Crustal structure and geothermal mechanism of Gonghe-Guide Basin based on EIGEN-6C4 satellite gravity and aeromagnetic data

Crustal structure and geothermal mechanism of Gonghe-Guide Basin based on EIGEN-6C4 satellite gravity and aeromagnetic data | Research Square window.SnipcartSettings = { analytics: { enabled: false } }; (function() { var accessVector = localStorage.getItem('access_vector') || ''; window.dataLayer = window.dataLayer || []; if (accessVector) { window.dataLayer.push({ user: { profile: { profileInfo: { snid: accessVector } } } }); } })(); (function(w,d,s,l,i){w[l]=w[l]||[];w[l].push({'gtm.start':new Date().getTime(),event:'gtm.js'});var f=d.getElementsByTagName(s)[0],j=d.createElement(s),dl=l!='dataLayer'?'&l='+l:'';j.async=true;j.src='https://www.googletagmanager.com/gtm.js?id='+i+dl;f.parentNode.insertBefore(j,f);})(window,document,'script','dataLayer','GTM-K279D39R'); Browse Preprints In Review Journals COVID-19 Preprints AJE Video Bytes Research Tools Research Promotion AJE Professional Editing AJE Rubriq About Preprint Platform In Review Editorial Policies Our Team Advisory Board Help Center Sign In Submit a Preprint Cite Share Download PDF Research Article Crustal structure and geothermal mechanism of Gonghe-Guide Basin based on EIGEN-6C4 satellite gravity and aeromagnetic data Wenna Zhou, Qiang Li, Dailei Zhang, Hai Tang This is a preprint; it has not been peer reviewed by a journal. https://doi.org/ 10.21203/rs.3.rs-2249266/v1 This work is licensed under a CC BY 4.0 License Status: Published Journal Publication published 01 Jun, 2023 Read the published version in Pure and Applied Geophysics → Version 1 posted 3 You are reading this latest preprint version Abstract Gonghe-Guide Basin is situated in the northeastern edge of the Tibetan Plateau. one of China's main targets for geothermal research and exploitation. It is also a crucial region for studying the Tibetan Plateau's uplift mechanisms. Therefore, the elaborate crustal structure of the entire basin is essential for recognizing the geothermal mechanisms, geothermal source targets and even the uplift mechanisms of the Tibetan Plateau. However, these issues remain enigmatic, partly because it is difficult to depict the crustal structure of entire base by using the profile results of magnetotelluric and seismic data. To overcome the limitations of profile results, we present a new crustal structure of the entire Gonghe-Guide Basin by using EIGEN-6C4 satellite gravity and aeromagnetic data. The gravity and magnetic data were processed using the wavelet multi-scale decomposition method and the iterative compact depth from extreme points imaging method. Satisfactory residual anomalies and inversion results were obtained. The gravity inversion results reveal pronounced low-density regions at the depths of 15–35 km in the middle-upper crustal, most likely caused by partial melting from heating the overlying hot dry rocks. The results correspond well with the magnetotelluric and seismic results and are an effective supplement. The magnetic inversion results show negative or no magnetism within a similar depth range. But at shallow depths of the same horizontal positions, there is high positive magnetism, which can be interpreted as granite. To confirm and validate this conclusion, a 2D geologic model of a profile from a typical area is created to show the detailed tectonic. Based on the new crustal structure results, the suggested geothermal target is the low/negative density corresponding to low/negative magnetism located at deep depths and high/ positive magnetism located at shallow depths. These density and magnetism anomalies are primarily located near the town of Guide, Gonghe, Xinjie, Chaka, Wayuxiangka, Tanggemu, Xinhai, which can be considered geothermal source targets. The geothermal source is thought to be due to mantle material upwelling or faults activity causing partial melting in the crust, and heat flows from deep to shallow along the faults in the region. Then we established a geological conceptual model to illustrate this process. This indicates that tectonic movement is taking place in the deep part of the earth in Gonghe-Guide Basin. The research on the geological structure and geothermal heat source mechanism in the Gonghe-Guide Basin can provide a primary reference for research on geothermal resources in other areas with similar geological structures. Satellite gravity Crustal structure Magnetic anomalies and interpretation Heat generation and transport Geothermal mechanisms Figures Figure 1 Figure 2 Figure 3 Figure 4 Figure 5 Figure 6 Figure 7 Figure 8 Figure 9 Figure 10 Figure 11 Figure 12 Figure 13 1. Introduction The Gonghe-Guide Basin is a structurally complex basin located at the northeastern edge of the Tibetan Plateau. It is currently one of the main targets for geothermal research and exploitation in China (Zhao et al., 2009 ; Xu et al., 2018a ). It is also considered one of the most crucial regions for studying the uplift mechanisms of the Tibetan Plateau (Clark and Royden, 2000 ; Zhang et al., 2011 ; Gao et al., 2020 ). In particular, with the increasing demand for clean energy, detecting geothermal energy requires new exploration techniques for widespread implementation (Li et al., 2015 ; Wang et al., 2018 ; Wang et al., 2018 ). A better understanding of the tectonic activity, geologic structures, and distribution characteristics of deep materials will also allow for increased geothermal detection and implementation. Furthermore, as an essential foundation for geothermal energy exploration in China (Wang et al., 2021 ), the research on the geological structure and geothermal heat source mechanism in the Gonghe-Guide Basin can provide a primary reference for research on geothermal resources in other areas that have similar geological structure. The Gonghe-Guide Basin is a faulted basin surrounded by fault-fold uplift mountains. The foothills of the Qinghainanshan Fault border it to the north, the Animaqing Suture Zone (an extension from Kunlun Fault (KLF)) to the south, the Wahongshan Fault to the west, and the Duohemao Fault to the east (Zheng et al., 2010 ) (Fig. 1 and Fig. 2 a). The main faults are extensive NW trending sinistral strike-slip thrust faults (Fang et al., 2005 ; Zhang et al., 2020a ). Hydrothermal and hot dry rocks (HDRs) have been found throughout the Gonghe-Guide area (Gao et al., 2018 ; Zhang C. et al., 2018 ). HDRs exceeding 200°C have been recently detected in the GR1 borehole (the red sign in Fig. 1 ) with temperatures up to 236°C at a bottom depth of 3705 m, a first in China (Zhang S. et al., 2018 ). The Gonghe-Guide Basin is now considered to have great potential for geothermal energy exploration and development. Previous studies have obtained numerous geophysical surveys and extensive subsurface data to delineate crustal structures across the Gonghe-Guide Basin. Geophysical surveys have been conducted, including magnetotelluric (MT), seismic, gravity, and magnetic methods (Li et al., 2018 ; Gao et al., 2018 ; Gao et al., 2020 ; Zhao et al., 2020a ). Three-dimensional MT imaging indicated a conductive layer in the middle-upper crustal in the southeastern Gonghe-Guide Basin and a possible magma chamber near Gonghe town (Gao et al., 2018 ). Zhang et al. ( 2020b ) and Tang et al. ( 2021 ) also found partial melting at depths of 15–35 km in the Gonghe-Guide Basin using MT data. In addition, seismic results also show partial melting with low-velocity zones at depths of 1–10 km, 25–40 km, and approximately 60 km in the basin (Zhang et al., 2019 ). With multiple geophysical datasets, Zhao et al. ( 2020b ) proposed a conceptual geothermal model for the Gonghe Basin with MT, seismic, MD, and CPD evidence. Zhao et al. ( 2020a ) used 2D manual inversion and 3D cross-gradient joint inversion of the gravity and magnetic data collected from Qiabuqia, and indicated that this area is overlain by sedimentary layers approximately 1000–1500 m in thickness. Wang et al. ( 2021 ) inversed Moho depth and Curie point depth in and around the basin using gravity and magnetic data using an improved Parker-Oldenburg algorithm. Then, they established different thermal models and concluded that the high heat flow in the Gonghe-Guide Basin coacted with radiogenic heat. In summary, studies have primarily focused on seismic and MT profiles and obtained the characteristics of local areas (Gao et al., 2018 ; Zhao et al., 2020b ). Inversion interpretation of gravity data and magnetic data have also been performed, emphasizing the inversion of the interface, which reflects the fluctuation characteristics of the Moho surface and Curie point depth (Zhao et al., 2019 ; Zhao et al., 2020b ; Wang e al., 2021). However, subject to the accuracy and resolution of previous gravity and magnetic data, no complete three-dimensional crust structure has been established despite the limitations of the data processing methods. Therefore, it is difficult to research the entire basin's three-dimensional distribution characteristics of geological bodies. Furthermore, there is a lack of comprehensive research on a large-scale and overall lithologic distribution of the entire basin, from shallow to deep. Therefore, there are many discrepancies on the geothermal mechanisms across the entire Gonghe-Guide Basin. To obtain the crust structure and further describe the geothermal mechanism of the Gonghe-Guide Basin, we present a detailed study of the Gonghe-Guide Basin based on EIGEN-6C4 satellite gravity and aeromagnetic data using the wavelet multi-scale decomposition (WMSD) method and iterative compact depth from extreme points imaging (ICDXEP) method (a fast inversion method can process the large data volume). First, we obtained the residual and regional fields using the WMSD method. Then, the lithologic distribution and crustal structure of the whole basin were inversed using the ICDEXP method with little constraint. In addition, to verify and reflect the accuracy of inversion, a 2D geologic model from typical area is created to show the detailed tectonic. Finally, target areas of geothermal resources are proposed, including their geophysical characteristics for detection. And then geological conceptual model was used to determine the relationships between the deep crustal structure and geothermal source. 2. Geologic Setting The Gonghe-Guide Basin is located north of the KLF and between the Qaidam Basin and Qinling Orogen (Zhang et al., 2006 ). Tectonically, the Gonghe-Guide Basin is a Cenozoic intermontane basin controlled by the KLF and Altyn Tagh Fault (ATF) (Fig. 1 ; Fang et al., 2005 ). To the north, it is bordered by the foothills of the Qinghainanshan (QHNS) Fault, to the south by the Animaqing Suture Zone (extension from KLF), to the west by the Wahongshan Fault, and to the east by the Duohemao fault (Zhang et al.,2006). Between these first-order strike-slip faults, there are numerous secondary thrust faults, including the faults along Qaidam Basin, Qinghainanshan (QHNS), and Gonghenanshan (GHNS), which contributed to the shortening and uplift of the mountains (Zhang et al., 2020a ). Within the basin, the QHNS and GHNS are two prominent narrow ranges and thus comprise the range and basin landscapes in the interior of the northeastern Tibetan Plateau (Fig. 2 a; Craddock et al., 2014 ; Zhang et al., 2012 ). The geologic map (Fig. 1 ) shows that surface is covered by the Quaternary system interior of the basin and its peripheral sporadic Neogene sediments (Sun et al., 2011 ). The Neoarchean-Early Proterozoic Jinshuikou Group is exposed in the southwest orogenic belt around the basin. The Early Proterozoic Daken-Daban Group is exposed in the northwest. The early Middle Triassic Longwuhe Group is exposed in the south, north, and east of the basin margin orogenic belt. Indosinian granites are primarily exposed in the west, north, and east of the orogenic belt around the basin. Multiple intrusions of different types of magma in the Indosinian period formed a compound granite batholith, which constitutes the main body of the basement of the Gonghe-Guide basin (Zhang et al., 2021 ). In the post-collision period, lithosphere delamination occurred due to crustal thickening, and Late Triassic hot spring rocks developed on the east and west sides of the southern basin (Shi et al., 2018 ). Many hydrothermal springs have been discovered along the NE–SW, and NS extending faults (Liu et al. 2017 ), and the hot water comes from the deeper part of the basin (~ 1000 m) (Fang et al., 2009 ). Thermal survey results also reveal excellent geothermal conditions in this basin due to the geothermal gradient and terrestrial heat flow. Based on geophysical detection results, there is a conductive layer in the middle-upper crustal in the southeastern Gonghe Basin and a possible magma chamber near Gonghe town (Gao et al., 2018 ). There is a partial melting body at depths of 15–35 km in the western Gonghe Basin (Zhang et al., 2020b ). The results have also been verified by seismic results (Zhang et al., 2019 ). However, seismic and MT methods mainly indicated profile results (2D cross section). It is difficult to display the geologic distribution characteristics of the entire basin. Therefore, gravity and magnetic data are used in this paper to further explore on the relationship between the geothermal heat source mechanism and crustal structure. 3. Data And Materials 3.1 EIGEN-6C4 satellite gravity data Satellite gravity observation technology has high coverage, precision and resolution, which significantly compensates for the deficiency of ground gravity measurements. To effectively analyze the density structure of the Gonghe-Guide Basin, the EIGEN-6C4 satellite gravity data was used in this study. EIGEN-6C4 is a static global combined gravity field model up to degree and order 2190 (Foerste et al., 2014 ). The gravity model is high resolution (9 km) and precision (2.73 mGal). Figure 2 a is the topographic data, and Fig. 2 b shows the Bouguer gravity anomaly with a grid spacing of 5 km of the Gonghe-Guide area. The Bouguer gravity anomaly (Fig. 2 b) ranges from − 520 to -320 mGal in the study area. The characteristic of gravity anomaly agrees well with the topographic data (Fig. 2 a). The low values in the southwest are the Kunlun Mountains, with high elevations and, therefore, a thick crust. The gravity value increases from the southwest part to the northeast. The high values in the northwest are the Xining Basin. In the Gonghe-Guide Basin, the gravity anomaly has relatively few dramatic changes. The gravity anomalies and fault structure zones also correspond well. 3.2 Aeromagnetic data Magnetic anomaly maps provide insight into the subsurface structure and composition of the Earth’s crust. The aeromagnetic anomaly grid used in our study area was derived from China Geological Survey (CGS). The aeromagnetic grid has a 2 km resolution grid of the magnetic intensity anomaly. The total field magnetic anomalies in the study area range between − 250 nT and 360 nT (Fig. 3 a). The magnetic anomalies in the Gonghe-Guide Basin are generally weak and evenly distributed. The prominent high magnetic anomalies are distributed in the structural belt around the basin. The dipole nature of magnetic anomalies makes them more challenging to interpret in terms of geological structure. Thus, an initial process of removing/minimizing the inclination effect is transforming the TMI map into the Differential Reduction to the Pole (DRTP) map (Arkani-Hamed, 2007 ). This DRTP transform reduces the magnetic anomalies to the pole and corrects for variation in inclination and declination over the study area, assuming that all magnetization is induced. The mean inclination and declination values for the center of the study area (Fig. 3 a) are 55.37° and − 1.29°, respectively. A comparative analysis of the aeromagnetic results can delineate the boundaries of the basin. Some differences exist between the RTP magnetic and gravity anomalies. More detailed aspects of their differences are discussed in the discussion of gravity and magnetic data inversion results. 4. Methodology This paper carries out multi-scale data processing and analysis of satellite gravity and aeromagnetic data to obtain more precise geological structure interpretation results. 4.1 Wavelet multi-scale decomposition method for potential field data separation The observed potential field data are the sum of gravity and magnetic effects at various depths in the subsurface half-space. The target anomalies must first be separated from the observed gravity and magnetic anomalies to study a specific geological problem using gravity and magnetic data. A variety of methods are proposed for separating gravity anomalies, such as upward continuation (Jacobsen, 1987), matched filtering (Spector and Grant, 1970 ), polynomial fitting (Telford et al., 1990 ), Wiener filtering (Pawlowski and Hansen, 1990 ), preferential continuation (Pawlowski, 1995 ), wavelet transformation multiple-scale decomposition (Fedi and Quarta, 1998 ) and nonlinear filtering (Keating and Pinet, 2011 ). The wavelet multi-scale decomposition (WMSD) method is helpful for decomposing the gravity and magnetic data to obtain residual and regional anomalies at different depths (Fedi and Quarta 1998 ; Xu et al., 2015 ; Xu et al., 2017 ). Yang et al. ( 2015 ) used the WMSD method to obtain the gravity effects at various depths of the Tibet Plateau and analyzed the geological structure at different depths. Xu et al. ( 2018 ) also used an improved WMSD method to analyze the gravity anomaly of the Tibet Plateau. The quality of results of WMSD method depends on wavelet basis function and decomposition terms. It has been shown that the “Coif3” wavelet basis function can be used to obtain the best decompose result (Xu et al., 2017 ). The decomposition terms need to be specific for different data. It depends on the depth of the equivalent layer. Therefore, the “Coif3” wavelet basis function was used to implement the potential field separation in this paper. First, we decomposed the gravity and magnetic data, and multi-scale data were obtained. The average depths of the equivalent layers were estimated using a radially averaged logarithm power spectrum. Then, the residual anomaly (generated by crustal) and regional anomaly (generated by Moho) were obtained. Finally, the crustal structure was inverted using the residual anomaly. 4.2 Iterative compact depth from extreme points imaging algorithm Inversion of potential field data is a powerful interpretation tool that provides a meaningful description of the source distribution (magnetization or density). Inversion methods are computationally expensive; moreover, the source models depend on the a priori information and constraints (Pilkington 1996 ). In studying the crustal structure, it is often difficult to carry out inversion calculations directly because of the large amount of data and few constraints. In addition to inversion, imaging methods may provide a fast preliminary picture of the source distribution. Various imaging methods have been proposed and used to solve different problems (Fedi et al., 2012). It can provide an initial source model to be improved with more refined inversion algorithms. Depth from Extreme Points (DEXP) image method is a popular method. It has been successfully applied in target locations (Paletti et al., 2020), geologic source imaging (Milano et al.., 2016 ; Paoletti et al, 2016 ), and other studies. Based on the DEXP image method, Baniamerian et al. ( 2016 ) proposed a new algorithm called “Compact Depth from Extreme Points,” which iteratively produces different source distribution models with an increasing degree of compactness and, correspondingly, increasing source-density values. Liu et al. ( 2020 ) compared the ICDEXP method with the inversion method and found that the ICDEXP method does not require any matrix inversions, so extensive RAM is not needed, and the solution can converge faster than the inverse algorithm. Furthermore, the results of the ICDEXP and inversion method are very similar. Therefore, this paper used the ICDEXP method to invert residual anomalies and obtain crustal structure. 5. Results 5.1 The results of potential data separation Figure 4 shows the results of WMSD, and the depth was calculated using the radially averaged logarithm power spectrum. In the wavelet decompositions, the regional component of the 4th terms of wavelet decomposition corresponds to a depth of 55 km, the average depth to the Moho (Shen et al., 2016 ; Gao et al., 2020 ). Therefore, its regional component can be believed to be caused by Moho. The distribution characteristics correspond to the Moho undulation. Therefore, we can use the result to calculate the depth of Moho, and the sum of 1st, 2nd, 3 rd, and 4th detail features of the wavelet decomposition can be used as the residual anomaly. The depths of 1st + 2nd, 3rd, and 4th wavelet decomposition are 5 km, 20 km, and 45 km. Compared with the original gravity anomaly, the characteristics of positive and negative local field alternation are more prominent. The overall characteristics of low in the southwest and high in the northeast were removed, indicating that the influence of the fluctuation characteristics of the deep Moho is removed, and the crustal density structure can be obtained. In the interior of the basin, there are large areas of negative gravity anomalies. There are also apparent negative anomalies near the Wahongshan and Xinjie faults. Overall, there are numerous low-density anomaly field sources in the crust. The gradient zone with sharp changes in NNW direction between 101 ° E and 102 ° E in the east of the working area appears to be caused by the Xinjie fault. The fault is ~ 20 km wide and has a prominent semi-flower structure (Zhang et al., 2020a ). It is the western boundary of the Guide Basin and the boundary between the Guide and Gonghe Basins. It mainly exposes banded Indosinian granites formed by sliding melting carried by the fault (Zhang et al., 2007 ). Near the Xinjie fault, it is inferred that these hot springs correspond to this low-density gravity anomaly zone, and abundant hot springs are exposed nearby. The NW trending gradient zone with abnormally sharp changes distributed in the west is caused by hidden faults such as the Guinan Nanshan fault, Wahongshan-Wenquan fault, and Wayuxiangka-Guinan fault. Intermittent strip or elliptical low-density gravity anomalies correspond to negative landforms such as intermountain basins and valleys. Generally, it is inferred that NW trending structures control the distribution of low-density bodies near the Gonghe Basin in the west, and the distribution of low-density bodies near the Guide basin in the east is controlled by NNW trending structures. Similarly, we use the WMSD to separate the residual and regional anomalies of magnetic data. Firstly, residual results of the 1st, 2nd, 3rd, and 4th (Fig. 5 ) were obtained, and the equivalent depths were calculated using a radially averaged logarithm power spectrum. To compare with geological information, the depth of 1st + 2nd, 3rd, and 4th wavelet decomposition is 3 km, 9 km, and 15 km. Then the sum of the 1st, 2nd, 3rd, and 4th detail features of the wavelet decomposition can be used as the residual anomaly because the magnetism disappears under the Curie point depth. The residual magnetic anomaly obtained after removing the regional field can be regarded as the distribution of magnetic anomaly generated by the substances above the Curie point depth. The main distribution directions of magnetic anomaly strips are NNW and NW, which are consistent with the main distribution directions of gravity anomalies. The main distribution direction in the western Gonghe Basin is NW, and NNW in the eastern Guide Basin. The weak magnetism is distributed in the Gonghe-Guide Basin. The monotonous and unvaried magnetic fields are generated by the overlying sedimentary rocks. Around the basin, positive and negative magnetic anomalies are distributed alternately in strips, which are close to the strike of main faults. The maximum value is 350 nT, which may be caused by granite intruding along the fault and its alteration zone. The magnetic anomaly is more prominent in the boundary characteristics of the basin, and the basin is controlled by NNW and NW deep faults. This may be related to the Gonghe-Guide Basin being a faulted basin controlled by late-stage faults and magmatic intrusions. Thick sedimentary layers accumulated in the basin, showing low magnetic anomalies. The late tectonic movement allowed the granite magma to intrude along the NNW and NW faults. These granite intrusions and the surrounding hydrothermal alteration often show high magnetic anomalies. In addition, the positive anomalies scattered in the basin may be caused by concealed granite. 5.2 The inversion results According to the results of WMSD, the field value variation characteristics at different depths were obtained, and the depth information was estimated. The average depth of the Moho surface is 55 km. Therefore, D4 is a regional field, and we have obtained the residual field of the crust by using the sum of the sum of 1st, 2nd, 3 rd, and 4th, as shown in Fig. 6 . Based on this information, the inversion of crustal structure density was calculated by using the ICDEXP algorithm. During the inversion calculation, for the satellite gravity data, the maximum depth was set as 50 km, the structure index was 3, the number of iterations was 20, and the upper and lower density limits were 1 and − 1. The three-dimensional structure result and vertical slices diagram are shown in Fig. 7 . The vertical slices AA’ is a profile located outside the basin. The densities of these slices are minor, and the negative data correspond to the Wahongshan fault. The vertical slices BB’ and CC’ are located near Tanggemu and Gonghe, located in the west and east basin, respectively. The negative density data is prominent. In profile BB’, the two negative densities correspond to the west Gonghe Basin and the Wahongshan fault. The vertical slice CC’ goes through the Gonghe Basin and near the town of Guinan. Two negative densities are located near the town of Gonghe and Guinan, which may be caused by deep partial melting. In the three-dimensional diagram and vertical section, the depth range of the density anomaly is clearly displayed, concentrated at a depth ranging between 15 ~ 35km. Cross section DD’ passes through the town of Guide. The negative densities are also very obvious in this profile. The burial depth is 15 km ~ 35 km, corresponding to the Xinjie fault and deep partial melting near the town of Guide. For display convenience, we intercepted the results of different depths (5, 10, 15, 20, 25, 30, 35 and 40 km), shown in Fig. 8 . The inversion results of different depths varied between methods. The sedimentary layers at shallow depths (up to 5 km) have little density fluctuation, consistent with the previous conclusion that the Cenozoic sedimentary thickness is greater than 5km (Sun et al., 2011 ). The low velocity bodies from near surface to a depth of about 5–10 km are Quaternary loose or weakly diagenetic strata, and there is no strong density anomaly in the shallow part. At 10 km and on, the high- and low-density anomalies are patently staged by stage. In addition to the shallow sedimentary layer with little density fluctuation, the resolution of satellite gravity cannot obtain shallow details. The distribution of density anomalies changes significantly from 15 km to 35 km. At depths greater than 35 km, the difference between high and low density anomalies begins to decrease. This shows that the density anomalies are mainly concentrated in the range of 15 ~ 35km. At a depth of 15km ~ 35km, the low-density anomaly is mainly distributed in the corresponding main fault zones, and the difference between high and low density anomalies is small. It is concentrated in the Wahongshan fault on the west side of the basin, the Xinjie Fault, and the Duohemao fault on the east side. The Xinjie fault corresponds well with known hot spots, so it can be inferred that the geothermal energy in this area is mainly concentrated in these low-density bodies and their vicinity. At the depths > 35km, the density distribution characteristic changes significantly. At a depth of 40km near the Xinjie fault zone, there are apparent low-density anomalies, and the low-density anomalies at other locations tend to disappear. It is speculated that the undercut depth of the Xinjie fault zone changes from south to north. This phenomenon can explain why the temperature increases successively from south to north. Generally speaking, the faults on the west side of the Gonghe-Guide Basin extend deep, mainly consisting of large faults extending into the lower crust. The eastern side of the fault is shallow. Therefore, the basin basement is deep in the west and shallow in the east. Similarly, based on the wavelet multi-scale decomposition method, Fig. 9 shows the residual magnetic anomaly, which is the magnetic material feature above the Curie point depth. During the inversion, for the aeromagnetic data, the maximum depth was set as 30km, the structure index was 3, the number of iterations was 20, and the upper and lower magnetization limits were 1 and − 1. The three-dimensional inversion results were obtained, as shown in Fig. 10 . To compare with gravity data, slices were taken at the same locations as Fig. 7 . The magnetic variation characteristic from shallow to deep is prominent. In the AA’ profile, magnetism is strong because of the intense tectonic activity. However, it is negative at the Wahongshan fault. Similarly, in the BB’ section, there is a significant negative magnetic anomaly on the west side of the Gonghe Basin with a depth range of 6 ~ 24km. The magnetism slowly dissipates with depth. In the CC’ section, a strong positive magnetic body in the basin’s center extends to 24km and below. This is a high-density and high magnetic anomaly body relative to the surrounding partial melting. It is speculated that this is a hidden granite body. No partial melting has occurred. Near the towns of Chaka, Tanggemu, Gonghe, and Xinjie, small-scale high magnetic anomalies at shallow depths and low magnetic negative anomalies at deeper depths, indicat shallow granite bodies and deep partial melting areas. This is consistent with the gravity results and the depth range. The same characteristics occur in section DD’; the characteristics of the Guide area are very similar to Gonghe, both of which are shallow granite bodies with deep weak or negative magnetic anomaly characteristics, reflecting deep partial melting. To facilitate analysis and display, slices at different depths were also made, as shown in Fig. 11 . At 3km and shallower depths, there are no significant magnetic anomalies, indicating no apparent magnetic body in the shallow part dominated by sedimentation. At depths less than 3km, there is weak magnetism and no apparent magnetic anomaly. It is speculated that sedimentary rocks mainly cause these characteristics. Furthermore, the resolution of the shallow data also can be a factor. In all the results at depths > 6km, there are scattered magnetic anomalies, mainly concentrated in the edge of the basin, faults, fold zones, and granite outcropping area in the western part of the basin. It is speculated that they are related to granite intrusions. The magnetic field inside the basin is consistent, and there is no obvious abnormal body. The magnetic bodies are mainly concentrated in the center of the basin. At a depth of 6 km, an east-west elliptical positive magnetic anomaly appears in east Gonghe County. This location also corresponds with a negative gravity anomaly, speculated as the Qiabuqia dry hot rock mass. It has been confirmed that the Qiabuqia thermal rock mass is about 21 km long in the east-west direction and 14 km wide in the north-south direction. The plane is nearly elliptical and develops stably within the depth of 21km (Zhang et al., 2020a ). There is a positive magnetic anomaly with a length of ~ 150km in the east-west direction in the granite area near Tanggemu. This location is also a negative gravity anomaly. The magnetic anomaly disappears at a depth of 24km. It is inferred that it is a granite intrusion extending to 24km. The difference from the Qiabuqia dry thermal rock mass is that the intrusion extends deeper. However, this granite mass has no surface exposure and no thermal insulation cover. The intrusive body extends deeply, and the concealed body can be found nearby as a geothermal exploration target. At a depth of 9 km, an NW bead-like positive magnetic anomaly is highlighted near the Wahongshan in the southwestern Wayuxiangka. There are dense EW and NW-W faults, numerous Permian and Triassic granites, and hot springs. There is also an apparent positive magnetic anomaly at a depth of 24km, indicating that this area is an excellent geothermal exploration area. In general, the gradient zone of magnetic anomaly from 15 km to 24 km is gradually flattened, indicating that the existence of underground high temperatures leads to the disappearance or weakening of magnetism. It is speculated that high temperatures have demagnetized the material. To further confirm and verify the correctness of the above interpretation, based on the inversion results, a 2D geologic model of CC’ profile is created to show the detailed tectonic framework (Fig. 12 ). In the basin, the experimental density and magnetic susceptibility of granites are 2.532–2.555 g/cm3 and 0.0456×10 –3 ~13.847×10 –3 SI separately (Zhao et al., 2020). The partial melting is widespread in in the upper-middle crust, where the density is set as 2.4–2.5 g/cm 3 . Correspondingly, middle and lower crust densities are set as 2.8 g/cm 3 and 3 g/cm 3 , respectively. To fit the magnetic data, we set the magnetic susceptibility of granite as 0.1×10 –3 SI for Ordovician granite and 0.05×10 –3 SI for Indosimian granite. The geologic model of CC’ profile corresponds well with our inversion results, in which the partial melting is located deeper, and the granites are shallow. 6 Discussion 6.1 Crustal partial melting Previous studies have shown that partial melting and fluids usually cause significant S-wave low-speed anomalies, and S-wave low-speed anomalies may also superimpose the effects of temperature increases and partial melting simultaneously (McKenzie et al., 2005 ). Furthermore, the MT results show that high conductivity regions can be interpreted as partial melting in the crust (Zhang et al., 2021 ; Tang et al., 2021 ). However, the characteristic of density and magnetism have not been explicated. In this study, we use the wavelet multi-scale field separation method and three-dimensional fast iteration imaging to implement the inversion calculation of large-scale data. We make full use of the advantages of gravity and magnetic field data in the study of regional geological structures. Effective residual anomalies were obtained based on the wavelet multi-scale field separation method, and subsurface material distribution characteristics were inverted. In the residual anomalies of the Gonghe-Guide Basin, a wide range of negative gravity and magnetic anomalies are displayed, which reflect the existence of low-density and magnetism geological bodies underlying the basin to a certain extent. The negative gravity anomalies correspond to the low resistivity and low velocity of previous results (Zhang et al., 2017 ). In addition, a temperature change is mainly manifested in the demagnetization of magnetic minerals and negative or weak magnetic anomalies. Especially when the rock temperature rises to the Curie temperature, rock magnetism disappears (Zeng et al., 2012 ). Based on this, we preliminarily believe that the negative or large consistent low magnetic field area in the Gonghe-Guide Basin may be related to the demagnetization of magnetic minerals caused by deep thermal factors. Based on low density and weak magnetism characteristics, it is reasonable to speculate partial melting regions in the deep crust. However, it is not enough to extrapolate solely from residual anomalies. In the study of large-scale crustal structural characteristics, the fast iteration imaging method (ICDEXP) reflects the advantages of calculation. The inversion results of gravity and magnetic data are consistent with the results of MT and seismic, and the existence of partial melting regions in the Gonghe-Guide Basin is further shown. From the inversion results, the density distribution is uniform from the near-surface to a depth of ~ 5 km, indicating Quaternary loose or weakly diagenetic stratum. Low-density geological bodies dominate the middle and lower crust from ~ 15 to 35 km, mainly distributed in the towns of Gonghe, Chaka, Tanggemu, Xinjie, Chaka, Xinjei, Wayuxiangka and Guide of the basin. In these areas, it also has certain low/weak magnetism. This characteristic can be inferred as a part of the partial melting regions. We determined the characteristics by using gravity and magnetic data inversion. Thus, we concluded that partial melting regions in the crust are generally characterized by low resistivity, low velocity, low density, and weak or no magnetism. 6.2 Hot dry rock target areas and their characteristics The idea of a partial melting area as a geothermal target needs further discussion. We found that density and magnetism correspond well at deep depths, with low density and low magnetism characteristics. However, as the main area of dry hot rock in Gonghe-Guide Basin, the shallow parts must have granite distributed throughout (Gao et al., 2020 ; Tang et al., 2021 ). Therefore, the shallow should have specific characteristics consisting of high magnetic anomalies. Therefore, we further analyze the target distribution of the dry hot rocks. The gravity and magnetic data show the partial melting regions of the entire basin and its surroundings, making it easier to delineate the existence of target areas. The results of the 3D inversion imaging prove this point. In the inversion results, the Gonghe-Guide basin shows a wide range of low-density and weak or low magnetic geological bodies, which suggests that there are high-temperature geological bodies or partial melting layers deep in the crust. We can conclude that the partial melting regions are the key geothermal prospecting target but not completely. Another key factor is the shallow signature. Because the granite also has low density, magnetic data must be used to distinguish geothermal targets. Based upon this study, the targets are the low/ negative density corresponding to low/negative magnetism in the deep and high/ positive magnetism in the shallow. According to the geological map of the study area, the strong magnetic anomaly is mainly due to the existence of intrusive granite rocks and granodiorite in the study area. Therefore, in the Gonghe-Guide Basin, the key geothermal prospecting target can be located near the towns of Guide, Gonghe, Xinjie, Chaka, Wayuxiangka, Tanggemu, Xinhai. In addition, the Wahongshan and Xinjie faults also can be ideal geothermal prospecting targets. 6.3 The geothermal source mechanism Determining the geothermal source mechanism is the main problem in geothermal exploration in the Gonghe-Guide Basin, and it is also a common problem in geothermal resource exploration in other similar basins. Different authors have proposed different mechanisms. There are three primary hypotheses: (1) Granite is the primary heat source (Zhang C. et al., 2018 ;Zhang et al., 2019 )༛(2) The geothermal is sourced from deeper sections, and transmits to the shallow part through the flower-shaped faults (Zhang S. et al., 2018 ; Gao et al., 2018 )༛(3) Geothermal is sourced from the deep mantle (Feng et al., 2018 ). These three views have certain rationality but also have shortcomings. The geothermal mechanisms are uncertain and have yet to be proven. The mechanisms of conduction and heat accumulation are also unclear. Overall, these disputes affect the understanding of dry hot rocks themselves and restrict the evaluation and efficient development and utilization of geothermal resources. The hot springs in the region are primarily concentrated along faults. Hot springs with higher temperatures are not directly formed in the basin due to the influence of sedimentary layers. This shows that the heat source in the study area mainly comes from the crust and at depth. According to the inversion results in this paper, several large faults, such as Duomaohe, Xinjie, and Qinghainanshan, extend deep into the crust. These faults also have high-temperature large hot springs, suggesting that large-scale faults play a vital role in heat conduction and supply. The Gonghe-Guide Basin is a faulted basin with a thick sedimentary cover and fault zones controlled by the stress field of the Tibet Plateau. Due to the existence of large-scale high-temperature bodies and the negative topography of the basin, the interior of the basin shows negative density and weak magnetism. Many fault zones around the basin allow high-temperature magma to intrude along the fault. The high-temperature alteration of the intrusive bodies and surrounding rocks makes prominent positive and negative alternating magnetic anomaly bands near the fault zone. The geothermal springs in the Gonghe-Guide Basin are mainly exposed near the fault zones on the east and west sides of the basin. Due to the numerous granite intrusions near the fault zone on the southwest side of the basin, magnetic anomalies controlled by structures are distributed in strips. It is speculated that the geothermal source here may be dominated by a large amount of deep molten materials. In addition, there has been no volcanic and magmatic activity in Gonghe Basin and its surrounding orogenic belt since the Cenozoic. The average heat generation rate of radioactive elements in drill core is 4.43 µW/m 3 (Zhang et al., 2020a ), which slightly higher than the global average value (3.09 µW/m 3 ) of radioactive element heat generation rate of Mesozoic Cenozoic granite (Artemieva et al., 2017 ). However, it is much lower than the basement granite in the area where the dry hot rock is produced in the Cooper Basin in Australia, with up to 7 ~ 10 µW/m 3 of radioactive element heat generation rate (McLaren et al., 2003 ; Beardsmore, 2004 ). Therefore, it is difficult for radioactive element decay heat generation to constitute the main heat source of Gonghe-Guide Basin. The residual heat of the granite magma and the heat generated by the decay of radioactive elements are probably not the heat source of the hot dry rock in the Gonghe-Guide Basin. In summary, as shown in Fig. 13 , we suggest that the essential geothermal source comes from the mantle caused by substantial tectonic activities since the early Cenozoic (Graddock et al., 2014; Gao et al. 2020 ), causing partial melting in the crustal, and the heat flows from deep to shallow along the faults. The Quaternary sediments covering the surface of the Gonghe Basin can serve as the geothermal system’s caprock. The heat source structure of the Gonghe-Guide Basin is closely related to the geological structure in the crust. 7 Conclusions The crustal structure of the entire Gonghe-Guide Basin was obtained based on the satellite gravity and aeromagnetic data, using the wavelet multi-scale decomposition field separation method and the iterative fast imaging inversion method, providing evidence for the existence of underground partial melting regions. The results show that the location of deep low density and low magnetic anomalies corresponds well to the partial melting regions and corresponds to the results of previous MT and seismic methods. In addition, the inversion results in this paper show that the regions near the town of Guide, Gonghe, Xinjie, Chaka, Wayuxiangka, Tanggemu, Xinhai, and Xinjie have abnormal characteristics of low density, shallow high magnetism, and deep low magnetism. These areas have good geothermal target potential, consistent with the existing geological and borehole data. Therefore, in the inversion of gravity and magnetic anomalies, regions with similar characteristics can be used as targets of geothermal resources. Combined with other geologic data, we suggest that the heat source mechanism is heating from deep to shallow due to mantle material upwelling and early Cenozoic Indosinian tectonic movement. The most important heat source comes from the mantle and tectonic activities, causing partial melting in the crust. The heat continues to flow along the faults into shallow strata, heating the surrounding rocks to adequate temperatures for geothermal exploration. Declarations ACKNOWLEDGMENTS Wenna Zhou would like to thank Prof. Shuang Liu of China University of Geosciences (Wuhan) for providing their ICDEXP code and permission to use it. This research was partly supported by the National Natural Science Foundation (42004068), the Second Tibetan Plateau Scientific Expedition and Research Program (Grant No. 2019QZKK0704), the Fundamental Research Funds for the Central Universities (Grant No. lzujbky-2021-sp65), the Science and Technology Plan of Gansu Province (20JR5RA251) and the Science and Technology Innovation 2025 Major project of Ningbo (2020Z073). DATA AVAILABILITY The gravity data can be download from ICGEM (http://icgem.gfz-potsdam.de/home). The aeromagnetic data associated with this research are confidential and cannot be released. AUTHOR CONTRIBUTION STATEMENT: Wenna Zhou: Methodology, Software, Formal analysis, Visualization, Writing - Original Draft, Review & Editing, Funding acquisition, Supervision. Qiang Li: Formal analysis, Visualization, Writing - Original Draft, Review & Editing, Funding acquisition. Dailei Zhang: Formal analysis, Review & Editing, Funding acquisition. 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Tectonics 29, 1–14. https://doi.org/10.1029/2008TC002428 Additional Declarations No competing interests reported. Cite Share Download PDF Status: Published Journal Publication published 01 Jun, 2023 Read the published version in Pure and Applied Geophysics → Version 1 posted Editor assigned by journal 09 Nov, 2022 Submission checks completed at journal 08 Nov, 2022 First submitted to journal 07 Nov, 2022 You are reading this latest preprint version Research Square lets you share your work early, gain feedback from the community, and start making changes to your manuscript prior to peer review in a journal. As a division of Research Square Company, we’re committed to making research communication faster, fairer, and more useful. We do this by developing innovative software and high quality services for the global research community. Our growing team is made up of researchers and industry professionals working together to solve the most critical problems facing scientific publishing. Also discoverable on Platform About Our Team In Review Editorial Policies Advisory Board Help Center Resources Author Services Accessibility API Access RSS feed Manage Cookie Preferences © Research Square 2026 | ISSN 2693-5015 (online) Privacy Policy Terms of Service Do Not Sell My Personal Information {"props":{"pageProps":{"initialData":{"identity":"rs-2249266","acceptedTermsAndConditions":true,"allowDirectSubmit":false,"archivedVersions":[],"articleType":"Research Article","associatedPublications":[],"authors":[{"id":150607410,"identity":"3c551e41-3c43-41cb-ae88-cd5fd079aec2","order_by":0,"name":"Wenna Zhou","email":"data:image/png;base64,iVBORw0KGgoAAAANSUhEUgAAAZAAAAAyAQMAAABI0h/eAAAABlBMVEX///8AAABVwtN+AAAACXBIWXMAAA7EAAAOxAGVKw4bAAAAv0lEQVRIiWNgGAWjYPCCAwwM7I2NDz+QpoXncLOxBGlaJNLbBHiIUWtwvPfYgx9/7sgZ3HzYxiDBYCen20BIy5lz6YY9PM+MDW4ntj0oYEg2NjtAQIvZjRwzCR6Jw4kbbie2G0gwHEjcRlDL/Tdmkn8MgFpuHmyT4CFKyw0eM2meBKCWG4xEarE/k2MmLXPgsLHkmURgIBsQ4RfJ9jNmkm/+HJbjO3784cMPFXZyBLWgAQPSlI+CUTAKRsEowAEADdVG66iCpZUAAAAASUVORK5CYII=","orcid":"","institution":"Lanzhou University","correspondingAuthor":true,"submittingAuthor":false,"prefix":"","firstName":"Wenna","middleName":"","lastName":"Zhou","suffix":""},{"id":150607411,"identity":"dec83ad4-bd59-40c3-ab5f-9df779b02c66","order_by":1,"name":"Qiang Li","email":"","orcid":"","institution":"Lanzhou University","correspondingAuthor":false,"submittingAuthor":false,"prefix":"","firstName":"Qiang","middleName":"","lastName":"Li","suffix":""},{"id":150607412,"identity":"7aaeb18d-ddd4-4783-bb04-a79b68f38cb1","order_by":2,"name":"Dailei Zhang","email":"","orcid":"","institution":"Geothermal and Hot Dry Rock Exploration and Development Technology Innovation Center of the Ministry of Natural Resources","correspondingAuthor":false,"submittingAuthor":false,"prefix":"","firstName":"Dailei","middleName":"","lastName":"Zhang","suffix":""},{"id":150607413,"identity":"73f612f9-7ac3-4c97-998c-fbdbd7a04264","order_by":3,"name":"Hai Tang","email":"","orcid":"","institution":"Lanzhou University","correspondingAuthor":false,"submittingAuthor":false,"prefix":"","firstName":"Hai","middleName":"","lastName":"Tang","suffix":""}],"badges":[],"createdAt":"2022-11-08 04:59:10","currentVersionCode":1,"declarations":"","doi":"10.21203/rs.3.rs-2249266/v1","doiUrl":"https://doi.org/10.21203/rs.3.rs-2249266/v1","draftVersion":[],"editorialEvents":[{"content":"https://doi.org/10.1007/s00024-023-03290-2","type":"published","date":"2023-06-01T21:03:55+00:00"}],"editorialNote":"","failedWorkflow":false,"files":[{"id":29029776,"identity":"da082b74-82ab-486e-9dfc-08e68c916be6","added_by":"auto","created_at":"2022-11-14 15:04:25","extension":"jpg","order_by":1,"title":"Figure 1","display":"","copyAsset":false,"role":"figure","size":3148897,"visible":true,"origin":"","legend":"\u003cp\u003eGeologic map of Gonghe-Guide Basin after Fang et al. (2005) and Zhang et al. (2006). Red solid lines represent faults, where LJSF: Lajishan fault, QHNF: Qinghainan fault, QHNSF: Qinghainanshan fault, DHMF: Duohemao fault, XJF: Xinjie fault, WGBF: Wayuxiangka-Guinan Buried fault, WHSF: Wahongshan fault, GNSF:Guinan south fault, KLF: Kunlun fault. The dashed black lines are the basin boundaries.\u003c/p\u003e","description":"","filename":"figure1.jpg","url":"https://assets-eu.researchsquare.com/files/rs-2249266/v1/7d2b8153b338f773dc350a23.jpg"},{"id":29030127,"identity":"2efa3ce8-3abe-4b26-9571-6320366e7bcc","added_by":"auto","created_at":"2022-11-14 15:12:25","extension":"jpg","order_by":2,"title":"Figure 2","display":"","copyAsset":false,"role":"figure","size":1932508,"visible":true,"origin":"","legend":"\u003cp\u003e\u003cstrong\u003e(\u003c/strong\u003ea). The topographic data of Gonghe-Guide Basin, (b). The Satellite Bouguer gravity anomaly. Graphical indications as described in Fig. 1.\u003c/p\u003e","description":"","filename":"figure2.jpg","url":"https://assets-eu.researchsquare.com/files/rs-2249266/v1/10c31f72fa27047d94cc0ba3.jpg"},{"id":29029774,"identity":"800fd963-d786-4671-af55-41da8f11f8a7","added_by":"auto","created_at":"2022-11-14 15:04:25","extension":"jpg","order_by":3,"title":"Figure 3","display":"","copyAsset":false,"role":"figure","size":4055466,"visible":true,"origin":"","legend":"\u003cp\u003e\u003cstrong\u003e(\u003c/strong\u003ea) The aeromagnetic anomaly of Gonghe-Guide Basin, (b) the reduction to the pole aeromagnetic anomaly of the Gonghe-Guide Basin. Graphical indications as described in Fig. 1.\u003c/p\u003e","description":"","filename":"figure3.jpg","url":"https://assets-eu.researchsquare.com/files/rs-2249266/v1/57f10f0c2a5cd95a17c6df9f.jpg"},{"id":29029779,"identity":"7456ba5a-5a15-402b-b5b1-71ed6fa147bc","added_by":"auto","created_at":"2022-11-14 15:04:25","extension":"jpg","order_by":4,"title":"Figure 4","display":"","copyAsset":false,"role":"figure","size":3927132,"visible":true,"origin":"","legend":"\u003cp\u003eThe gravity results of Wavelet multi-scale decomposition (WMSD) method. (a). the detail features of 1\u003csup\u003est\u003c/sup\u003e+2\u003csup\u003end\u003c/sup\u003e of wavelet decomposition, (b) the detail features of 3\u003csup\u003erd\u003c/sup\u003e of wavelet decomposition, (c) the detail features 4\u003csup\u003eth\u003c/sup\u003e wavelet decomposition (d) the regional component of 4\u003csup\u003eth\u003c/sup\u003e terms of wavelet decomposition. Graphical indications as described in Fig. 1.\u003c/p\u003e\n\u003cp\u003e\u0026nbsp;\u003c/p\u003e","description":"","filename":"figure4.jpg","url":"https://assets-eu.researchsquare.com/files/rs-2249266/v1/e475093264266d77260ab85c.jpg"},{"id":29030128,"identity":"e14fda6c-76cf-43d7-ac30-7a6610cce6b3","added_by":"auto","created_at":"2022-11-14 15:12:25","extension":"jpg","order_by":5,"title":"Figure 5","display":"","copyAsset":false,"role":"figure","size":3924520,"visible":true,"origin":"","legend":"\u003cp\u003eThe magnetic results of Wavelet multi-scale decomposition (WMSD) method. (a). the detail features of 1\u003csup\u003est\u003c/sup\u003e+2\u003csup\u003end\u003c/sup\u003e of wavelet decomposition, (b) the detail features of 3\u003csup\u003erd\u003c/sup\u003e of wavelet decomposition, (c) the detail features 4\u003csup\u003eth\u003c/sup\u003e wavelet decomposition, (d) the regional component of 4\u003csup\u003eth\u003c/sup\u003e terms of wavelet decomposition. Graphical indications as described in Fig. 1.\u003c/p\u003e","description":"","filename":"figure5.jpg","url":"https://assets-eu.researchsquare.com/files/rs-2249266/v1/b5190dffdaa619893a5f938b.jpg"},{"id":29031824,"identity":"60d1562b-8512-47a5-aff2-ba66ce84d010","added_by":"auto","created_at":"2022-11-14 15:20:25","extension":"jpg","order_by":6,"title":"Figure 6","display":"","copyAsset":false,"role":"figure","size":1189488,"visible":true,"origin":"","legend":"\u003cp\u003eThe residual gravity anomaly of Gonghe-Guide Basin obtained by using WMSD method. Graphical indications as described in Fig. 1.\u003c/p\u003e","description":"","filename":"figure6.jpg","url":"https://assets-eu.researchsquare.com/files/rs-2249266/v1/54e909a2c98398669dc625fa.jpg"},{"id":29030130,"identity":"1ee3eb51-b029-4995-87a4-539d3f9f969a","added_by":"auto","created_at":"2022-11-14 15:12:25","extension":"jpg","order_by":7,"title":"Figure 7","display":"","copyAsset":false,"role":"figure","size":1544852,"visible":true,"origin":"","legend":"\u003cp\u003eThe inversion results of residual gravity. (a) the 3D inversion result, (b) the vertical slices result from 3D inversion result.\u003c/p\u003e","description":"","filename":"figure7.jpg","url":"https://assets-eu.researchsquare.com/files/rs-2249266/v1/0183d948cc69bdfdec2fc70d.jpg"},{"id":29029785,"identity":"0f9535fb-3f43-4e4b-9fbf-5a1f0ed87f44","added_by":"auto","created_at":"2022-11-14 15:04:25","extension":"jpg","order_by":8,"title":"Figure 8","display":"","copyAsset":false,"role":"figure","size":7344759,"visible":true,"origin":"","legend":"\u003cp\u003eThe gravity inversion results at different depths, (a)-(h) is the results of 5 km, 10 km, 15km , 20 km, 25km, 30km, 35km and 40 km in turns. Graphical indications as described in Fig. 1.\u003c/p\u003e","description":"","filename":"figure8.jpg","url":"https://assets-eu.researchsquare.com/files/rs-2249266/v1/70447575ff1336c015f6454d.jpg"},{"id":29030131,"identity":"94c5f9c7-c659-4360-919f-59db5f3f36e1","added_by":"auto","created_at":"2022-11-14 15:12:25","extension":"jpg","order_by":9,"title":"Figure 9","display":"","copyAsset":false,"role":"figure","size":1247833,"visible":true,"origin":"","legend":"\u003cp\u003eThe residual magnetic anomaly of Gonghe-Guide Basin obtained by using the WMSD method. Graphical indications as described in Fig. 1.\u003c/p\u003e","description":"","filename":"figure9.jpg","url":"https://assets-eu.researchsquare.com/files/rs-2249266/v1/d52f676a8f9d3f8d40092016.jpg"},{"id":29029782,"identity":"3dc69a77-3e8e-4862-8b1a-10cfde46082b","added_by":"auto","created_at":"2022-11-14 15:04:25","extension":"jpg","order_by":10,"title":"Figure 10","display":"","copyAsset":false,"role":"figure","size":1591695,"visible":true,"origin":"","legend":"\u003cp\u003eThe inversion results of residual magnetic data. (a) the 3D inversion result, (b) the vertical slices result from 3D inversion result.\u003c/p\u003e","description":"","filename":"figure10.jpg","url":"https://assets-eu.researchsquare.com/files/rs-2249266/v1/24635dfb007d605d4c2823ca.jpg"},{"id":29029786,"identity":"943b247a-786d-4067-81cb-683adbd256da","added_by":"auto","created_at":"2022-11-14 15:04:25","extension":"jpg","order_by":11,"title":"Figure 11","display":"","copyAsset":false,"role":"figure","size":8415991,"visible":true,"origin":"","legend":"\u003cp\u003eThe inversion results of different depths, (a)~(h) is the result of 3, 6, 9, 12, 15, 18, 21and 24 km in turns. Graphical indications as described in Fig. 1.\u003c/p\u003e","description":"","filename":"figure11.jpg","url":"https://assets-eu.researchsquare.com/files/rs-2249266/v1/e9fb579cd0b59f3eef68c6eb.jpg"},{"id":29030133,"identity":"cf32ffa1-c199-42e8-a511-c2098897aa3a","added_by":"auto","created_at":"2022-11-14 15:12:25","extension":"jpg","order_by":12,"title":"Figure 12","display":"","copyAsset":false,"role":"figure","size":1313778,"visible":true,"origin":"","legend":"\u003cp\u003ea) observed magnetic values and predicted magnetic from CC’, b) observed gravity values and predicted gravity data from the profile, c) the model of density and magnetic susceptibility distribution limited to the upper 50 km.\u003c/p\u003e","description":"","filename":"figure12.jpg","url":"https://assets-eu.researchsquare.com/files/rs-2249266/v1/3cff5b2bcc55567394977b5d.jpg"},{"id":29030132,"identity":"4a973b82-3316-422f-a408-eaab7a7e85b1","added_by":"auto","created_at":"2022-11-14 15:12:25","extension":"jpg","order_by":13,"title":"Figure 13","display":"","copyAsset":false,"role":"figure","size":2697730,"visible":true,"origin":"","legend":"\u003cp\u003eCartoon sketch showing the thrust belt development, partial melting and Granite, the geothermal mechanism beneath Gonghe-Guide Basin.\u003c/p\u003e","description":"","filename":"figure13.jpg","url":"https://assets-eu.researchsquare.com/files/rs-2249266/v1/0c047e23b688960ce69d4952.jpg"},{"id":44732028,"identity":"55c41e4d-40d7-4f7e-a792-58228c6a9a0a","added_by":"auto","created_at":"2023-10-16 21:50:41","extension":"pdf","order_by":0,"title":"","display":"","copyAsset":false,"role":"manuscript-pdf","size":3064725,"visible":true,"origin":"","legend":"","description":"","filename":"manuscript.pdf","url":"https://assets-eu.researchsquare.com/files/rs-2249266/v1/c1204a33-637d-4634-8313-61759d9c303c.pdf"}],"financialInterests":"No competing interests reported.","formattedTitle":"Crustal structure and geothermal mechanism of Gonghe-Guide Basin based on EIGEN-6C4 satellite gravity and aeromagnetic data","fulltext":[{"header":"1. Introduction","content":"\u003cp\u003eThe Gonghe-Guide Basin is a structurally complex basin located at the northeastern edge of the Tibetan Plateau. It is currently one of the main targets for geothermal research and exploitation in China (Zhao et al., \u003cspan citationid=\"CR59\" class=\"CitationRef\"\u003e2009\u003c/span\u003e; Xu et al., \u003cspan citationid=\"CR41\" class=\"CitationRef\"\u003e2018a\u003c/span\u003e). It is also considered one of the most crucial regions for studying the uplift mechanisms of the Tibetan Plateau (Clark and Royden, \u003cspan citationid=\"CR5\" class=\"CitationRef\"\u003e2000\u003c/span\u003e; Zhang et al., \u003cspan citationid=\"CR54\" class=\"CitationRef\"\u003e2011\u003c/span\u003e; Gao et al., \u003cspan citationid=\"CR13\" class=\"CitationRef\"\u003e2020\u003c/span\u003e). In particular, with the increasing demand for clean energy, detecting geothermal energy requires new exploration techniques for widespread implementation (Li et al., \u003cspan citationid=\"CR17\" class=\"CitationRef\"\u003e2015\u003c/span\u003e; Wang et al., \u003cspan citationid=\"CR36\" class=\"CitationRef\"\u003e2018\u003c/span\u003e; Wang et al., \u003cspan citationid=\"CR36\" class=\"CitationRef\"\u003e2018\u003c/span\u003e). A better understanding of the tectonic activity, geologic structures, and distribution characteristics of deep materials will also allow for increased geothermal detection and implementation. Furthermore, as an essential foundation for geothermal energy exploration in China (Wang et al., \u003cspan citationid=\"CR37\" class=\"CitationRef\"\u003e2021\u003c/span\u003e), the research on the geological structure and geothermal heat source mechanism in the Gonghe-Guide Basin can provide a primary reference for research on geothermal resources in other areas that have similar geological structure.\u003c/p\u003e \u003cp\u003eThe Gonghe-Guide Basin is a faulted basin surrounded by fault-fold uplift mountains. The foothills of the Qinghainanshan Fault border it to the north, the Animaqing Suture Zone (an extension from Kunlun Fault (KLF)) to the south, the Wahongshan Fault to the west, and the Duohemao Fault to the east (Zheng et al., \u003cspan citationid=\"CR60\" class=\"CitationRef\"\u003e2010\u003c/span\u003e) (Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003e and Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003ea). The main faults are extensive NW trending sinistral strike-slip thrust faults (Fang et al., \u003cspan citationid=\"CR8\" class=\"CitationRef\"\u003e2005\u003c/span\u003e; Zhang et al., \u003cspan citationid=\"CR51\" class=\"CitationRef\"\u003e2020a\u003c/span\u003e). Hydrothermal and hot dry rocks (HDRs) have been found throughout the Gonghe-Guide area (Gao et al., \u003cspan citationid=\"CR14\" class=\"CitationRef\"\u003e2018\u003c/span\u003e; Zhang C. et al., \u003cspan citationid=\"CR44\" class=\"CitationRef\"\u003e2018\u003c/span\u003e). HDRs exceeding 200\u0026deg;C have been recently detected in the GR1 borehole (the red sign in Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003e) with temperatures up to 236\u0026deg;C at a bottom depth of 3705 m, a first in China (Zhang S. et al., \u003cspan citationid=\"CR52\" class=\"CitationRef\"\u003e2018\u003c/span\u003e). The Gonghe-Guide Basin is now considered to have great potential for geothermal energy exploration and development.\u003c/p\u003e \u003cp\u003ePrevious studies have obtained numerous geophysical surveys and extensive subsurface data to delineate crustal structures across the Gonghe-Guide Basin. Geophysical surveys have been conducted, including magnetotelluric (MT), seismic, gravity, and magnetic methods (Li et al., \u003cspan citationid=\"CR18\" class=\"CitationRef\"\u003e2018\u003c/span\u003e; Gao et al., \u003cspan citationid=\"CR14\" class=\"CitationRef\"\u003e2018\u003c/span\u003e; Gao et al., \u003cspan citationid=\"CR13\" class=\"CitationRef\"\u003e2020\u003c/span\u003e; Zhao et al., \u003cspan citationid=\"CR57\" class=\"CitationRef\"\u003e2020a\u003c/span\u003e). Three-dimensional MT imaging indicated a conductive layer in the middle-upper crustal in the southeastern Gonghe-Guide Basin and a possible magma chamber near Gonghe town (Gao et al., \u003cspan citationid=\"CR14\" class=\"CitationRef\"\u003e2018\u003c/span\u003e). Zhang et al. (\u003cspan citationid=\"CR48\" class=\"CitationRef\"\u003e2020b\u003c/span\u003e) and Tang et al. (\u003cspan citationid=\"CR33\" class=\"CitationRef\"\u003e2021\u003c/span\u003e) also found partial melting at depths of 15\u0026ndash;35 km in the Gonghe-Guide Basin using MT data. In addition, seismic results also show partial melting with low-velocity zones at depths of 1\u0026ndash;10 km, 25\u0026ndash;40 km, and approximately 60 km in the basin (Zhang et al., \u003cspan citationid=\"CR53\" class=\"CitationRef\"\u003e2019\u003c/span\u003e). With multiple geophysical datasets, Zhao et al. (\u003cspan citationid=\"CR56\" class=\"CitationRef\"\u003e2020b\u003c/span\u003e) proposed a conceptual geothermal model for the Gonghe Basin with MT, seismic, MD, and CPD evidence. Zhao et al. (\u003cspan citationid=\"CR57\" class=\"CitationRef\"\u003e2020a\u003c/span\u003e) used 2D manual inversion and 3D cross-gradient joint inversion of the gravity and magnetic data collected from Qiabuqia, and indicated that this area is overlain by sedimentary layers approximately 1000\u0026ndash;1500 m in thickness. Wang et al. (\u003cspan citationid=\"CR37\" class=\"CitationRef\"\u003e2021\u003c/span\u003e) inversed Moho depth and Curie point depth in and around the basin using gravity and magnetic data using an improved Parker-Oldenburg algorithm. Then, they established different thermal models and concluded that the high heat flow in the Gonghe-Guide Basin coacted with radiogenic heat.\u003c/p\u003e \u003cp\u003eIn summary, studies have primarily focused on seismic and MT profiles and obtained the characteristics of local areas (Gao et al., \u003cspan citationid=\"CR14\" class=\"CitationRef\"\u003e2018\u003c/span\u003e; Zhao et al., \u003cspan citationid=\"CR56\" class=\"CitationRef\"\u003e2020b\u003c/span\u003e). Inversion interpretation of gravity data and magnetic data have also been performed, emphasizing the inversion of the interface, which reflects the fluctuation characteristics of the Moho surface and Curie point depth (Zhao et al., \u003cspan citationid=\"CR58\" class=\"CitationRef\"\u003e2019\u003c/span\u003e; Zhao et al., \u003cspan citationid=\"CR56\" class=\"CitationRef\"\u003e2020b\u003c/span\u003e; Wang e al., 2021). However, subject to the accuracy and resolution of previous gravity and magnetic data, no complete three-dimensional crust structure has been established despite the limitations of the data processing methods. Therefore, it is difficult to research the entire basin's three-dimensional distribution characteristics of geological bodies. Furthermore, there is a lack of comprehensive research on a large-scale and overall lithologic distribution of the entire basin, from shallow to deep. Therefore, there are many discrepancies on the geothermal mechanisms across the entire Gonghe-Guide Basin.\u003c/p\u003e \u003cp\u003eTo obtain the crust structure and further describe the geothermal mechanism of the Gonghe-Guide Basin, we present a detailed study of the Gonghe-Guide Basin based on EIGEN-6C4 satellite gravity and aeromagnetic data using the wavelet multi-scale decomposition (WMSD) method and iterative compact depth from extreme points imaging (ICDXEP) method (a fast inversion method can process the large data volume). First, we obtained the residual and regional fields using the WMSD method. Then, the lithologic distribution and crustal structure of the whole basin were inversed using the ICDEXP method with little constraint. In addition, to verify and reflect the accuracy of inversion, a 2D geologic model from typical area is created to show the detailed tectonic. Finally, target areas of geothermal resources are proposed, including their geophysical characteristics for detection. And then geological conceptual model was used to determine the relationships between the deep crustal structure and geothermal source.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e"},{"header":"2. Geologic Setting","content":"\u003cp\u003eThe Gonghe-Guide Basin is located north of the KLF and between the Qaidam Basin and Qinling Orogen (Zhang et al., \u003cspan citationid=\"CR47\" class=\"CitationRef\"\u003e2006\u003c/span\u003e). Tectonically, the Gonghe-Guide Basin is a Cenozoic intermontane basin controlled by the KLF and Altyn Tagh Fault (ATF) (Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003e; Fang et al., \u003cspan citationid=\"CR8\" class=\"CitationRef\"\u003e2005\u003c/span\u003e). To the north, it is bordered by the foothills of the Qinghainanshan (QHNS) Fault, to the south by the Animaqing Suture Zone (extension from KLF), to the west by the Wahongshan Fault, and to the east by the Duohemao fault (Zhang et al.,2006). Between these first-order strike-slip faults, there are numerous secondary thrust faults, including the faults along Qaidam Basin, Qinghainanshan (QHNS), and Gonghenanshan (GHNS), which contributed to the shortening and uplift of the mountains (Zhang et al., \u003cspan citationid=\"CR51\" class=\"CitationRef\"\u003e2020a\u003c/span\u003e). Within the basin, the QHNS and GHNS are two prominent narrow ranges and thus comprise the range and basin landscapes in the interior of the northeastern Tibetan Plateau (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003ea; Craddock et al., \u003cspan citationid=\"CR6\" class=\"CitationRef\"\u003e2014\u003c/span\u003e; Zhang et al., \u003cspan citationid=\"CR46\" class=\"CitationRef\"\u003e2012\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eThe geologic map (Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003e) shows that surface is covered by the Quaternary system interior of the basin and its peripheral sporadic Neogene sediments (Sun et al., \u003cspan citationid=\"CR32\" class=\"CitationRef\"\u003e2011\u003c/span\u003e). The Neoarchean-Early Proterozoic Jinshuikou Group is exposed in the southwest orogenic belt around the basin. The Early Proterozoic Daken-Daban Group is exposed in the northwest. The early Middle Triassic Longwuhe Group is exposed in the south, north, and east of the basin margin orogenic belt. Indosinian granites are primarily exposed in the west, north, and east of the orogenic belt around the basin. Multiple intrusions of different types of magma in the Indosinian period formed a compound granite batholith, which constitutes the main body of the basement of the Gonghe-Guide basin (Zhang et al., \u003cspan citationid=\"CR50\" class=\"CitationRef\"\u003e2021\u003c/span\u003e). In the post-collision period, lithosphere delamination occurred due to crustal thickening, and Late Triassic hot spring rocks developed on the east and west sides of the southern basin (Shi et al., \u003cspan citationid=\"CR30\" class=\"CitationRef\"\u003e2018\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eMany hydrothermal springs have been discovered along the NE\u0026ndash;SW, and NS extending faults (Liu et al. \u003cspan citationid=\"CR20\" class=\"CitationRef\"\u003e2017\u003c/span\u003e), and the hot water comes from the deeper part of the basin (~\u0026thinsp;1000 m) (Fang et al., \u003cspan citationid=\"CR7\" class=\"CitationRef\"\u003e2009\u003c/span\u003e). Thermal survey results also reveal excellent geothermal conditions in this basin due to the geothermal gradient and terrestrial heat flow. Based on geophysical detection results, there is a conductive layer in the middle-upper crustal in the southeastern Gonghe Basin and a possible magma chamber near Gonghe town (Gao et al., \u003cspan citationid=\"CR14\" class=\"CitationRef\"\u003e2018\u003c/span\u003e). There is a partial melting body at depths of 15\u0026ndash;35 km in the western Gonghe Basin (Zhang et al., \u003cspan citationid=\"CR48\" class=\"CitationRef\"\u003e2020b\u003c/span\u003e). The results have also been verified by seismic results (Zhang et al., \u003cspan citationid=\"CR53\" class=\"CitationRef\"\u003e2019\u003c/span\u003e). However, seismic and MT methods mainly indicated profile results (2D cross section). It is difficult to display the geologic distribution characteristics of the entire basin. Therefore, gravity and magnetic data are used in this paper to further explore on the relationship between the geothermal heat source mechanism and crustal structure.\u003c/p\u003e"},{"header":"3. Data And Materials","content":"\u003cdiv id=\"Sec4\" class=\"Section2\"\u003e \u003ch2\u003e3.1 EIGEN-6C4 satellite gravity data\u003c/h2\u003e \u003cp\u003eSatellite gravity observation technology has high coverage, precision and resolution, which significantly compensates for the deficiency of ground gravity measurements. To effectively analyze the density structure of the Gonghe-Guide Basin, the EIGEN-6C4 satellite gravity data was used in this study. EIGEN-6C4 is a static global combined gravity field model up to degree and order 2190 (Foerste et al., \u003cspan citationid=\"CR12\" class=\"CitationRef\"\u003e2014\u003c/span\u003e). The gravity model is high resolution (9 km) and precision (2.73 mGal). Figure\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003ea is the topographic data, and Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003eb shows the Bouguer gravity anomaly with a grid spacing of 5 km of the Gonghe-Guide area. The Bouguer gravity anomaly (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003eb) ranges from \u0026minus;\u0026thinsp;520 to -320 mGal in the study area. The characteristic of gravity anomaly agrees well with the topographic data (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003ea). The low values in the southwest are the Kunlun Mountains, with high elevations and, therefore, a thick crust. The gravity value increases from the southwest part to the northeast. The high values in the northwest are the Xining Basin. In the Gonghe-Guide Basin, the gravity anomaly has relatively few dramatic changes. The gravity anomalies and fault structure zones also correspond well.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec5\" class=\"Section2\"\u003e \u003ch2\u003e3.2 Aeromagnetic data\u003c/h2\u003e \u003cp\u003eMagnetic anomaly maps provide insight into the subsurface structure and composition of the Earth\u0026rsquo;s crust. The aeromagnetic anomaly grid used in our study area was derived from China Geological Survey (CGS). The aeromagnetic grid has a 2 km resolution grid of the magnetic intensity anomaly. The total field magnetic anomalies in the study area range between \u0026minus;\u0026thinsp;250 nT and 360 nT (Fig.\u0026nbsp;\u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e3\u003c/span\u003ea). The magnetic anomalies in the Gonghe-Guide Basin are generally weak and evenly distributed. The prominent high magnetic anomalies are distributed in the structural belt around the basin. The dipole nature of magnetic anomalies makes them more challenging to interpret in terms of geological structure. Thus, an initial process of removing/minimizing the inclination effect is transforming the TMI map into the Differential Reduction to the Pole (DRTP) map (Arkani-Hamed, \u003cspan citationid=\"CR1\" class=\"CitationRef\"\u003e2007\u003c/span\u003e). This DRTP transform reduces the magnetic anomalies to the pole and corrects for variation in inclination and declination over the study area, assuming that all magnetization is induced. The mean inclination and declination values for the center of the study area (Fig.\u0026nbsp;\u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e3\u003c/span\u003ea) are 55.37\u0026deg; and \u0026minus;\u0026thinsp;1.29\u0026deg;, respectively.\u003c/p\u003e \u003cp\u003eA comparative analysis of the aeromagnetic results can delineate the boundaries of the basin. Some differences exist between the RTP magnetic and gravity anomalies. More detailed aspects of their differences are discussed in the discussion of gravity and magnetic data inversion results.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003c/div\u003e"},{"header":"4. Methodology","content":"\u003cp\u003eThis paper carries out multi-scale data processing and analysis of satellite gravity and aeromagnetic data to obtain more precise geological structure interpretation results.\u003c/p\u003e \u003cdiv id=\"Sec7\" class=\"Section2\"\u003e \u003ch2\u003e4.1 Wavelet multi-scale decomposition method for potential field data separation\u003c/h2\u003e \u003cp\u003eThe observed potential field data are the sum of gravity and magnetic effects at various depths in the subsurface half-space. The target anomalies must first be separated from the observed gravity and magnetic anomalies to study a specific geological problem using gravity and magnetic data. A variety of methods are proposed for separating gravity anomalies, such as upward continuation (Jacobsen, 1987), matched filtering (Spector and Grant, \u003cspan citationid=\"CR31\" class=\"CitationRef\"\u003e1970\u003c/span\u003e), polynomial fitting (Telford et al., \u003cspan citationid=\"CR34\" class=\"CitationRef\"\u003e1990\u003c/span\u003e), Wiener filtering (Pawlowski and Hansen, \u003cspan citationid=\"CR27\" class=\"CitationRef\"\u003e1990\u003c/span\u003e), preferential continuation (Pawlowski, \u003cspan citationid=\"CR26\" class=\"CitationRef\"\u003e1995\u003c/span\u003e), wavelet transformation multiple-scale decomposition (Fedi and Quarta, \u003cspan citationid=\"CR10\" class=\"CitationRef\"\u003e1998\u003c/span\u003e) and nonlinear filtering (Keating and Pinet, \u003cspan citationid=\"CR16\" class=\"CitationRef\"\u003e2011\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eThe wavelet multi-scale decomposition (WMSD) method is helpful for decomposing the gravity and magnetic data to obtain residual and regional anomalies at different depths (Fedi and Quarta \u003cspan citationid=\"CR10\" class=\"CitationRef\"\u003e1998\u003c/span\u003e; Xu et al., \u003cspan citationid=\"CR40\" class=\"CitationRef\"\u003e2015\u003c/span\u003e; Xu et al., \u003cspan citationid=\"CR38\" class=\"CitationRef\"\u003e2017\u003c/span\u003e). Yang et al. (\u003cspan citationid=\"CR42\" class=\"CitationRef\"\u003e2015\u003c/span\u003e) used the WMSD method to obtain the gravity effects at various depths of the Tibet Plateau and analyzed the geological structure at different depths. Xu et al. (\u003cspan citationid=\"CR39\" class=\"CitationRef\"\u003e2018\u003c/span\u003e) also used an improved WMSD method to analyze the gravity anomaly of the Tibet Plateau. The quality of results of WMSD method depends on wavelet basis function and decomposition terms. It has been shown that the \u0026ldquo;Coif3\u0026rdquo; wavelet basis function can be used to obtain the best decompose result (Xu et al., \u003cspan citationid=\"CR38\" class=\"CitationRef\"\u003e2017\u003c/span\u003e). The decomposition terms need to be specific for different data. It depends on the depth of the equivalent layer.\u003c/p\u003e \u003cp\u003eTherefore, the \u0026ldquo;Coif3\u0026rdquo; wavelet basis function was used to implement the potential field separation in this paper. First, we decomposed the gravity and magnetic data, and multi-scale data were obtained. The average depths of the equivalent layers were estimated using a radially averaged logarithm power spectrum. Then, the residual anomaly (generated by crustal) and regional anomaly (generated by Moho) were obtained. Finally, the crustal structure was inverted using the residual anomaly.\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec8\" class=\"Section2\"\u003e \u003ch2\u003e4.2 Iterative compact depth from extreme points imaging algorithm\u003c/h2\u003e \u003cp\u003eInversion of potential field data is a powerful interpretation tool that provides a meaningful description of the source distribution (magnetization or density). Inversion methods are computationally expensive; moreover, the source models depend on the a priori information and constraints (Pilkington \u003cspan citationid=\"CR28\" class=\"CitationRef\"\u003e1996\u003c/span\u003e). In studying the crustal structure, it is often difficult to carry out inversion calculations directly because of the large amount of data and few constraints. In addition to inversion, imaging methods may provide a fast preliminary picture of the source distribution. Various imaging methods have been proposed and used to solve different problems (Fedi et al., 2012). It can provide an initial source model to be improved with more refined inversion algorithms.\u003c/p\u003e \u003cp\u003eDepth from Extreme Points (DEXP) image method is a popular method. It has been successfully applied in target locations (Paletti et al., 2020), geologic source imaging (Milano et al.., \u003cspan citationid=\"CR23\" class=\"CitationRef\"\u003e2016\u003c/span\u003e; Paoletti et al, \u003cspan citationid=\"CR24\" class=\"CitationRef\"\u003e2016\u003c/span\u003e), and other studies. Based on the DEXP image method, Baniamerian et al. (\u003cspan citationid=\"CR3\" class=\"CitationRef\"\u003e2016\u003c/span\u003e) proposed a new algorithm called \u0026ldquo;Compact Depth from Extreme Points,\u0026rdquo; which iteratively produces different source distribution models with an increasing degree of compactness and, correspondingly, increasing source-density values. Liu et al. (\u003cspan citationid=\"CR19\" class=\"CitationRef\"\u003e2020\u003c/span\u003e) compared the ICDEXP method with the inversion method and found that the ICDEXP method does not require any matrix inversions, so extensive RAM is not needed, and the solution can converge faster than the inverse algorithm. Furthermore, the results of the ICDEXP and inversion method are very similar. Therefore, this paper used the ICDEXP method to invert residual anomalies and obtain crustal structure.\u003c/p\u003e \u003c/div\u003e"},{"header":"5. Results","content":"\u003cdiv id=\"Sec10\" class=\"Section2\"\u003e \u003ch2\u003e5.1 The results of potential data separation\u003c/h2\u003e \u003cp\u003eFigure\u0026nbsp;\u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e shows the results of WMSD, and the depth was calculated using the radially averaged logarithm power spectrum. In the wavelet decompositions, the regional component of the 4th terms of wavelet decomposition corresponds to a depth of 55 km, the average depth to the Moho (Shen et al., \u003cspan citationid=\"CR29\" class=\"CitationRef\"\u003e2016\u003c/span\u003e; Gao et al., \u003cspan citationid=\"CR13\" class=\"CitationRef\"\u003e2020\u003c/span\u003e). Therefore, its regional component can be believed to be caused by Moho. The distribution characteristics correspond to the Moho undulation. Therefore, we can use the result to calculate the depth of Moho, and the sum of 1st, 2nd, 3\u003csup\u003erd,\u003c/sup\u003e and 4th detail features of the wavelet decomposition can be used as the residual anomaly. The depths of 1st\u0026thinsp;+\u0026thinsp;2nd, 3rd, and 4th wavelet decomposition are 5 km, 20 km, and 45 km.\u003c/p\u003e \u003cp\u003eCompared with the original gravity anomaly, the characteristics of positive and negative local field alternation are more prominent. The overall characteristics of low in the southwest and high in the northeast were removed, indicating that the influence of the fluctuation characteristics of the deep Moho is removed, and the crustal density structure can be obtained. In the interior of the basin, there are large areas of negative gravity anomalies. There are also apparent negative anomalies near the Wahongshan and Xinjie faults. Overall, there are numerous low-density anomaly field sources in the crust.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003eThe gradient zone with sharp changes in NNW direction between 101 \u0026deg; E and 102 \u0026deg; E in the east of the working area appears to be caused by the Xinjie fault. The fault is ~\u0026thinsp;20 km wide and has a prominent semi-flower structure (Zhang et al., \u003cspan citationid=\"CR51\" class=\"CitationRef\"\u003e2020a\u003c/span\u003e). It is the western boundary of the Guide Basin and the boundary between the Guide and Gonghe Basins. It mainly exposes banded Indosinian granites formed by sliding melting carried by the fault (Zhang et al., \u003cspan citationid=\"CR55\" class=\"CitationRef\"\u003e2007\u003c/span\u003e). Near the Xinjie fault, it is inferred that these hot springs correspond to this low-density gravity anomaly zone, and abundant hot springs are exposed nearby.\u003c/p\u003e \u003cp\u003eThe NW trending gradient zone with abnormally sharp changes distributed in the west is caused by hidden faults such as the Guinan Nanshan fault, Wahongshan-Wenquan fault, and Wayuxiangka-Guinan fault. Intermittent strip or elliptical low-density gravity anomalies correspond to negative landforms such as intermountain basins and valleys. Generally, it is inferred that NW trending structures control the distribution of low-density bodies near the Gonghe Basin in the west, and the distribution of low-density bodies near the Guide basin in the east is controlled by NNW trending structures.\u003c/p\u003e \u003cp\u003eSimilarly, we use the WMSD to separate the residual and regional anomalies of magnetic data. Firstly, residual results of the 1st, 2nd, 3rd, and 4th (Fig.\u0026nbsp;\u003cspan refid=\"Fig5\" class=\"InternalRef\"\u003e5\u003c/span\u003e) were obtained, and the equivalent depths were calculated using a radially averaged logarithm power spectrum. To compare with geological information, the depth of 1st\u0026thinsp;+\u0026thinsp;2nd, 3rd, and 4th wavelet decomposition is 3 km, 9 km, and 15 km. Then the sum of the 1st, 2nd, 3rd, and 4th detail features of the wavelet decomposition can be used as the residual anomaly because the magnetism disappears under the Curie point depth. The residual magnetic anomaly obtained after removing the regional field can be regarded as the distribution of magnetic anomaly generated by the substances above the Curie point depth. The main distribution directions of magnetic anomaly strips are NNW and NW, which are consistent with the main distribution directions of gravity anomalies.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003eThe main distribution direction in the western Gonghe Basin is NW, and NNW in the eastern Guide Basin. The weak magnetism is distributed in the Gonghe-Guide Basin. The monotonous and unvaried magnetic fields are generated by the overlying sedimentary rocks. Around the basin, positive and negative magnetic anomalies are distributed alternately in strips, which are close to the strike of main faults. The maximum value is 350 nT, which may be caused by granite intruding along the fault and its alteration zone.\u003c/p\u003e \u003cp\u003eThe magnetic anomaly is more prominent in the boundary characteristics of the basin, and the basin is controlled by NNW and NW deep faults. This may be related to the Gonghe-Guide Basin being a faulted basin controlled by late-stage faults and magmatic intrusions. Thick sedimentary layers accumulated in the basin, showing low magnetic anomalies. The late tectonic movement allowed the granite magma to intrude along the NNW and NW faults. These granite intrusions and the surrounding hydrothermal alteration often show high magnetic anomalies. In addition, the positive anomalies scattered in the basin may be caused by concealed granite.\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec11\" class=\"Section2\"\u003e \u003ch2\u003e5.2 The inversion results\u003c/h2\u003e \u003cp\u003eAccording to the results of WMSD, the field value variation characteristics at different depths were obtained, and the depth information was estimated. The average depth of the Moho surface is 55 km. Therefore, D4 is a regional field, and we have obtained the residual field of the crust by using the sum of the sum of 1st, 2nd, 3\u003csup\u003erd,\u003c/sup\u003e and 4th, as shown in Fig.\u0026nbsp;\u003cspan refid=\"Fig6\" class=\"InternalRef\"\u003e6\u003c/span\u003e. Based on this information, the inversion of crustal structure density was calculated by using the ICDEXP algorithm.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003eDuring the inversion calculation, for the satellite gravity data, the maximum depth was set as 50 km, the structure index was 3, the number of iterations was 20, and the upper and lower density limits were 1 and \u0026minus;\u0026thinsp;1. The three-dimensional structure result and vertical slices diagram are shown in Fig.\u0026nbsp;\u003cspan refid=\"Fig7\" class=\"InternalRef\"\u003e7\u003c/span\u003e. The vertical slices AA\u0026rsquo; is a profile located outside the basin. The densities of these slices are minor, and the negative data correspond to the Wahongshan fault.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003eThe vertical slices BB\u0026rsquo; and CC\u0026rsquo; are located near Tanggemu and Gonghe, located in the west and east basin, respectively. The negative density data is prominent. In profile BB\u0026rsquo;, the two negative densities correspond to the west Gonghe Basin and the Wahongshan fault. The vertical slice CC\u0026rsquo; goes through the Gonghe Basin and near the town of Guinan. Two negative densities are located near the town of Gonghe and Guinan, which may be caused by deep partial melting. In the three-dimensional diagram and vertical section, the depth range of the density anomaly is clearly displayed, concentrated at a depth ranging between 15\u0026thinsp;~\u0026thinsp;35km. Cross section DD\u0026rsquo; passes through the town of Guide. The negative densities are also very obvious in this profile. The burial depth is 15 km\u0026thinsp;~\u0026thinsp;35 km, corresponding to the Xinjie fault and deep partial melting near the town of Guide.\u003c/p\u003e \u003cp\u003eFor display convenience, we intercepted the results of different depths (5, 10, 15, 20, 25, 30, 35 and 40 km), shown in Fig.\u0026nbsp;\u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e. The inversion results of different depths varied between methods. The sedimentary layers at shallow depths (up to 5 km) have little density fluctuation, consistent with the previous conclusion that the Cenozoic sedimentary thickness is greater than 5km (Sun et al., \u003cspan citationid=\"CR32\" class=\"CitationRef\"\u003e2011\u003c/span\u003e). The low velocity bodies from near surface to a depth of about 5\u0026ndash;10 km are Quaternary loose or weakly diagenetic strata, and there is no strong density anomaly in the shallow part. At 10 km and on, the high- and low-density anomalies are patently staged by stage. In addition to the shallow sedimentary layer with little density fluctuation, the resolution of satellite gravity cannot obtain shallow details. The distribution of density anomalies changes significantly from 15 km to 35 km. At depths greater than 35 km, the difference between high and low density anomalies begins to decrease. This shows that the density anomalies are mainly concentrated in the range of 15\u0026thinsp;~\u0026thinsp;35km.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003eAt a depth of 15km\u0026thinsp;~\u0026thinsp;35km, the low-density anomaly is mainly distributed in the corresponding main fault zones, and the difference between high and low density anomalies is small. It is concentrated in the Wahongshan fault on the west side of the basin, the Xinjie Fault, and the Duohemao fault on the east side. The Xinjie fault corresponds well with known hot spots, so it can be inferred that the geothermal energy in this area is mainly concentrated in these low-density bodies and their vicinity.\u003c/p\u003e \u003cp\u003eAt the depths\u0026thinsp;\u0026gt;\u0026thinsp;35km, the density distribution characteristic changes significantly. At a depth of 40km near the Xinjie fault zone, there are apparent low-density anomalies, and the low-density anomalies at other locations tend to disappear. It is speculated that the undercut depth of the Xinjie fault zone changes from south to north. This phenomenon can explain why the temperature increases successively from south to north. Generally speaking, the faults on the west side of the Gonghe-Guide Basin extend deep, mainly consisting of large faults extending into the lower crust. The eastern side of the fault is shallow. Therefore, the basin basement is deep in the west and shallow in the east.\u003c/p\u003e \u003cp\u003eSimilarly, based on the wavelet multi-scale decomposition method, Fig.\u0026nbsp;\u003cspan refid=\"Fig9\" class=\"InternalRef\"\u003e9\u003c/span\u003e shows the residual magnetic anomaly, which is the magnetic material feature above the Curie point depth. During the inversion, for the aeromagnetic data, the maximum depth was set as 30km, the structure index was 3, the number of iterations was 20, and the upper and lower magnetization limits were 1 and \u0026minus;\u0026thinsp;1. The three-dimensional inversion results were obtained, as shown in Fig.\u0026nbsp;\u003cspan refid=\"Fig10\" class=\"InternalRef\"\u003e10\u003c/span\u003e. To compare with gravity data, slices were taken at the same locations as Fig.\u0026nbsp;\u003cspan refid=\"Fig7\" class=\"InternalRef\"\u003e7\u003c/span\u003e.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003eThe magnetic variation characteristic from shallow to deep is prominent. In the AA\u0026rsquo; profile, magnetism is strong because of the intense tectonic activity. However, it is negative at the Wahongshan fault. Similarly, in the BB\u0026rsquo; section, there is a significant negative magnetic anomaly on the west side of the Gonghe Basin with a depth range of 6\u0026thinsp;~\u0026thinsp;24km. The magnetism slowly dissipates with depth. In the CC\u0026rsquo; section, a strong positive magnetic body in the basin\u0026rsquo;s center extends to 24km and below. This is a high-density and high magnetic anomaly body relative to the surrounding partial melting. It is speculated that this is a hidden granite body. No partial melting has occurred. Near the towns of Chaka, Tanggemu, Gonghe, and Xinjie, small-scale high magnetic anomalies at shallow depths and low magnetic negative anomalies at deeper depths, indicat shallow granite bodies and deep partial melting areas. This is consistent with the gravity results and the depth range. The same characteristics occur in section DD\u0026rsquo;; the characteristics of the Guide area are very similar to Gonghe, both of which are shallow granite bodies with deep weak or negative magnetic anomaly characteristics, reflecting deep partial melting.\u003c/p\u003e \u003cp\u003eTo facilitate analysis and display, slices at different depths were also made, as shown in Fig.\u0026nbsp;\u003cspan refid=\"Fig11\" class=\"InternalRef\"\u003e11\u003c/span\u003e. At 3km and shallower depths, there are no significant magnetic anomalies, indicating no apparent magnetic body in the shallow part dominated by sedimentation. At depths less than 3km, there is weak magnetism and no apparent magnetic anomaly. It is speculated that sedimentary rocks mainly cause these characteristics. Furthermore, the resolution of the shallow data also can be a factor.\u003c/p\u003e \u003cp\u003eIn all the results at depths\u0026thinsp;\u0026gt;\u0026thinsp;6km, there are scattered magnetic anomalies, mainly concentrated in the edge of the basin, faults, fold zones, and granite outcropping area in the western part of the basin. It is speculated that they are related to granite intrusions. The magnetic field inside the basin is consistent, and there is no obvious abnormal body. The magnetic bodies are mainly concentrated in the center of the basin.\u003c/p\u003e \u003cp\u003eAt a depth of 6 km, an east-west elliptical positive magnetic anomaly appears in east Gonghe County. This location also corresponds with a negative gravity anomaly, speculated as the Qiabuqia dry hot rock mass. It has been confirmed that the Qiabuqia thermal rock mass is about 21 km long in the east-west direction and 14 km wide in the north-south direction. The plane is nearly elliptical and develops stably within the depth of 21km (Zhang et al., \u003cspan citationid=\"CR51\" class=\"CitationRef\"\u003e2020a\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eThere is a positive magnetic anomaly with a length of ~\u0026thinsp;150km in the east-west direction in the granite area near Tanggemu. This location is also a negative gravity anomaly. The magnetic anomaly disappears at a depth of 24km. It is inferred that it is a granite intrusion extending to 24km. The difference from the Qiabuqia dry thermal rock mass is that the intrusion extends deeper. However, this granite mass has no surface exposure and no thermal insulation cover. The intrusive body extends deeply, and the concealed body can be found nearby as a geothermal exploration target.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003eAt a depth of 9 km, an NW bead-like positive magnetic anomaly is highlighted near the Wahongshan in the southwestern Wayuxiangka. There are dense EW and NW-W faults, numerous Permian and Triassic granites, and hot springs. There is also an apparent positive magnetic anomaly at a depth of 24km, indicating that this area is an excellent geothermal exploration area.\u003c/p\u003e \u003cp\u003eIn general, the gradient zone of magnetic anomaly from 15 km to 24 km is gradually flattened, indicating that the existence of underground high temperatures leads to the disappearance or weakening of magnetism. It is speculated that high temperatures have demagnetized the material.\u003c/p\u003e \u003cp\u003eTo further confirm and verify the correctness of the above interpretation, based on the inversion results, a 2D geologic model of CC\u0026rsquo; profile is created to show the detailed tectonic framework (Fig.\u0026nbsp;\u003cspan refid=\"Fig12\" class=\"InternalRef\"\u003e12\u003c/span\u003e). In the basin, the experimental density and magnetic susceptibility of granites are 2.532\u0026ndash;2.555 g/cm3 and 0.0456\u0026times;10\u003csup\u003e\u0026ndash;3\u003c/sup\u003e ~13.847\u0026times;10\u003csup\u003e\u0026ndash;3\u003c/sup\u003e SI separately (Zhao et al., 2020). The partial melting is widespread in in the upper-middle crust, where the density is set as 2.4\u0026ndash;2.5 g/cm\u003csup\u003e3\u003c/sup\u003e. Correspondingly, middle and lower crust densities are set as 2.8 g/cm\u003csup\u003e3\u003c/sup\u003e and 3 g/cm\u003csup\u003e3\u003c/sup\u003e, respectively. To fit the magnetic data, we set the magnetic susceptibility of granite as 0.1\u0026times;10\u003csup\u003e\u0026ndash;3\u003c/sup\u003e SI for Ordovician granite and 0.05\u0026times;10\u003csup\u003e\u0026ndash;3\u003c/sup\u003e SI for Indosimian granite. The geologic model of CC\u0026rsquo; profile corresponds well with our inversion results, in which the partial melting is located deeper, and the granites are shallow.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003c/div\u003e"},{"header":"6 Discussion","content":"\u003cdiv id=\"Sec13\" class=\"Section2\"\u003e \u003ch2\u003e6.1 Crustal partial melting\u003c/h2\u003e \u003cp\u003ePrevious studies have shown that partial melting and fluids usually cause significant S-wave low-speed anomalies, and S-wave low-speed anomalies may also superimpose the effects of temperature increases and partial melting simultaneously (McKenzie et al., \u003cspan citationid=\"CR22\" class=\"CitationRef\"\u003e2005\u003c/span\u003e). Furthermore, the MT results show that high conductivity regions can be interpreted as partial melting in the crust (Zhang et al., \u003cspan citationid=\"CR50\" class=\"CitationRef\"\u003e2021\u003c/span\u003e; Tang et al., \u003cspan citationid=\"CR33\" class=\"CitationRef\"\u003e2021\u003c/span\u003e). However, the characteristic of density and magnetism have not been explicated.\u003c/p\u003e \u003cp\u003eIn this study, we use the wavelet multi-scale field separation method and three-dimensional fast iteration imaging to implement the inversion calculation of large-scale data. We make full use of the advantages of gravity and magnetic field data in the study of regional geological structures. Effective residual anomalies were obtained based on the wavelet multi-scale field separation method, and subsurface material distribution characteristics were inverted.\u003c/p\u003e \u003cp\u003eIn the residual anomalies of the Gonghe-Guide Basin, a wide range of negative gravity and magnetic anomalies are displayed, which reflect the existence of low-density and magnetism geological bodies underlying the basin to a certain extent. The negative gravity anomalies correspond to the low resistivity and low velocity of previous results (Zhang et al., \u003cspan citationid=\"CR49\" class=\"CitationRef\"\u003e2017\u003c/span\u003e). In addition, a temperature change is mainly manifested in the demagnetization of magnetic minerals and negative or weak magnetic anomalies. Especially when the rock temperature rises to the Curie temperature, rock magnetism disappears (Zeng et al., \u003cspan citationid=\"CR43\" class=\"CitationRef\"\u003e2012\u003c/span\u003e). Based on this, we preliminarily believe that the negative or large consistent low magnetic field area in the Gonghe-Guide Basin may be related to the demagnetization of magnetic minerals caused by deep thermal factors. Based on low density and weak magnetism characteristics, it is reasonable to speculate partial melting regions in the deep crust. However, it is not enough to extrapolate solely from residual anomalies.\u003c/p\u003e \u003cp\u003eIn the study of large-scale crustal structural characteristics, the fast iteration imaging method (ICDEXP) reflects the advantages of calculation. The inversion results of gravity and magnetic data are consistent with the results of MT and seismic, and the existence of partial melting regions in the Gonghe-Guide Basin is further shown. From the inversion results, the density distribution is uniform from the near-surface to a depth of ~\u0026thinsp;5 km, indicating Quaternary loose or weakly diagenetic stratum. Low-density geological bodies dominate the middle and lower crust from ~\u0026thinsp;15 to 35 km, mainly distributed in the towns of Gonghe, Chaka, Tanggemu, Xinjie, Chaka, Xinjei, Wayuxiangka and Guide of the basin. In these areas, it also has certain low/weak magnetism. This characteristic can be inferred as a part of the partial melting regions. We determined the characteristics by using gravity and magnetic data inversion. Thus, we concluded that partial melting regions in the crust are generally characterized by low resistivity, low velocity, low density, and weak or no magnetism.\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec14\" class=\"Section2\"\u003e \u003ch2\u003e6.2 Hot dry rock target areas and their characteristics\u003c/h2\u003e \u003cp\u003eThe idea of a partial melting area as a geothermal target needs further discussion. We found that density and magnetism correspond well at deep depths, with low density and low magnetism characteristics. However, as the main area of dry hot rock in Gonghe-Guide Basin, the shallow parts must have granite distributed throughout (Gao et al., \u003cspan citationid=\"CR13\" class=\"CitationRef\"\u003e2020\u003c/span\u003e; Tang et al., \u003cspan citationid=\"CR33\" class=\"CitationRef\"\u003e2021\u003c/span\u003e). Therefore, the shallow should have specific characteristics consisting of high magnetic anomalies. Therefore, we further analyze the target distribution of the dry hot rocks.\u003c/p\u003e \u003cp\u003eThe gravity and magnetic data show the partial melting regions of the entire basin and its surroundings, making it easier to delineate the existence of target areas. The results of the 3D inversion imaging prove this point. In the inversion results, the Gonghe-Guide basin shows a wide range of low-density and weak or low magnetic geological bodies, which suggests that there are high-temperature geological bodies or partial melting layers deep in the crust.\u003c/p\u003e \u003cp\u003eWe can conclude that the partial melting regions are the key geothermal prospecting target but not completely. Another key factor is the shallow signature. Because the granite also has low density, magnetic data must be used to distinguish geothermal targets. Based upon this study, the targets are the low/ negative density corresponding to low/negative magnetism in the deep and high/ positive magnetism in the shallow. According to the geological map of the study area, the strong magnetic anomaly is mainly due to the existence of intrusive granite rocks and granodiorite in the study area. Therefore, in the Gonghe-Guide Basin, the key geothermal prospecting target can be located near the towns of Guide, Gonghe, Xinjie, Chaka, Wayuxiangka, Tanggemu, Xinhai. In addition, the Wahongshan and Xinjie faults also can be ideal geothermal prospecting targets.\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec15\" class=\"Section2\"\u003e \u003ch2\u003e6.3 The geothermal source mechanism\u003c/h2\u003e \u003cp\u003eDetermining the geothermal source mechanism is the main problem in geothermal exploration in the Gonghe-Guide Basin, and it is also a common problem in geothermal resource exploration in other similar basins. Different authors have proposed different mechanisms. There are three primary hypotheses: (1) Granite is the primary heat source (Zhang C. et al., \u003cspan citationid=\"CR44\" class=\"CitationRef\"\u003e2018\u003c/span\u003e;Zhang et al., \u003cspan citationid=\"CR53\" class=\"CitationRef\"\u003e2019\u003c/span\u003e)༛(2) The geothermal is sourced from deeper sections, and transmits to the shallow part through the flower-shaped faults (Zhang S. et al., \u003cspan citationid=\"CR52\" class=\"CitationRef\"\u003e2018\u003c/span\u003e; Gao et al., \u003cspan citationid=\"CR14\" class=\"CitationRef\"\u003e2018\u003c/span\u003e)༛(3) Geothermal is sourced from the deep mantle (Feng et al., \u003cspan citationid=\"CR11\" class=\"CitationRef\"\u003e2018\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eThese three views have certain rationality but also have shortcomings. The geothermal mechanisms are uncertain and have yet to be proven. The mechanisms of conduction and heat accumulation are also unclear. Overall, these disputes affect the understanding of dry hot rocks themselves and restrict the evaluation and efficient development and utilization of geothermal resources.\u003c/p\u003e \u003cp\u003eThe hot springs in the region are primarily concentrated along faults. Hot springs with higher temperatures are not directly formed in the basin due to the influence of sedimentary layers. This shows that the heat source in the study area mainly comes from the crust and at depth. According to the inversion results in this paper, several large faults, such as Duomaohe, Xinjie, and Qinghainanshan, extend deep into the crust. These faults also have high-temperature large hot springs, suggesting that large-scale faults play a vital role in heat conduction and supply. The Gonghe-Guide Basin is a faulted basin with a thick sedimentary cover and fault zones controlled by the stress field of the Tibet Plateau. Due to the existence of large-scale high-temperature bodies and the negative topography of the basin, the interior of the basin shows negative density and weak magnetism.\u003c/p\u003e \u003cp\u003eMany fault zones around the basin allow high-temperature magma to intrude along the fault. The high-temperature alteration of the intrusive bodies and surrounding rocks makes prominent positive and negative alternating magnetic anomaly bands near the fault zone. The geothermal springs in the Gonghe-Guide Basin are mainly exposed near the fault zones on the east and west sides of the basin. Due to the numerous granite intrusions near the fault zone on the southwest side of the basin, magnetic anomalies controlled by structures are distributed in strips. It is speculated that the geothermal source here may be dominated by a large amount of deep molten materials.\u003c/p\u003e \u003cp\u003eIn addition, there has been no volcanic and magmatic activity in Gonghe Basin and its surrounding orogenic belt since the Cenozoic. The average heat generation rate of radioactive elements in drill core is 4.43 \u0026micro;W/m\u003csup\u003e3\u003c/sup\u003e (Zhang et al., \u003cspan citationid=\"CR51\" class=\"CitationRef\"\u003e2020a\u003c/span\u003e), which slightly higher than the global average value (3.09 \u0026micro;W/m\u003csup\u003e3\u003c/sup\u003e) of radioactive element heat generation rate of Mesozoic Cenozoic granite (Artemieva et al., \u003cspan citationid=\"CR2\" class=\"CitationRef\"\u003e2017\u003c/span\u003e). However, it is much lower than the basement granite in the area where the dry hot rock is produced in the Cooper Basin in Australia, with up to 7\u0026thinsp;~\u0026thinsp;10 \u0026micro;W/m\u003csup\u003e3\u003c/sup\u003e of radioactive element heat generation rate (McLaren et al., \u003cspan citationid=\"CR21\" class=\"CitationRef\"\u003e2003\u003c/span\u003e; Beardsmore, \u003cspan citationid=\"CR4\" class=\"CitationRef\"\u003e2004\u003c/span\u003e). Therefore, it is difficult for radioactive element decay heat generation to constitute the main heat source of Gonghe-Guide Basin. The residual heat of the granite magma and the heat generated by the decay of radioactive elements are probably not the heat source of the hot dry rock in the Gonghe-Guide Basin.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003eIn summary, as shown in Fig.\u0026nbsp;\u003cspan refid=\"Fig13\" class=\"InternalRef\"\u003e13\u003c/span\u003e, we suggest that the essential geothermal source comes from the mantle caused by substantial tectonic activities since the early Cenozoic (Graddock et al., 2014; Gao et al. \u003cspan citationid=\"CR13\" class=\"CitationRef\"\u003e2020\u003c/span\u003e), causing partial melting in the crustal, and the heat flows from deep to shallow along the faults. The Quaternary sediments covering the surface of the Gonghe Basin can serve as the geothermal system\u0026rsquo;s caprock. The heat source structure of the Gonghe-Guide Basin is closely related to the geological structure in the crust.\u003c/p\u003e \u003c/div\u003e"},{"header":"7 Conclusions","content":"\u003cp\u003eThe crustal structure of the entire Gonghe-Guide Basin was obtained based on the satellite gravity and aeromagnetic data, using the wavelet multi-scale decomposition field separation method and the iterative fast imaging inversion method, providing evidence for the existence of underground partial melting regions. The results show that the location of deep low density and low magnetic anomalies corresponds well to the partial melting regions and corresponds to the results of previous MT and seismic methods. In addition, the inversion results in this paper show that the regions near the town of Guide, Gonghe, Xinjie, Chaka, Wayuxiangka, Tanggemu, Xinhai, and Xinjie have abnormal characteristics of low density, shallow high magnetism, and deep low magnetism. These areas have good geothermal target potential, consistent with the existing geological and borehole data. Therefore, in the inversion of gravity and magnetic anomalies, regions with similar characteristics can be used as targets of geothermal resources. Combined with other geologic data, we suggest that the heat source mechanism is heating from deep to shallow due to mantle material upwelling and early Cenozoic Indosinian tectonic movement. The most important heat source comes from the mantle and tectonic activities, causing partial melting in the crust. The heat continues to flow along the faults into shallow strata, heating the surrounding rocks to adequate temperatures for geothermal exploration.\u003c/p\u003e"},{"header":"Declarations","content":"\u003cp\u003e\u003cstrong\u003eACKNOWLEDGMENTS\u003c/strong\u003e\u003c/p\u003e\n\u003cp\u003eWenna Zhou would like to thank Prof. Shuang Liu of China University of Geosciences (Wuhan) for providing their ICDEXP code and permission to use it. This research was partly supported by the National Natural Science Foundation (42004068), the Second Tibetan Plateau Scientific Expedition and Research Program (Grant No. 2019QZKK0704), the Fundamental Research Funds for the Central Universities (Grant No. lzujbky-2021-sp65), the Science and Technology Plan of Gansu Province (20JR5RA251) and the Science and Technology Innovation 2025 Major project of Ningbo (2020Z073).\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003eDATA AVAILABILITY\u003c/strong\u003e\u003c/p\u003e\n\u003cp\u003eThe gravity data can be download from ICGEM (http://icgem.gfz-potsdam.de/home). The aeromagnetic data associated with this research are confidential and cannot be released.\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003eAUTHOR CONTRIBUTION STATEMENT:\u003c/strong\u003e\u003c/p\u003e\n\u003cp\u003eWenna Zhou: Methodology, Software, Formal analysis, Visualization, Writing - Original Draft, Review \u0026amp; Editing, Funding acquisition, Supervision.\u003c/p\u003e\n\u003cp\u003eQiang Li: Formal analysis, Visualization, Writing - Original Draft, Review \u0026amp; Editing, Funding acquisition.\u003c/p\u003e\n\u003cp\u003eDailei Zhang: Formal analysis, Review \u0026amp; Editing, Funding acquisition.\u003c/p\u003e\n\u003cp\u003eHai Tang: Image editing, Validation.\u003c/p\u003e"},{"header":"References","content":"\u003col\u003e\n\u003cli\u003eArkani-Hamed, J., 2007. Differential reduction to the pole: revisited. Geophysics 72, L13\u0026ndash;L20.\u003c/li\u003e\n\u003cli\u003eArtemieva IM, Thybo H, Jakobsen K, S\u0026oslash;rensen NK, Nielsen LSK., 2017. 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Characteristics of regional and geothermal geology of the Reshuiquan HDR in Guide County, Qinghai Province. Acta geologice sinica. 94,1591\u0026ndash;1605 (in Chinese with English abstract). https://doi.org/10.19762/j.cnki.dizhixuebao.2020159\u003c/li\u003e\n\u003cli\u003eZhang, S., Yan, W., Li, D., Jia, X., Zhang, S., Li, S., Fu, L., Wu, H., Zeng, Z., Li, Z., Mu, J., Cheng, Z., Hu, L., 2018. Characteristics of geothermal geology of the Qiabuqia HDR in Gonghe Basin, Qinghai Province. Geol. China 45, 1087\u0026ndash;1102(in Chinese with English abstract). https://doi.org/10.12029/gc20180601\u003c/li\u003e\n\u003cli\u003eZhang, S., Zhang, L., Tian, C., Cai, J., and Tang, B., 2019. Occurrence geological characteristics and development potential of hot dry rocks in Qinghai Gonghe Basin. 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Journal of Qinghai Environment 19, 81\u0026ndash;84 (in Chinese with English abstract). https://doi.org/10.3969/j.issn.1007-2454.2009.02.010\u003c/li\u003e\n\u003cli\u003eZheng, J., Griffin, W., Sun, M., O\u0026rsquo;Reilly, S., Zhang, H., Zhou, H., Xiao, L., Tang, H., Zhang, Z., 2010. Tectonic affinity of the west Qinling terrane (central China): North China or Yangtze? Tectonics 29, 1\u0026ndash;14. https://doi.org/10.1029/2008TC002428\u003c/li\u003e\n\u003c/ol\u003e"}],"fulltextSource":"","fullText":"","funders":[],"hasAdminPriorityOnWorkflow":false,"hasManuscriptDocX":true,"hasOptedInToPreprint":true,"hasPassedJournalQc":"","hasAnyPriority":false,"hideJournal":false,"highlight":"","institution":"","isAcceptedByJournal":true,"isAuthorSuppliedPdf":false,"isDeskRejected":"","isHiddenFromSearch":false,"isInQc":false,"isInWorkflow":false,"isPdf":false,"isPdfUpToDate":true,"isWithdrawnOrRetracted":false,"journal":{"display":true,"email":"[email protected]","identity":"pure-and-applied-geophysics","isNatureJournal":false,"hasQc":true,"allowDirectSubmit":false,"externalIdentity":"paag","sideBox":"Learn more about [Pure and Applied Geophysics](https://www.springer.com/journal/24)","snPcode":"24","submissionUrl":"https://submission.nature.com/new-submission/24/3","title":"Pure and Applied Geophysics","twitterHandle":"","acdcEnabled":true,"dfaEnabled":true,"editorialSystem":"em","reportingPortfolio":"Springer Hybrid","inReviewEnabled":true,"inReviewRevisionsEnabled":false},"keywords":"Satellite gravity, Crustal structure, Magnetic anomalies and interpretation, Heat generation and transport, Geothermal mechanisms","lastPublishedDoi":"10.21203/rs.3.rs-2249266/v1","lastPublishedDoiUrl":"https://doi.org/10.21203/rs.3.rs-2249266/v1","license":{"name":"CC BY 4.0","url":"https://creativecommons.org/licenses/by/4.0/"},"manuscriptAbstract":"\u003cp\u003eGonghe-Guide Basin is situated in the northeastern edge of the Tibetan Plateau. one of China's main targets for geothermal research and exploitation. It is also a crucial region for studying the Tibetan Plateau's uplift mechanisms. Therefore, the elaborate crustal structure of the entire basin is essential for recognizing the geothermal mechanisms, geothermal source targets and even the uplift mechanisms of the Tibetan Plateau. However, these issues remain enigmatic, partly because it is difficult to depict the crustal structure of entire base by using the profile results of magnetotelluric and seismic data. To overcome the limitations of profile results, we present a new crustal structure of the entire Gonghe-Guide Basin by using EIGEN-6C4 satellite gravity and aeromagnetic data. The gravity and magnetic data were processed using the wavelet multi-scale decomposition method and the iterative compact depth from extreme points imaging method. Satisfactory residual anomalies and inversion results were obtained. The gravity inversion results reveal pronounced low-density regions at the depths of 15\u0026ndash;35 km in the middle-upper crustal, most likely caused by partial melting from heating the overlying hot dry rocks. The results correspond well with the magnetotelluric and seismic results and are an effective supplement. The magnetic inversion results show negative or no magnetism within a similar depth range. But at shallow depths of the same horizontal positions, there is high positive magnetism, which can be interpreted as granite. To confirm and validate this conclusion, a 2D geologic model of a profile from a typical area is created to show the detailed tectonic. Based on the new crustal structure results, the suggested geothermal target is the low/negative density corresponding to low/negative magnetism located at deep depths and high/ positive magnetism located at shallow depths. These density and magnetism anomalies are primarily located near the town of Guide, Gonghe, Xinjie, Chaka, Wayuxiangka, Tanggemu, Xinhai, which can be considered geothermal source targets. The geothermal source is thought to be due to mantle material upwelling or faults activity causing partial melting in the crust, and heat flows from deep to shallow along the faults in the region. Then we established a geological conceptual model to illustrate this process. This indicates that tectonic movement is taking place in the deep part of the earth in Gonghe-Guide Basin. The research on the geological structure and geothermal heat source mechanism in the Gonghe-Guide Basin can provide a primary reference for research on geothermal resources in other areas with similar geological structures.\u003c/p\u003e","manuscriptTitle":"Crustal structure and geothermal mechanism of Gonghe-Guide Basin based on EIGEN-6C4 satellite gravity and aeromagnetic data","msid":"","msnumber":"","nonDraftVersions":[{"code":1,"date":"2022-11-14 15:04:20","doi":"10.21203/rs.3.rs-2249266/v1","editorialEvents":[{"type":"communityComments","content":0},{"type":"editorAssigned","content":"","date":"2022-11-09T07:10:15+00:00","index":"","fulltext":""},{"type":"checksComplete","content":"","date":"2022-11-09T04:10:09+00:00","index":"","fulltext":""},{"type":"submitted","content":"Pure and Applied Geophysics","date":"2022-11-08T04:44:32+00:00","index":"","fulltext":""}],"status":"published","journal":{"display":true,"email":"[email protected]","identity":"pure-and-applied-geophysics","isNatureJournal":false,"hasQc":true,"allowDirectSubmit":false,"externalIdentity":"paag","sideBox":"Learn more about [Pure and Applied Geophysics](https://www.springer.com/journal/24)","snPcode":"24","submissionUrl":"https://submission.nature.com/new-submission/24/3","title":"Pure and Applied Geophysics","twitterHandle":"","acdcEnabled":true,"dfaEnabled":true,"editorialSystem":"em","reportingPortfolio":"Springer Hybrid","inReviewEnabled":true,"inReviewRevisionsEnabled":false}}],"origin":"","ownerIdentity":"5bd7c75d-a4d9-4238-8524-907e3c22087c","owner":[],"postedDate":"November 14th, 2022","published":true,"recentEditorialEvents":[],"rejectedJournal":[],"revision":"","amendment":"","status":"published-in-journal","subjectAreas":[],"tags":[],"updatedAt":"2023-10-16T21:35:04+00:00","versionOfRecord":{"articleIdentity":"rs-2249266","link":"https://doi.org/10.1007/s00024-023-03290-2","journal":{"identity":"pure-and-applied-geophysics","isVorOnly":false,"title":"Pure and Applied Geophysics"},"publishedOn":"2023-06-01 21:03:55","publishedOnDateReadable":"June 1st, 2023"},"versionCreatedAt":"2022-11-14 15:04:20","video":"","vorDoi":"10.1007/s00024-023-03290-2","vorDoiUrl":"https://doi.org/10.1007/s00024-023-03290-2","workflowStages":[]},"version":"v1","identity":"rs-2249266","journalConfig":"researchsquare"},"__N_SSP":true},"page":"/article/[identity]/[[...version]]","query":{"redirect":"/article/rs-2249266","identity":"rs-2249266","version":["v1"]},"buildId":"7rjqhiLT3MXkJMwkYKINL","isFallback":false,"isExperimentalCompile":false,"dynamicIds":[84888],"gssp":true,"scriptLoader":[]}