Startseite The violent ground motion before the Jiuzhaigou earthquake Ms7.0
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The violent ground motion before the Jiuzhaigou earthquake Ms7.0

  • Kangsheng Xu EMAIL logo und Ying Li
Veröffentlicht/Copyright: 29. September 2020
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Abstract

An Ms7.0 earthquake occurred in Jiuzhaigou, Sichuan Province, China, on August 8, 2017. In this study, we used the vertical component data from 31 seismic stations near the epicenter from May 1 to August 20, 2017, to calculate the amplitude spectrum hourly using the fast Fourier transform method. Furthermore, the spectral area of the low frequency band (0.02–1 Hz), which represents the energy of low frequency motion, was calculated. In this way, the temporal and spatial variations in the vertical ground motion in this region were determined. Four high-value processes occurred in mid-June, mid-July, late July, and early August (the last three are discussed in this article). Based on a comparison with the local meteorological data, the meteorological factors had no influence, local geological factors did not affect the results, and typhoon factors did not show obvious correlation. Combined with the results of previous studies, we believe that the increase in the spectral area reflects the intense movement of deep material in the region related to the Jiuzhaigou earthquake. The spatial distribution of the spectral area (energy) reveals that the deep material moved eastward rapidly, was obstructed by the Sichuan Basin, and expanded to the northwest in a U-shaped channel, which may be the main dynamic factor for the formation or triggering of the earthquake.

Keywords: Ms7.0 Jiuzhaigou earthquake; ground motion; FFT; amplitude spectrum; spectral area; dynamic process

1 Introduction

On August 8, 2017, at 21:49:24, an Ms7.0 earthquake (33.14°N, 103.79°E) occurred in Jiuzhaigou County, Sichuan Province, China, with a focal depth of 20 km (http://news.ceic.ac.cn/CC201808211947.html). The earthquake was located in the northeastern margin of the Bayan Hara block, which is surrounded by the eastern segment of the East Kunlun Fault, the Longriba Fault, the Minjiang Fault, the Huya Fault, and the Tazang Fault. The northern segment of the Huya Fault is a left-lateral strike-slip fault, and the southern segment is a thrust fault. To the east of this fault is the Longmenshan Fault, which trends northeast. The Longmenshan Fault is a thrust fault between the Bayan Hara block and the Sichuan Basin (Figure 1). A more consistent view is that the seismogenic fault of the earthquake is in the extension line of the northern segment of the Huya Fault [1,2]. Several studies have been published on this earthquake. Based on the distribution of the aftershocks, the orientation of the long axis of the intensity determined from the field investigation, and the investigation of the collapses and landslides caused by the earthquake, several studies have pointed out that the seismogenic fault of this earthquake should be the northward extension of the Huya Fault, which is a left-lateral strike-slip fault, and the fracture process occurred upward from depth [1,2,3]. Based on the seismic observation data, several scholars have studied the crustal structure in this region. The results show that there are low velocity layers in the middle crust at a depth of 20–40 km throughout most of the regions and a few in the upper crust at depths of 10–20 km and in the lower crust at depths of 40–60 km [4]. On the southern side of the Bayan Hara block, the southeastward middle-lower crustal flow was obstructed and turned southward in the Luding-Shimian area. On the northern side of the Bayan Hara block, it flows northeastward, and there is a southeastward crustal flow perpendicular to the Longmenshan Fault. This study also shows that the crustal flow in the middle and lower crust is also diverted into the upward and downward branches after being obstructed by the Sichuan Basin, and then, it intrudes into the upper crust [5]. As for the dynamic background of the earthquake, it is generally believed that the eastward movement of the Bayan Hara block was strongly obstructed by the Sichuan Basin, which caused the accumulation of energy and led to formation of the earthquake [1,2,3,4]. Several studies have concluded that the earthquake was the result of the northeastern extrusion of the lower crust in the northeastern part of the Bayan Hara block [6,7], but a more detailed dynamic process has not been reported. In this article, the temporal and spatial characteristics of the crustal movement in this region are studied in detail using seismic observation data collected before the earthquake, and the relationship between the characteristics of the crustal movement in this region and the formation and occurrence of the Jiuzhaigou earthquake is discussed accordingly.

Figure 1 The distribution of the seismic stations used in this study and location of the Jiuzhaigou earthquake (Ms7.0).
Figure 1

The distribution of the seismic stations used in this study and location of the Jiuzhaigou earthquake (Ms7.0).

2 Methods

Our research period is from May 1 to August 20, 2017. The data were collected from 13 stations in the Gansu Seismic Network and 18 stations in the Sichuan Seismic Network, China. All of the stations have broadband seismographs with a frequency range of 60 s to 50 Hz. These stations are mainly distributed around the epicenter (Figure 1).

The signal recorded by a seismograph contains abundant frequency components. When a finite signal is expressed in the frequency domain, the signal energy is distributed at all of the frequency points, and the amplitude spectrum represents the signal energy at each frequency point. Generally, the high-frequency band of seismic records describes the shallower, small-scale, medium motion state, whereas the low-frequency band carries more deep, large-scale motion information. Since the bandwidth of the seismograph is 60 s to 50 Hz, and we focused on the low-frequency motion, the frequency range used in this study was 0.02–1 Hz. Herein, we used the spectral area (the area of the geometric shape formed by the spectral curve and the transverse axis) of this frequency band to represent the energy of the low-frequency ground motion (Figure 2). The trial calculation shows that this method reduces the sensitivity of the accidental vibration interference to the peak amplitude and makes the result more robust than the conventional peak spectrum method.

Figure 2 The amplitude spectrum of the ground motion.
Figure 2

The amplitude spectrum of the ground motion.

The data processing steps are as follows.

  1. The seismic observation records of 31 stations (112 days) were collected as the data for the study.

  2. The fast Fourier transform (FFT) of the hourly vertical recording was calculated and the amplitude spectrum was obtained.

  3. The amplitude spectrum was smoothed. The 0.02–1 Hz spectral curve and the transverse axis form a geometric shape (area enclosed by the red line in Figure 2). The area of this shape was calculated. This is defined as the spectral area.

  4. For each station, 2,688 spectral area values were obtained. The time series curve of the spectral area values from the 31 stations is shown in Figure 3.

3 Results

From May 1 to August 20, 2017, the temporal variation in the spectral areas for the 31 stations is shown in Figure 3, in which the black thick line is the mean line for all of the stations. During the study period, there were four high-value processes, which occurred in mid-June, mid-July, late July, and early August. Since the last three high-value processes have a good consistency, this study focuses on the latter three processes, which are called event 1 (July 11–21), event 2 (July 25–August 2), and event 3 (August 3–7) in chronological order. Event 2 has the largest amplitude, followed by event 1, and event 3 has the smallest amplitude. In the following description, the high value of the spectrum area is abbreviated as the high value, and its distribution area as the high value area.

Figure 3 The temporal variation in the spectral areas (May 1–August 20, 2017). The black thick line is the mean value of all of the stations.
Figure 3

The temporal variation in the spectral areas (May 1–August 20, 2017). The black thick line is the mean value of all of the stations.

To discuss the spatial characteristics of the three events, the mean values of each station from May 16 to May 31 were taken as reference values (or normal values). Their spatial distribution is shown in Figure 4a. The areas with slightly higher values mainly occurred on the western margin of the Sichuan Basin. There is a strip between Songpan-Heishui and Bazhong (about 1–2), and the rest are all below 0.8. Figure 4b shows the spatial distribution of event 1. The high value distribution range is similar to that in Figure 4a, but the values are larger, about 1.5–2.3, and the value of the low value area is larger, about 0.7–1.0. The highest value area is near Emeishan, which extends northeastward along the edge of the Sichuan Basin, and is connected to the Songpan-Heishui region. Figure 4c shows the spatial distribution of event 2, which is the largest event. The value in the study area increases overall. The peak area appears in the northwestern part of Emeishan, with values of 3–3.6. The high value area extends to the northeast along the edge of the Sichuan Basin, with values of 2.6–3.0. The value of the high value band in the north-west direction in Bazhong increases from 2.5 to 3.0. From the Longmenshan fault zone to the edge of the Sichuan Basin, the value increases gradually. Near Songpan, the value is also higher (2.3–2.5). Figure 4d shows the spatial distribution of event 3. Compared with event 2, the level of event 3 decreases significantly, but it is higher than that of Figure 4a. The high value area is mainly concentrated on both ends of the western margin of the Sichuan Basin. One is in the northwestern part of Bazhong, the other is near Dujiangyan-Emeishan. It seems that the high value area extends northwest. Along the edge of the Sichuan Basin, the value between Bazhong and Emeishan decreases, and the value near Songpan recovers to the same level as that in Figure 4a.

Figure 4 The spatial distribution of the spectral areas. (a) The spatial distribution of the spectral area for May 16–31. (b) The spatial distribution of the spectral area of event 1. (c) The spatial distribution of the spectral area of event 2. (d) The spatial distribution of the spectral area of event 3. The black lines are faults: (1) Longriba Fault, (2) Minjiang Fault, (3) Huya Fault, (4) Tazang Fault, and (5) Longmenshan Fault.
Figure 4

The spatial distribution of the spectral areas. (a) The spatial distribution of the spectral area for May 16–31. (b) The spatial distribution of the spectral area of event 1. (c) The spatial distribution of the spectral area of event 2. (d) The spatial distribution of the spectral area of event 3. The black lines are faults: (1) Longriba Fault, (2) Minjiang Fault, (3) Huya Fault, (4) Tazang Fault, and (5) Longmenshan Fault.

Local geological factors may cause ambient noise local variation, in order to suppress the influence of this difference on the results. Herein, we took the spectral area of May 16–31 as the “normal value,” and subtract the normal value from the spectral area of event 1, event 2, and event 3, and the result is shown in Figure 5. Compared with Figures 4 and 5, it can be seen that the distribution region of high value has not changed substantially. It can be considered that the difference of local geological factors has not affected the results of this paper.

Figure 5 The spatial distribution of the spectral areas denomality. (a) The spatial distribution of the spectral area of event 1. (b) The spatial distribution of the spectral area of event 2. (c) The spatial distribution of the spectral area of event 3. The black lines are faults: (1) Longriba Fault, (2) Minjiang Fault, (3) Huya Fault, (4) Tazang Fault, and (5) Longmenshan Fault.
Figure 5

The spatial distribution of the spectral areas denomality. (a) The spatial distribution of the spectral area of event 1. (b) The spatial distribution of the spectral area of event 2. (c) The spatial distribution of the spectral area of event 3. The black lines are faults: (1) Longriba Fault, (2) Minjiang Fault, (3) Huya Fault, (4) Tazang Fault, and (5) Longmenshan Fault.

The temperatures, pressures, rainfall, and spectral areas of PLT station and TSS station were compared (Figure 6) for PLT stations. The correlation analysis shows that the correlation coefficients of the spectral area and meteorological factors (air temperature, air pressure, and rainfall) are 0.27, 0.24, and 0.16, respectively, for TSS station, they are 0.31, 0.26, and 0.17, respectively. Therefore, there was no obvious correlation between the increase in the spectral area and the meteorological factors in this study.

Figure 6 Comparison of the temperatures, pressures, rainfall, and spectral areas of PLT and TSS stations (May 1–August 20, 2017). (a, c, e, and g) Temperatures, pressures, rainfall, and spectral areas of PLT station. (b, d, f, and h) Temperatures, pressures, rainfall, and spectral areas of TSS station.
Figure 6

Comparison of the temperatures, pressures, rainfall, and spectral areas of PLT and TSS stations (May 1–August 20, 2017). (a, c, e, and g) Temperatures, pressures, rainfall, and spectral areas of PLT station. (b, d, f, and h) Temperatures, pressures, rainfall, and spectral areas of TSS station.

Several reports point out that the monsoon is a factor of ambient noise variation [8,9,10,11]. During this study period, there were the following four typhoons: “MERBOK,” “NANMADOL,” “TRLAS,” and “NORU” (http://www.typhone.org.cn). Herein, we focus on the relationship between NORU and spectral area. NORU is the strongest typhoon among these typhoons, which occurred from July 19 to August 9, 2017. We show the change in wind speed of NORU and spectral area of SPA and EMS stations in Figure 7. The correlation coefficients of wind speed and spectral area of SPA and EMS are 0.5 and 0.4, respectively. It can be seen that there was little correlation, while the correlation coefficient of the spectral area on two stations is 0.98. In addition, it can be seen that the peak of the spectral area appeared at July 30, whereas the peak of wind speed appeared at July 31. The spectral area recovered on August 2, but the typhoon remained at a high wind speed until August 7. However, we think that the triggering effect of typhoon to earthquake is worth further exploration.

Figure 7 Comparison of the wind speed and spectral areas of SPA and EMS stations.
Figure 7

Comparison of the wind speed and spectral areas of SPA and EMS stations.

4 Discussion

The spectrum area represents the energy state of the motion. These three events mean that they correspond to the intensification of the three low-frequency ground motions. As for the seismogenic faults of the Ms7.0 Jiuzhaigou earthquake, it is generally accepted that the earthquake occurred on the northward extension of the Huya Fault, which is a left-lateral slip fault [2,12]. The fault plane is nearly upright, and the earthquake has a rupture process extending upward from depth. The Minjiang Fault and the Huya Fault are the main faults on the western and eastern sides, respectively [1,2,3]. The distribution of the maximum shear strain rate field based on GPS observations in 2013–2016 shows that the southern segment of the Longmenshan Fault was one of the high value areas [5], which coincides with the peak area in Figure 4. Based on the seismographic imaging, magnetotelluric sounding, and aftershock locations, several studies have shown that the movement and physical property difference of the lower and middle crust constitutes the background of the earthquake [12,14]. The Longmenshan Fault system is the intersection of the Qinghai-Tibet block and the South China block. The spatial and temporal characteristics of the three high value ground motion processes that occurred before the earthquake indicate the following. The high values of the ground motion form an approximately U-shaped region in the study area, and the bottom of the U was parallel to the Longmenshan fault zone (Figure 4). We believe that this describes the following process, the eastward movement of the Bayan Hara block, which was obstructed by the rigid crust of the Sichuan Basin. The rheological material in the crust was extruded laterally, the U-shaped area may represent the extrusion process. Based on studies of the crustal flow and dynamic processes in this region, several scholars have pointed out that a diversion phenomenon occurred after the eastward movement of the middle and lower crustal flow was obstructed by the Sichuan Basin [3]. A study of the electrical structure of the region also shows that there is a 10–20 km deep, high conductivity layer between the Minjiang Fault and the Longmenshan Fault, and it shows rheological properties [14]. These are consistent with the results of this study.

Based on the gravity field data, several scholars have studied the 3D density structure and material movement of the Qinghai-Tibetan Plateau using the wavelet multi-scale analysis method. The results show the path and direction of the movement of low-density materials at a depth of 52 km [13]. Near the Emeishan, there was a diverging zone of the lateral extrusion of low-density materials. One branch flowed southward, and the other branch flowed northeastward along the Longmenshan Fault and into the Longmenshan branch again. One branch of the northeastern segment of the faults continues to migrate toward the northeast, whereas the other branch turns to the northwest.

The northeastern side of the U-shaped region (high value area) in Figure 8 is consistent with the location and direction of this low-density zone, which means that the high value area in this study mainly shows the movement of low-density materials within the crust. Therefore, we think that the dynamic background of the Jiuzhaigou earthquake was as follows. First, the eastern movement of the Qinghai-Tibetan block was obstructed by the rigid crust on the eastern side of the Huya Fault, and the energy for the earthquake gathered in the confined areas of the Longriba Fault, the East Kunlun Fault, and the Huya Fault. Second, the eastern movement of the Qinghai-Tibetan block was obstructed in the Sichuan Basin and was diverted (or extruded) at both ends of the Longmenshan Fault, forming a U-shaped movement path.

Figure 8 The low-density zones at a depth of 52 km. This figure is from reference [13]. The black arrow indicates the motion direction of the low-density material. The gray area indicates the high value area in this study.
Figure 8

The low-density zones at a depth of 52 km. This figure is from reference [13]. The black arrow indicates the motion direction of the low-density material. The gray area indicates the high value area in this study.

The results of this study also show that the extrusion at the two ends was not balanced, and the energy at the southwestern end was more concentrated or intense, which exerted an important effect on the enclosed areas of the Longriba Fault, the East Kunlun Fault, and the Huya fault. The other side of the U-shaped area (northeast) also had an impact on the occurrence of the earthquake, but the southeastern part of the high value area had a more direct role. This is a possible dynamic background for the formation and occurrence of this earthquake. At the very least, we believe that this effect accelerated the occurrence of the Jiuzhaigou earthquake, which coincides with the left-lateral slip mechanism of the earthquake [12].

5 Conclusion

Based on the above discussion, we believe that the high-value process was the reflection of the intense movement of the lower crustal material during the study period, which is related to the Ms7.0 Jiuzhaigou earthquake. These three events show the rapid eastward movement of the lower crustal material. After encountering the obstruction of the Sichuan Basin, the extruded material expanded northwest in the form of a U-shaped high-energy region. These violent movements may be related to the movement of rheological materials in the middle and lower crust. This result is also consistent with the research results of other scholars [1,2,3,12,13,14]. We believe that this was the main dynamic factor that caused or triggered the Ms7.0 Jiuzhaigou earthquake.

Acknowledgments

The seismic data were obtained from the Sichuan Seismic Network and the Gansu Seismic Network. Some of the figures were prepared using the Generic Mapping Tools (http://gmt.soest.hawaii.edu/projects/gmt/wiki/Download, last accessed June 2019). The MATLAB code developed by Vaishali Shrivastava was used for some of the calculations (https://ww2.mathworks.cn/matlabcentral/fileexchange/24597-area-under-a-curve, last accessed Sept. 2016). The authors thank LetPub (www.letpub.com) for its linguistic assistance during the preparation of this manuscript. The authors also thank the editors and reviewers for their comments on this manuscript.

  1. Author contributions: YL collected and collated the data. KSX developed the calculated code, performed the calculations, and prepared the manuscript with contributions from co-author.

References

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Received: 2019-11-06
Revised: 2020-07-14
Accepted: 2020-07-23
Published Online: 2020-09-29

© 2020 Kangsheng Xu and Ying Li, published by De Gruyter

This work is licensed under the Creative Commons Attribution 4.0 International License.

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  73. Accuracy and functional assessment of an original low-cost fibre-based inclinometer designed for structural monitoring
  74. The impacts of diagenetic facies on reservoir quality in tight sandstones
  75. Application of electrical resistivity imaging to detection of hidden geological structures in a single roadway
  76. Comparison between electrical resistivity tomography and tunnel seismic prediction 303 methods for detecting the water zone ahead of the tunnel face: A case study
  77. The genesis model of carbonate cementation in the tight oil reservoir: A case of Chang 6 oil layers of the Upper Triassic Yanchang Formation in the western Jiyuan area, Ordos Basin, China
  78. Disintegration characteristics in granite residual soil and their relationship with the collapsing gully in South China
  79. Analysis of surface deformation and driving forces in Lanzhou
  80. Geochemical characteristics of produced water from coalbed methane wells and its influence on productivity in Laochang Coalfield, China
  81. A combination of genetic inversion and seismic frequency attributes to delineate reservoir targets in offshore northern Orange Basin, South Africa
  82. Explore the application of high-resolution nighttime light remote sensing images in nighttime marine ship detection: A case study of LJ1-01 data
  83. DTM-based analysis of the spatial distribution of topolineaments
  84. Spatiotemporal variation and climatic response of water level of major lakes in China, Mongolia, and Russia
  85. The Cretaceous stratigraphy, Songliao Basin, Northeast China: Constrains from drillings and geophysics
  86. Canal of St. Bartholomew in Seča/Sezza: Social construction of the seascape
  87. A modelling resin material and its application in rock-failure study: Samples with two 3D internal fracture surfaces
  88. Utilization of marble piece wastes as base materials
  89. Slope stability evaluation using backpropagation neural networks and multivariate adaptive regression splines
  90. Rigidity of “Warsaw clay” from the Poznań Formation determined by in situ tests
  91. Numerical simulation for the effects of waves and grain size on deltaic processes and morphologies
  92. Impact of tourism activities on water pollution in the West Lake Basin (Hangzhou, China)
  93. Fracture characteristics from outcrops and its meaning to gas accumulation in the Jiyuan Basin, Henan Province, China
  94. Impact evaluation and driving type identification of human factors on rural human settlement environment: Taking Gansu Province, China as an example
  95. Identification of the spatial distributions, pollution levels, sources, and health risk of heavy metals in surface dusts from Korla, NW China
  96. Petrography and geochemistry of clastic sedimentary rocks as evidence for the provenance of the Jurassic stratum in the Daqingshan area
  97. Super-resolution reconstruction of a digital elevation model based on a deep residual network
  98. Seismic prediction of lithofacies heterogeneity in paleogene hetaoyuan shale play, Biyang depression, China
  99. Cultural landscape of the Gorica Hills in the nineteenth century: Franciscean land cadastre reports as the source for clarification of the classification of cultivable land types
  100. Analysis and prediction of LUCC change in Huang-Huai-Hai river basin
  101. Hydrochemical differences between river water and groundwater in Suzhou, Northern Anhui Province, China
  102. The relationship between heat flow and seismicity in global tectonically active zones
  103. Modeling of Landslide susceptibility in a part of Abay Basin, northwestern Ethiopia
  104. M-GAM method in function of tourism potential assessment: Case study of the Sokobanja basin in eastern Serbia
  105. Dehydration and stabilization of unconsolidated laminated lake sediments using gypsum for the preparation of thin sections
  106. Agriculture and land use in the North of Russia: Case study of Karelia and Yakutia
  107. Textural characteristics, mode of transportation and depositional environment of the Cretaceous sandstone in the Bredasdorp Basin, off the south coast of South Africa: Evidence from grain size analysis
  108. One-dimensional constrained inversion study of TEM and application in coal goafs’ detection
  109. The spatial distribution of retail outlets in Urumqi: The application of points of interest
  110. Aptian–Albian deposits of the Ait Ourir basin (High Atlas, Morocco): New additional data on their paleoenvironment, sedimentology, and palaeogeography
  111. Traditional agricultural landscapes in Uskopaljska valley (Bosnia and Herzegovina)
  112. A detection method for reservoir waterbodies vector data based on EGADS
  113. Modelling and mapping of the COVID-19 trajectory and pandemic paths at global scale: A geographer’s perspective
  114. Effect of organic maturity on shale gas genesis and pores development: A case study on marine shale in the upper Yangtze region, South China
  115. Gravel roundness quantitative analysis for sedimentary microfacies of fan delta deposition, Baikouquan Formation, Mahu Depression, Northwestern China
  116. Features of terraces and the incision rate along the lower reaches of the Yarlung Zangbo River east of Namche Barwa: Constraints on tectonic uplift
  117. Application of laser scanning technology for structure gauge measurement
  118. Calibration of the depth invariant algorithm to monitor the tidal action of Rabigh City at the Red Sea Coast, Saudi Arabia
  119. Evolution of the Bystrzyca River valley during Middle Pleistocene Interglacial (Sudetic Foreland, south-western Poland)
  120. A 3D numerical analysis of the compaction effects on the behavior of panel-type MSE walls
  121. Landscape dynamics at borderlands: analysing land use changes from Southern Slovenia
  122. Effects of oil viscosity on waterflooding: A case study of high water-cut sandstone oilfield in Kazakhstan
  123. Special Issue: Alkaline-Carbonatitic magmatism
  124. Carbonatites from the southern Brazilian Platform: A review. II: Isotopic evidences
  125. Review Article
  126. Technology and innovation: Changing concept of rural tourism – A systematic review
https://doi.org/10.1515/geo-2020-0184
Schlagwörter für diesen Artikel
Ms7.0 Jiuzhaigou earthquake; ground motion; FFT; amplitude spectrum; spectral area; dynamic process
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Artikel in diesem Heft

  1. Regular Articles
  2. The simulation approach to the interpretation of archival aerial photographs
  3. The application of137Cs and210Pbexmethods in soil erosion research of Titel loess plateau, Vojvodina, Northern Serbia
  4. Provenance and tectonic significance of the Zhongwunongshan Group from the Zhongwunongshan Structural Belt in China: insights from zircon geochronology
  5. Analysis, Assessment and Early Warning of Mudflow Disasters along the Shigatse Section of the China–Nepal Highway
  6. Sedimentary succession and recognition marks of lacustrine gravel beach-bars, a case study from the Qinghai Lake, China
  7. Predicting small water courses’ physico-chemical status from watershed characteristics with two multivariate statistical methods
  8. An Overview of the Carbonatites from the Indian Subcontinent
  9. A new statistical approach to the geochemical systematics of Italian alkaline igneous rocks
  10. The significance of karst areas in European national parks and geoparks
  11. Geochronology, trace elements and Hf isotopic geochemistry of zircons from Swat orthogneisses, Northern Pakistan
  12. Regional-scale drought monitor using synthesized index based on remote sensing in northeast China
  13. Application of combined electrical resistivity tomography and seismic reflection method to explore hidden active faults in Pingwu, Sichuan, China
  14. Impact of interpolation techniques on the accuracy of large-scale digital elevation model
  15. Natural and human-induced factors controlling the phreatic groundwater geochemistry of the Longgang River basin, South China
  16. Land use/land cover assessment as related to soil and irrigation water salinity over an oasis in arid environment
  17. Effect of tillage, slope, and rainfall on soil surface microtopography quantified by geostatistical and fractal indices during sheet erosion
  18. Validation of the number of tie vectors in post-processing using the method of frequency in a centric cube
  19. An integrated petrophysical-based wedge modeling and thin bed AVO analysis for improved reservoir characterization of Zhujiang Formation, Huizhou sub-basin, China: A case study
  20. A grain size auto-classification of Baikouquan Formation, Mahu Depression, Junggar Basin, China
  21. Dynamics of mid-channel bars in the Middle Vistula River in response to ferry crossing abutment construction
  22. Estimation of permeability and saturation based on imaginary component of complex resistivity spectra: A laboratory study
  23. Distribution characteristics of typical geological relics in the Western Sichuan Plateau
  24. Inconsistency distribution patterns of different remote sensing land-cover data from the perspective of ecological zoning
  25. A new methodological approach (QEMSCAN®) in the mineralogical study of Polish loess: Guidelines for further research
  26. Displacement and deformation study of engineering structures with the use of modern laser technologies
  27. Virtual resolution enhancement: A new enhancement tool for seismic data
  28. Aeromagnetic mapping of fault architecture along Lagos–Ore axis, southwestern Nigeria
  29. Deformation and failure mechanism of full seam chamber with extra-large section and its control technology
  30. Plastic failure zone characteristics and stability control technology of roadway in the fault area under non-uniformly high geostress: A case study from Yuandian Coal Mine in Northern Anhui Province, China
  31. Comparison of swarm intelligence algorithms for optimized band selection of hyperspectral remote sensing image
  32. Soil carbon stock and nutrient characteristics of Senna siamea grove in the semi-deciduous forest zone of Ghana
  33. Carbonatites from the Southern Brazilian platform: I
  34. Seismicity, focal mechanism, and stress tensor analysis of the Simav region, western Turkey
  35. Application of simulated annealing algorithm for 3D coordinate transformation problem solution
  36. Application of the terrestrial laser scanner in the monitoring of earth structures
  37. The Cretaceous igneous rocks in southeastern Guangxi and their implication for tectonic environment in southwestern South China Block
  38. Pore-scale gas–water flow in rock: Visualization experiment and simulation
  39. Assessment of surface parameters of VDW foundation piles using geodetic measurement techniques
  40. Spatial distribution and risk assessment of toxic metals in agricultural soils from endemic nasopharyngeal carcinoma region in South China
  41. An ABC-optimized fuzzy ELECTRE approach for assessing petroleum potential at the petroleum system level
  42. Microscopic mechanism of sandstone hydration in Yungang Grottoes, China
  43. Importance of traditional landscapes in Slovenia for conservation of endangered butterfly
  44. Landscape pattern and economic factors’ effect on prediction accuracy of cellular automata-Markov chain model on county scale
  45. The influence of river training on the location of erosion and accumulation zones (Kłodzko County, South West Poland)
  46. Multi-temporal survey of diaphragm wall with terrestrial laser scanning method
  47. Functionality and reliability of horizontal control net (Poland)
  48. Strata behavior and control strategy of backfilling collaborate with caving fully-mechanized mining
  49. The use of classical methods and neural networks in deformation studies of hydrotechnical objects
  50. Ice-crevasse sedimentation in the eastern part of the Głubczyce Plateau (S Poland) during the final stage of the Drenthian Glaciation
  51. Structure of end moraines and dynamics of the recession phase of the Warta Stadial ice sheet, Kłodawa Upland, Central Poland
  52. Mineralogy, mineral chemistry and thermobarometry of post-mineralization dykes of the Sungun Cu–Mo porphyry deposit (Northwest Iran)
  53. Main problems of the research on the Palaeolithic of Halych-Dnister region (Ukraine)
  54. Application of isometric transformation and robust estimation to compare the measurement results of steel pipe spools
  55. Hybrid machine learning hydrological model for flood forecast purpose
  56. Rainfall thresholds of shallow landslides in Wuyuan County of Jiangxi Province, China
  57. Dynamic simulation for the process of mining subsidence based on cellular automata model
  58. Developing large-scale international ecological networks based on least-cost path analysis – a case study of Altai mountains
  59. Seismic characteristics of polygonal fault systems in the Great South Basin, New Zealand
  60. New approach of clustering of late Pleni-Weichselian loess deposits (L1LL1) in Poland
  61. Implementation of virtual reference points in registering scanning images of tall structures
  62. Constraints of nonseismic geophysical data on the deep geological structure of the Benxi iron-ore district, Liaoning, China
  63. Mechanical analysis of basic roof fracture mechanism and feature in coal mining with partial gangue backfilling
  64. The violent ground motion before the Jiuzhaigou earthquake Ms7.0
  65. Landslide site delineation from geometric signatures derived with the Hilbert–Huang transform for cases in Southern Taiwan
  66. Hydrological process simulation in Manas River Basin using CMADS
  67. LA-ICP-MS U–Pb ages of detrital zircons from Middle Jurassic sedimentary rocks in southwestern Fujian: Sedimentary provenance and its geological significance
  68. Analysis of pore throat characteristics of tight sandstone reservoirs
  69. Effects of igneous intrusions on source rock in the early diagenetic stage: A case study on Beipiao Formation in Jinyang Basin, Northeast China
  70. Applying floodplain geomorphology to flood management (The Lower Vistula River upstream from Plock, Poland)
  71. Effect of photogrammetric RPAS flight parameters on plani-altimetric accuracy of DTM
  72. Morphodynamic conditions of heavy metal concentration in deposits of the Vistula River valley near Kępa Gostecka (central Poland)
  73. Accuracy and functional assessment of an original low-cost fibre-based inclinometer designed for structural monitoring
  74. The impacts of diagenetic facies on reservoir quality in tight sandstones
  75. Application of electrical resistivity imaging to detection of hidden geological structures in a single roadway
  76. Comparison between electrical resistivity tomography and tunnel seismic prediction 303 methods for detecting the water zone ahead of the tunnel face: A case study
  77. The genesis model of carbonate cementation in the tight oil reservoir: A case of Chang 6 oil layers of the Upper Triassic Yanchang Formation in the western Jiyuan area, Ordos Basin, China
  78. Disintegration characteristics in granite residual soil and their relationship with the collapsing gully in South China
  79. Analysis of surface deformation and driving forces in Lanzhou
  80. Geochemical characteristics of produced water from coalbed methane wells and its influence on productivity in Laochang Coalfield, China
  81. A combination of genetic inversion and seismic frequency attributes to delineate reservoir targets in offshore northern Orange Basin, South Africa
  82. Explore the application of high-resolution nighttime light remote sensing images in nighttime marine ship detection: A case study of LJ1-01 data
  83. DTM-based analysis of the spatial distribution of topolineaments
  84. Spatiotemporal variation and climatic response of water level of major lakes in China, Mongolia, and Russia
  85. The Cretaceous stratigraphy, Songliao Basin, Northeast China: Constrains from drillings and geophysics
  86. Canal of St. Bartholomew in Seča/Sezza: Social construction of the seascape
  87. A modelling resin material and its application in rock-failure study: Samples with two 3D internal fracture surfaces
  88. Utilization of marble piece wastes as base materials
  89. Slope stability evaluation using backpropagation neural networks and multivariate adaptive regression splines
  90. Rigidity of “Warsaw clay” from the Poznań Formation determined by in situ tests
  91. Numerical simulation for the effects of waves and grain size on deltaic processes and morphologies
  92. Impact of tourism activities on water pollution in the West Lake Basin (Hangzhou, China)
  93. Fracture characteristics from outcrops and its meaning to gas accumulation in the Jiyuan Basin, Henan Province, China
  94. Impact evaluation and driving type identification of human factors on rural human settlement environment: Taking Gansu Province, China as an example
  95. Identification of the spatial distributions, pollution levels, sources, and health risk of heavy metals in surface dusts from Korla, NW China
  96. Petrography and geochemistry of clastic sedimentary rocks as evidence for the provenance of the Jurassic stratum in the Daqingshan area
  97. Super-resolution reconstruction of a digital elevation model based on a deep residual network
  98. Seismic prediction of lithofacies heterogeneity in paleogene hetaoyuan shale play, Biyang depression, China
  99. Cultural landscape of the Gorica Hills in the nineteenth century: Franciscean land cadastre reports as the source for clarification of the classification of cultivable land types
  100. Analysis and prediction of LUCC change in Huang-Huai-Hai river basin
  101. Hydrochemical differences between river water and groundwater in Suzhou, Northern Anhui Province, China
  102. The relationship between heat flow and seismicity in global tectonically active zones
  103. Modeling of Landslide susceptibility in a part of Abay Basin, northwestern Ethiopia
  104. M-GAM method in function of tourism potential assessment: Case study of the Sokobanja basin in eastern Serbia
  105. Dehydration and stabilization of unconsolidated laminated lake sediments using gypsum for the preparation of thin sections
  106. Agriculture and land use in the North of Russia: Case study of Karelia and Yakutia
  107. Textural characteristics, mode of transportation and depositional environment of the Cretaceous sandstone in the Bredasdorp Basin, off the south coast of South Africa: Evidence from grain size analysis
  108. One-dimensional constrained inversion study of TEM and application in coal goafs’ detection
  109. The spatial distribution of retail outlets in Urumqi: The application of points of interest
  110. Aptian–Albian deposits of the Ait Ourir basin (High Atlas, Morocco): New additional data on their paleoenvironment, sedimentology, and palaeogeography
  111. Traditional agricultural landscapes in Uskopaljska valley (Bosnia and Herzegovina)
  112. A detection method for reservoir waterbodies vector data based on EGADS
  113. Modelling and mapping of the COVID-19 trajectory and pandemic paths at global scale: A geographer’s perspective
  114. Effect of organic maturity on shale gas genesis and pores development: A case study on marine shale in the upper Yangtze region, South China
  115. Gravel roundness quantitative analysis for sedimentary microfacies of fan delta deposition, Baikouquan Formation, Mahu Depression, Northwestern China
  116. Features of terraces and the incision rate along the lower reaches of the Yarlung Zangbo River east of Namche Barwa: Constraints on tectonic uplift
  117. Application of laser scanning technology for structure gauge measurement
  118. Calibration of the depth invariant algorithm to monitor the tidal action of Rabigh City at the Red Sea Coast, Saudi Arabia
  119. Evolution of the Bystrzyca River valley during Middle Pleistocene Interglacial (Sudetic Foreland, south-western Poland)
  120. A 3D numerical analysis of the compaction effects on the behavior of panel-type MSE walls
  121. Landscape dynamics at borderlands: analysing land use changes from Southern Slovenia
  122. Effects of oil viscosity on waterflooding: A case study of high water-cut sandstone oilfield in Kazakhstan
  123. Special Issue: Alkaline-Carbonatitic magmatism
  124. Carbonatites from the southern Brazilian Platform: A review. II: Isotopic evidences
  125. Review Article
  126. Technology and innovation: Changing concept of rural tourism – A systematic review
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