmatic rocks are mapped onto the reflection phase axes on the seismic profile using synthetic seismic records. In the aforementioned amplitude anomaly zones, combined with well calibration results (i.e., the lithology and stratigraphy of the magmatic diapir), continuous, high-amplitude reflection axes are identified as the top reflection interface of the magmatic diapir, and reflection phase axes with abrupt changes in wave impedance below them are identified as the bottom reflection interface of the magmatic diapir. Figure 2This invention illustrates the principle of how magmatic diapirs disturb the topography of rift basins. In this embodiment, the existence of a magmatic diapir is determined by a combination of well and seismic analysis.

[0026] Understandably, in some other embodiments, for wells that cannot penetrate the bottom interface of a magma diapir, seismic reflection anomalies can be used to determine the top and bottom reflection interfaces of the magma diapir. Figure 3 The boundary of a magmatic diapiric body is shown. Specifically, it can be identified based on the seismic reflection characteristics of the seismic reflection signals between the upper and lower interfaces of the magmatic diapiric body in the seismic profile. The top reflection interface is the top interface of the magmatic diapiric body, and the bottom reflection interface is the footwall interface. Seismic reflection signals refer to the seismic wave signals received and recorded by seismic detectors when elastic waves (mainly P-waves) excited by artificial or natural sources propagate underground and encounter stratigraphic interfaces (such as lithological interfaces, unconformities, fault planes, etc.) with non-zero wave impedance differences. A portion of the energy is reflected back to the surface according to the law of reflection (the angle of incidence equals the angle of reflection, and the three lines are coplanar). The seismic reflection signals of magmatic diapiric bodies are usually accompanied by a series of envelope structures, chaotic reflections, continuous strong reflections, or ridge-like reflections. These characteristics often cause local deformation of the surrounding rock, forming forced folds. These characteristics can determine the location of the magmatic diapiric body. There are significant differences in the seismic reflection characteristics of sedimentary strata and igneous rocks: Sedimentary strata, due to their layered structure of progressive accumulation, exhibit seismic reflections that often show regular, parallel / subparallel, progradational, or divergent layered structures. They exhibit good continuity of phase axes, lateral stability of amplitude and frequency, and can be traced over long distances. They often display sheet-like or wedge-shaped strata-bound morphologies and have conformable or unconformable parallel contact relationships with the preceding and following strata. Furthermore, typical sedimentary structural seismic responses such as top-waist and bottom-waist can be identified. Therefore, these differences in seismic signals can be used to distinguish between sedimentary strata and igneous diapirs.

[0027] Step S30: Determine the two-way travel time of the earthquake based on the top and bottom reflection interfaces of the magma diapir.

[0028] In some embodiments, determining the two-way travel time of an earthquake based on the top and bottom reflection interfaces of a magma diapir includes: obtaining the corresponding seismic reflection signals based on the top and bottom reflection interfaces of the magma diapir; and identifying the seismic reflection characteristics of the seismic reflection signals to obtain the two-way travel time of the earthquake.

[0029] Specifically, after identifying the top and bottom reflection interfaces of the magma diapir in step S20, the time coordinates corresponding to the top and bottom reflection interfaces of the magma diapir can be directly read. Then, the time difference between the top and bottom reflection interfaces is calculated; this time difference is the two-way seismic travel time between the upper and lower interfaces of the magma diapir (i.e., the top and bottom reflection interfaces). For time-domain seismic data, direct reading is sufficient; for depth-domain seismic data, conversion to the time domain is required using a time-depth relationship. This time-depth conversion can be achieved using a time-depth conversion formula, as follows: (1); In the formula, D is the depth in meters (m); C is the two-way seismic travel time between the upper and lower interfaces of the magma diapir in milliseconds (ms).

[0030] Step S40: Based on the two-way travel time of the earthquake, combined with the magma diapiric data and using the uplift calculation model, calculate the R value at each location.

[0031] In some embodiments, the R-values ​​at each location are obtained by combining seismic two-way travel time with magmatic diapiric data and using a uplift calculation model. This includes: converting the seismic two-way travel time to depth to obtain the thickness of the magmatic diapiric; determining the uplift elevation difference and the original stratum thickness based on the magmatic diapiric data; and calculating the R-values ​​at each location using the uplift calculation model based on the thickness of the magmatic diapiric, the uplift elevation difference, and the original stratum thickness. In this embodiment, the R-value at each location refers to the vertical distance of the uplifted area caused by the magmatic diapiric. Each location refers to each position of a single magmatic diapiric. It can be understood that an ideal magmatic diapiric is similar to a cone, and the R-values ​​that can be measured on each seismic profile are variable values, not completely fixed values.

[0032] The calculation model for the uplift volume is as follows: (2); Where R represents the diapiric uplift; T represents the thickness of the magmatic diapiric body; h represents the uplift height difference; and H represents the thickness of the original strata.

[0033] In some embodiments, the uplift difference is determined by: determining the seismic time interval between the bottom of the magmatic body and the top of the stratum deformation based on magmatic diapirs; and performing time-depth conversion on the seismic time interval to obtain the uplift difference.

[0034] The seismic time interval between the bottom of the magma core and the top of the strata refers to the final travel time caused by deformation after the deep magma diapir uplift.

[0035] In some embodiments, the original formation thickness is determined by: obtaining the time difference and formation velocity from the bottom of the magmatic body to the undeformed stratum based on magmatic diapirs; calculating the undeformed formation thickness based on the time difference and formation velocity; determining the formation thickness below the highest intrusion point; and calculating the original formation thickness based on the undeformed formation thickness and the formation thickness below the highest intrusion point.

[0036] Specifically, in this step, the R value can be obtained using the following method: First: Based on the two-way earthquake travel time of the upper and lower interfaces of the magma diapiric body determined in step S30, the time-depth conversion is performed using formula (1) to convert the earthquake time into depth and obtain the thickness T of the magma diapiric body. Secondly, based on the earthquake time interval between the bottom of the magmatic rock mass and the top of the stratum deformation, the time-depth conversion is performed using formula (1) to convert the earthquake time into depth and obtain the uplift height difference h. Next, the time difference between the bottom of the magmatic mass and the undeformed strata was obtained. Formation velocity Based on the time difference from the bottom of the magmatic mass to the undeformed stratum Formation velocity Calculations were performed to obtain the thickness of the undeformed strata. The specific calculation formula is as follows: ; Formation velocity The average velocity of seismic waves passing through rock strata is expressed in meters per second. Its value can fluctuate within a range of ±10% to define the uncertainty range of the magma diapiric recovery height R value.

[0037] Then, determine the formation thickness below the highest intrusion point. And based on the thickness of the strata below the highest intrusion point and thickness of undeformed strata The original thickness H of the formation is obtained through calculation. The specific calculation formula is as follows: ; in, The value is consistent with the value of the thickness T of the magma diapiric body.

[0038] Finally, based on the obtained thickness T of the magmatic diapiric body, the uplift difference h, and the original thickness H of the strata, the diapiric uplift R value is obtained by using formula (2).

[0039] Based on the aforementioned method for calculating R-values, the R-values ​​at each location are quantitatively calculated. Specifically, the major and minor axis extension directions of the magma diapir are obtained through 3D seismic interpretation. Profiles are selected along the span of the magma diapir, and the R-values ​​at each location are calculated progressively. The seismic profile is shown below. Figure 4 As shown.

[0040] Step S50: Construct a profile based on the R value to obtain multiple profile lines.

[0041] Specifically, in this step, after calculating the R value at each location through step S40, a profile is constructed based on the calculated R value at each location to obtain multiple profile lines, thereby constructing the external morphology of the magma diapiric uplift.

[0042] Step S60: Determine the ratio function.

[0043] Specifically, in this step, after obtaining the external morphology of the magma diapiric uplift through step S50, parabolic fitting is used to calculate the cross-sectional area A and volume parameter V of the magma diapiric. Based on the calculated R values ​​at each location, the ratio functions of R² / A and R³ / V are constructed respectively.

[0044] Step S70: Identify abnormal raised areas based on the ratio function.

[0045] Specifically, in this step, the abnormal uplift areas are identified based on the R² / A ratio function and R³ / V ratio function constructed in step S60. Specifically, when both R² / A and R³ / V are greater than 0, the uplift area is considered an abnormal uplift area; when both R² / A and R³ / V are equal to 0, it represents the boundary of the abnormal uplift, indicating parallel strata distribution.

[0046] Step S80: Based on the R value of each profile line, reverse the calculation and combine it with the abnormal uplift area to restore the ancient landform of the rift basin.

[0047] Specifically, after identifying the anomalous uplift area in step S70, the original stratigraphic bedding position is inferred from the R value calculated for each profile line. A smaller R value indicates a smaller uplift amplitude, thus predicting the deformation boundary of the forced fold. Geomorphological restoration stops when the R value reaches 0, completing the bedding boundary closure and thus the restoration and reconstruction of the paleomorphology of the rift basin. In other words, by identifying the anomalous uplift area and using the R value to infer its location until it reaches 0, the external morphology or influence range of the anomalous uplift can be described. The external morphology or influence range of this anomalous uplift indicates the extent of stratigraphic erosion caused by the upwelling of the magma diapirs. After obtaining the external morphology or influence range of the anomalous uplift, the original stratigraphic thickness can be obtained by adding the current residual stratigraphic thickness to the uplift amplitude of the magma diapirs.

[0048] Finally, the reconstructed 3D paleogeographic map is output to verify its good consistency with the morphology of the surrounding unintruded areas, so as to be used for subsequent oil and gas exploration research.

[0049] The following example uses a basin as an illustration.

[0050] Taking a structural profile of a certain area in the Kaiping Depression of a basin as an example, the core parameters are quantitatively explained: This embodiment targets the Kaiping depression area of ​​the basin in the region and quantitatively reconstructs the paleomorphological disturbance caused by the magmatic diapiric body. The "ternary restoration model" proposed in this invention is used to accurately calculate the uplift of the magmatic diapiric body. The ternary restoration model is shown in formula (2).

[0051] The two-way seismic travel time between the upper and lower interfaces of the magma diapir is 3750 ms to 5250 ms. Using the time-depth conversion formula in formula (1), the time can be converted to depth to obtain the thickness T of the magma diapir. Specifically: T=D(5250)−D(3750)=2476.80m.

[0052] The seismic time interval between the bottom of the magmatic rock mass and the top of the strata deformation is 2125 ms. Using the time-depth conversion formula in formula (1), the time can be converted to depth to obtain the uplift height difference h. Specifically: h=D(5250)−D(2125)=4652.19m.

[0053] The time range of the undeformed sedimentary strata is 1750 ms to 2550 ms, with a time difference of 800 ms, or 0.8 s. The intrusive bodies in the Kaiping Depression are predominantly ferromagnesian; therefore, 5550 ± 10% m / s is used as the intrusion velocity, and the average value is taken. =5550m / s, then: =0.8×5550=4440m.

[0054] Therefore, we can obtain: =2476.80+4440.00=6916.80m.

[0055] Substituting the data obtained from the above calculations into formula (2) yields: R=2476.80+4652.19−6916.80=212.19m.

[0056] The above calculation results show that, after quantitatively eliminating the interference of magmatic diapirs, the actual vertical disturbance of the target profile under the geomorphological restoration conditions is 212.19 m, which is reasonable given the regional geological background. This embodiment verifies the applicability and effectiveness of the method of the present invention in quantitative geomorphological restoration.

[0057] The R value calculated by this invention can be used to construct paleogeographic reconstruction of rift basins, as well as for sedimentary simulation, oil and gas reservoir prediction, or geological modeling.

[0058] refer to Figure 5 The present invention also provides a device for restoring ancient landforms in fault basins.

[0059] Specifically, such as Figure 5 As shown, the paleogeographic reconstruction device for the rift basin includes: The data acquisition unit 601 is used to acquire seismic profile data of the target basin.

[0060] Interface recognition unit 602 is used to identify the top and bottom reflection interfaces of a magma diapir based on seismic profile data.

[0061] Time analysis unit 603 is used to determine the two-way travel time of an earthquake based on the top and bottom reflection interfaces of a magma diapir.

[0062] The calculation unit 604 is used to calculate the R value at each location based on the two-way travel time of the earthquake, combined with the magma diapiric data and the uplift calculation model.

[0063] Profile building unit 605 is used to build profiles based on R value to obtain multiple profile lines.

[0064] Function determination unit 606 is used to determine the ratio function.

[0065] Anomaly identification unit 607 is used to identify abnormal raised areas based on a ratio function.

[0066] Geomorphological restoration unit 608 is used to back-calculate based on the R value of each profile line and restore the paleomorphology of the fault basin in combination with the abnormal uplift area.

[0067] Specifically, the specific operational process of the various units in the rift basin paleogeographic restoration device can be referred to the above-mentioned rift basin paleogeographic restoration method, and will not be repeated here.

[0068] The paleogeographic restoration method for rift basins of the present invention proposes a three-element quantitative model of diapiric uplift (i.e., formula (2)), which for the first time uses physical parameters to quantitatively characterize the degree of diapiric influence; through multi-scale fusion (profile + plane + volume) reconstruction, it ensures the realization of integrated restoration of structure-geomorphology-sedimentation; and can achieve adaptive identification of boundaries and restoration thickness in areas with strong diapiric interference, thereby improving the scientificity and rationality of reconstruction; and can be compatible with current mainstream seismic inversion platforms and modeling software, thus possessing strong applicability.

[0069] Furthermore, an electronic device of the present invention includes a memory and a processor; the memory is used to store a computer program; the processor is used to execute the computer program to implement the paleogeographic restoration method for rift basins as described above. Specifically, according to embodiments of the present invention, the processes described above with reference to the flowchart can be implemented as computer software programs. For example, embodiments of the present invention include a computer program product comprising a computer program carried on a computer-readable medium, the computer program containing program code for performing the methods shown in the flowchart. In such embodiments, when the computer program is downloaded, installed, and executed by an electronic device, it performs the functions defined in the methods of the embodiments of the present invention. The electronic device in the present invention can be a terminal such as a laptop, desktop computer, tablet computer, or smartphone, or it can be a server.

[0070] Furthermore, one type of storage medium of the present invention stores a computer program thereon, which, when executed by a processor, implements the paleogeographic restoration method for rift basins described above. Specifically, it should be noted that the storage medium described above in the present invention can be a computer-readable signal medium or a computer-readable storage medium, or any combination thereof. A computer-readable storage medium can be, for example, but not limited to, an electrical, magnetic, optical, electromagnetic, infrared, or semiconductor system, apparatus, or device, or any combination thereof. More specific examples of a computer-readable storage medium may include, but are not limited to: an electrical connection having one or more wires, a portable computer disk, a hard disk, random access memory (RAM), read-only memory (ROM), erasable programmable read-only memory (EPROM or flash memory), optical fiber, portable compact disk read-only memory (CD-ROM), optical storage device, magnetic storage device, or any suitable combination thereof. In the present invention, a computer-readable storage medium can be any tangible medium containing or storing a program that can be used by or in conjunction with an instruction execution system, apparatus, or device. In the present invention, a computer-readable signal medium can include a data signal propagated in baseband or as part of a carrier wave, wherein computer-readable program code is carried. The transmitted data signal can take various forms, including but not limited to electromagnetic signals, optical signals, or any suitable combination thereof. The computer-readable signal medium can also be any computer-readable medium other than a computer-readable storage medium, which can send, propagate, or transmit a program for use by or in connection with an instruction execution system, apparatus, or device. The program code contained on the computer-readable medium can be transmitted using any suitable medium, including but not limited to: wires, optical fibers, RF (radio frequency), etc., or any suitable combination thereof.

[0071] The aforementioned computer-readable medium may be included in the aforementioned electronic device; or it may exist independently and not assembled into the electronic device.

[0072] The various embodiments in this specification are described in a progressive manner, with each embodiment focusing on its differences from other embodiments. Similar or identical parts between embodiments can be referred to interchangeably. For the apparatus disclosed in the embodiments, since they correspond to the methods disclosed in the embodiments, the description is relatively simple; relevant parts can be referred to the method section.

[0073] Those skilled in the art will further recognize that the units and algorithm steps of the various examples described in conjunction with the embodiments disclosed herein can be implemented in electronic hardware, computer software, or a combination of both. To clearly illustrate the interchangeability of hardware and software, the components and steps of the various examples have been generally described in terms of functionality in the foregoing description. Whether these functions are implemented in hardware or software depends on the specific application and design constraints of the technical solution. Those skilled in the art can use different methods to implement the described functions for each specific application, but such implementations should not be considered beyond the scope of this invention.

[0074] The steps of the methods or algorithms described in conjunction with the embodiments disclosed herein can be implemented directly by hardware, a software module executed by a processor, or a combination of both. The software module can be located in random access memory (RAM), main memory, read-only memory (ROM), electrically programmable ROM, electrically erasable programmable ROM, registers, hard disk, removable disk, CD-ROM, or any other form of storage medium known in the art.

[0075] The above embodiments are only for illustrating the technical concept and features of the present invention, and are intended to enable those skilled in the art to understand the content of the present invention and implement it accordingly. They do not limit the scope of protection of the present invention. All equivalent changes and modifications made within the scope of the claims of the present invention should fall within the scope of the claims of the present invention.

Claims

1. A method for recovering a paleogeomorphology of a rifted basin, characterized by, The method comprises the following steps: obtaining seismic profile data of a target basin; identifying top and bottom reflection interfaces of a magma diapir according to the seismic profile data; determining seismic two-way travel time based on the top and bottom reflection interfaces of the magma diapir; calculating R values at different positions based on the seismic two-way travel time, combining magma diapir data and using uplift amount calculation model; constructing profiles based on the R values to obtain a plurality of profile lines; determining a ratio function; identifying an abnormal uplift area according to the ratio function; restoring a paleogeomorphology of a rift basin according to the R values of each profile line and combining the abnormal uplift area.

2. The method according to claim 1, wherein, The identifying of the top and bottom reflection interfaces of the magma diapir according to the seismic profile data comprises: determining profile amplitude anomaly data and reflection energy variation according to the seismic profile data; identifying the top and bottom reflection interfaces of the magma diapir on the profile according to the profile amplitude anomaly data and reflection energy variation and combining well-controlled stratum data.

3. The method according to claim 1, wherein, The determination of the seismic two-way travel time based on the top and bottom reflection interfaces of the magma diapir comprises: obtaining corresponding seismic reflection signals according to the top and bottom reflection interfaces of the magma diapir; identifying seismic reflection characteristics of the seismic reflection signals to obtain the seismic two-way travel time.

4. The method according to claim 1, wherein, The calculation of the R values at different positions based on the seismic two-way travel time, combining magma diapir data and using uplift amount calculation model comprises: performing time-depth conversion on the seismic two-way travel time to obtain thickness of the magma diapir; determining uplift height difference and original stratum thickness according to the magma diapir data; calculating the R values at different positions according to the thickness of the magma diapir, the uplift height difference and the original stratum thickness and using the uplift amount calculation model.

5. The method according to claim 4, wherein, The uplift height difference is determined by: determining seismic time interval between the bottom of the magma rock mass and the top of the deformed stratum according to the magma diapir data; performing time-depth conversion on the seismic time interval to obtain the uplift height difference.

6. The method according to claim 4, wherein, The original stratum thickness is determined by: obtaining time difference and stratum velocity from the bottom of the magma rock mass to the un-deformed horizon according to the magma diapir data; calculating un-deformed stratum thickness according to the time difference and the stratum velocity; determining stratum thickness below the highest intrusion point; calculating the original stratum thickness according to the un-deformed stratum thickness and the stratum thickness below the highest intrusion point.

7. The method according to any one of claims 1 to 6, wherein, The uplift amount calculation model is: ； wherein, R represents the diapir uplift amount; T represents the thickness of the magma diapir; h represents the uplift height difference; H represents the original stratum thickness.

8. A device for recovering a palaeogeomorphology of a rifted basin, characterized in that, The method comprises: a data acquisition unit configured to obtain seismic profile data of a target basin; an interface identification unit configured to identify top and bottom reflection interfaces of a magma diapir according to the seismic profile data; a time analysis unit configured to determine seismic two-way travel time based on the top and bottom reflection interfaces of the magma diapir; a calculation unit configured to calculate R values at different positions based on the seismic two-way travel time, combining magma diapir data and using uplift amount calculation model. The profile construction unit is configured to construct a profile based on the R value, and obtain a plurality of profile lines; The function determination unit is configured to determine a ratio function; The anomaly identification unit is configured to identify an abnormal uplift area according to the ratio function; The geomorphology recovery unit is configured to recover a paleogeomorphology of the rift basin by backstepping according to the R value of each profile line and combining the abnormal uplift area.

9. A storage medium, characterized by The storage medium stores a computer program, which is adapted to be loaded by the processor to execute the steps of the method for recovering the paleogeomorphology of the rift basin according to any one of claims 1 to 7.

10. An electronic device, comprising: The device comprises a memory and a processor, and the memory stores a computer program. The processor executes the steps of the method for recovering the paleogeomorphology of the rift basin according to any one of claims 1 to 7 by calling the computer program stored in the memory.

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