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Zircon U–Pb ages of the Paleozoic volcaniclastic strata in the Junggar Basin, NW China

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From the journal Open Geosciences Volume 16 Issue 1

Abstract

A large set of Paleozoic volcaniclastic rocks is exposed in the northwestern margin of the Junggar Basin from the southern part of the Central Asian Orogenic Belt. The Carboniferous volcaniclastic strata in this area have been studied in depth, and an accurate chronostratigraphic framework of these strata has been established. However, there is a lack of sufficient geochronological data for the deposition times of the other Paleozoic volcaniclastic strata. In this study, zircon U–Pb dating of the Ordovician, Silurian, and Devonian volcaniclastic strata in the area reveals that the youngest age of the tuffite sample collected from the originally defined Ordovician strata is 398 ± 11 Ma, which represents the age of volcanic activity during the period of tuffite deposition. Based on this finding, the originally defined Ordovician strata are redefined as the Lower Devonian. The youngest ages of the silty tuff samples collected from the originally defined Silurian strata peak are 445–418 Ma, so its age is Upper Silurian. The youngest ages of the tuffaceous sandstone samples collected from the originally defined Devonian strata peak are 346–342 Ma, so these Devonian are redefined as the Early Carboniferous strata. Two Archean ages (2,501 ± 12 and 3,193 ± 8 Ma) were obtained in Silurian strata, thus confirming the existence of metamorphic rock basement in the provenance areas from which the sediments were derived.

Keywords: Junggar Basin; Paleozoic; pyroclastic rock; zircon U–Pb dating

1 Introduction

The Central Asian Orogenic Belt is the largest Phanerozoic accretionary orogenic and continental metallogenic belt in the world and consists of an immense and complex collage of accreted terranes [1,2,3,4,5,6]. The northwestern margin of the Junggar is located in the southern part of the Central Asian Orogenic Belt, forming an important component of the Central Asian Orogenic Belt. The Northwest of Junggar underwent a transition from the tectonic processes of seafloor spreading and subduction to arc–arc collision and post-collisional extension during the Early Cambrian-Early Devonian [7]. The ocean was formed by the mid-ocean ridge spreading at ca. 512–478 Ma and subduction initiation at ca. 476–467 Ma and developed a transitional oceanic arc at ca. 456–452 Ma [8].

The northwestern margin of the Junggar Basin has developed a large range of Paleozoic composed of mostly clastic and volcaniclastic rocks with rare fossils (Figure 1). The development of folds and faults in this region has disrupted the relationship between strata. Moreover, post-sedimentation tectonics makes it impossible to obtain the stratigraphic section of some strata [9]. Furthermore, it is found that some fossils are re-deposited to other strata [10]. The stratigraphic chronology of this area is based on biostratigraphy and is still in use. However, the confusion of fossil sequences indicates that this evidence is defective and needs to be corrected by Chronology data.

Figure 1 Geological sketch map of West Junggar (modified after [11]).
Figure 1

Geological sketch map of West Junggar (modified after [11]).

Fortunately, a large number of volcaniclastic rocks distributed in the Paleozoic strata provide a basis for geochronological research. In recent years, with the development of zircon dating technology, many scholars have dated the volcanic rocks in the Carboniferous-Permian strata in the study area and established a geochronological framework for each Carboniferous formation as well as some Permian strata [12,13,14,15,16]. This framework greatly promoted research on the tectonic evolution of this area during the Carboniferous and Permian. However, an accurate geochronological framework is still needed for the early Paleozoic strata, which are widely exposed in the area. Zhang et al. [15] also noted that the intermediate–basic volcanic rock strata of the Middle Devonian must be further determined, which limits the further understanding of the tectonic evolution of this area. Therefore, in this study, I collected volcaniclastic samples from the Paleozoic strata and corrected the stratigraphic age accordingly.

2 Regional geology

The West Junggar area is located between the Altai and Tianshan tectonic belts in the central and southern Central Asian Orogenic Belt. This area has developed a set of NE-SW-trending strike-slip faults, including the Darlbute, Tuoli, Barleik, and Dongbielieke faults (Figure 1).

The magmatic activity of the Paleozoic in the northwest of the Junggar basin is very strong. A wide range of Paleozoic strata are exposed, and volcaniclastic rocks are widely developed. The volcanic rock belt was formed in the evolution stage of the closed ocean-continent pattern of the Junggar Ocean in the Paleozoic and is mainly alkaline and calcalkaline series [17].

The Ordovician system is mainly composed of the Labahe Formation and the Kekeshayi Formation (Figure 2). The upper part of the Labahe Formation is composed of siltstone, argillaceous, silty tuff, and felsophyre, and the lower part of the Labahe Formation is composed of biotite-quartz schist intercalated with a small amount of quartzite. The Kekeshayi Formation is mainly composed of volcaniclastic rocks. Specifically, its upper section is composed of tuff, tuff breccia, and lithic–crystal tuff, and its lower section is composed of andesite, basalt, and tuff lava intercalated with siliceous rock. The Silurian system includes the Qiaergaye Formation and the Mayile Formation, which are mainly composed of tuffaceous siltstone, siliceous slate, and andesitic porphyrite. The Devonian system includes the Kulumudi Formation (or the Sawuershan Formation), the Baerluke Formation, and the Tielieketi Formation, with an outcropping thickness exceeding 6,000 m. The upper section of the Kulumudi Formation is mainly composed of tuff intercalated with andesitic porphyrite and glutenite, and its lower section is mainly composed of tuffaceous siltstone with a small amount of basal conglomerate at the bottom.

Figure 2 Column of Ordovician-Lower Carboniferous sequences of West Junggar.
Figure 2

Column of Ordovician-Lower Carboniferous sequences of West Junggar.

The upper section of the Baerluke Formation is interbedded with gray-grayish green crystalline clastic tuff and calcareous siltstone intercalated with felsophyric lens, the middle section of the Baerluke Formation is interbedded with grayish-green crystal–lithic breccial tuff and tuffaceous siltstone, and the lower section of the Baerluke Formation is composed of lithic-crystal tuff intercalated with tuffaceous siltstone. The Tielieketi Formation is composed of plagioclase porphyritic tuff and tuffaceous siltstone in the upper section, calcareous sandstone in the middle section, and conglomerate in the lower section. Therefore, it can be seen that there are many volcanic rocks in the strata of each era, and they provide a basis for our geochronological study (Figure 2).

In addition, the study area has been intensively intruded by late Carboniferous granite and diorite [18,19], which have an emplacement age between 310 and 290 Ma and are considered the products of post-collisional plutonic magmatism [18,20,21,22].

3 Petrological characteristics

In this study, samples were collected from the Ordovician Labahe Formation (sample 19-6) and the Lower Silurian Qiaergaye Formation (sample 19-9) in the southern segment of the Darlbute fault and the Upper Devonian Tielieketi Formation (sample 16-3A) in the western Tuoli Basin. The sampling location is shown in Figure 1. The sample 19-6 is grayish-purple fine-grained tuff intercalated with grayish-green fine-grained silty tuff and with a massive structure (Figure 3a). The tuff contains a large amount of fibrous and needle-like quartz crystal fragments (Figure 3b), the grain clast is mainly subangular quartz and lithic fragments with grain sizes of approximately 0.1 mm, and the interstitial material is mostly volcanic ash, which contains fibrous crystal fragments (Figure 3c).

Figure 3 Field photos and microphotographs of samples: (a–c) sample 19-6; (d–g) sample 16-3A; and (h–j) sample 19-9.
Figure 3

Field photos and microphotographs of samples: (a–c) sample 19-6; (d–g) sample 16-3A; and (h–j) sample 19-9.

The sample (16-3A) collected from the Upper Devonian Tielieketi Formation is a medium-grained tuffaceous sandstone (Figure 3d). The grain clast is mainly composed of angular–subangular quartz with poor roundness (Figure 3e), followed by plagioclase that contains sickle-shaped, fishhook-like, and needle-like crystal fragments (Figure 3e–g).

The sample collected from the Lower Silurian Qiaergaye Formation (19-9) is purplish-red medium-thick layered silty tuff (Figure 3h) containing needle-like and fibrous crystal fragments (Figure 3i). The interstitial material is volcanic ash. In addition, a quartz vein intrusion occurred during the post-tectonic phase (Figure 3g).

4 Methods

After the zircon samples were sorted using artificial heavy sand, heavy liquid, and an electromagnetic apparatus, the impurities were removed under a binocular microscope. Then, the colorless, transparent, crack-free, and inclusion-free zircon grains were sorted and glued onto epoxy resin with standard zircon grains (Qinghu), smoothed and polished with sandpaper to expose 1/3–1/2 of the zircon grains, optically analyzed (transmitted and reflected light) under a microscope, and coated with gold for cathodoluminescence (CL) microscopic imaging and in situ U‒Pb isotope analyses of the zircon microdomains were undertaken.

U–Pb dating and trace element analyses of zircons were accomplished synchronously by Laser Ablation Inductively Coupled Plasma Mass Spectrometer (LA-ICP-MS) at the Key Laboratory of Continental Collision and Plateau Uplift, Institute of Tibetan Plateau Research, Chinese Academy of Sciences. The NewWave and 193 nm ArF Excimer laser ablation system (Model: UP193FX) produced by ATL are used for laser sampling, which is characterized by short pulse width (<4 ns) and spot sizes 35 μm. Element and isotope ion-signal intensities were acquired by Inductively Coupled Plasma Mass Spectrometer (ICP-MS) instrument, model 7500a, produced by AGL. Both high-purity Helium and Argon gases were used as carrier gas, which were mixed via a T-connector before entering the Inductively Coupled Plasma. Helium gas was controlled by a mass flow controller, which is installed into the Laser system. Argon gas was controlled by the ICP-MS. Helium and argon carrier gas flows were optimized by ablating NIST SRM 612 (a silicate glass reference material produced by the National Institute of Standards and Technology) to obtain maximum signal intensity for 238U and 208Pb, minimum oxide and double-charge interference, minimum gas blank, and most stable signal intensity. In the conditions of 100 μm spot size, 15 Hz repetition rate, ∼8 J/cm2 fluence, 1.6 GW/cm2 irradiance, ICP-MS could acquire these results: 6 × 104 cps/ppm 238U and 2.5 × 104 cps/ppm 208Pb signal intensities, <0.3% ThO/Th ratios, <100 cps 204Pb gas blank, and <3% RSD for most elements (Rare Earth Element, U, Th, Pb) by ablating the NIST SRM 612 by the line-ablation mode. Each analysis incorporated with ∼15–20 s gas blank acquisition (warm up), 40 s data acquisition from the sample aerosol (ablation), and 45–55 s washout time by the spot sampling mode of the laser system and Time Resolved Analysis data acquisition mode of the Agilent Chemstation. Plesovice and SL natural zircon references were used as an external standard for the matrix-matched calibration of U–Pb dating. NIST SRM 612 reference glasses were analyzed as an external standard for the trace element content calibration. A Plesovice, a Qinghu, and a NIST SRM 612 were analyzed followed by 5–10 sample analyses. Off-line isotope ratios and trace element concentrations were calculated by GLITTER_Ver4.0 [23]; Common Pb correction and ages of the samples were calibrated and calculated using ComPbCorr#3.17 [24]; U–Pb concordia diagrams, weighted mean calculations and probability density plots of U–Pb ages were made using Isoplot/Ex_ver 3 [25]. The accuracy of selection criteria of concordance is 90–110%.

5 Results

Dickinson and Gehrels [26] proposed several methods to determine and constrain the maximum depositional ages, such as youngest single grain age (YSG), youngest graphical age peak (YPP), mean age of the youngest two or more grains that overlap in age at 1σ (YC1σ, youngest 1σ grain cluster), and YC2σ (youngest 2σ grain cluster). It should be noted that although Dickinson and Gehrels [26] confirmed that YPP is less likely congruent with depositional age, but if the level of incompatibility is acceptable, YPP is in all cases a reliable measure of youngest age. And YC1σ appears to be as reliable a measure of youngest age as YPP for even fewer samples. In this article, the YSG and the youngest age group are used to constrain the latest time of deposition of the strata.

5.1 Zircon dating of the Labahe Formation (19-6)

A total of 40 zircon grains were selected from sample 19-6 for testing (Appendix). Most of the zircon grains were euhedral or subhedral with a long or short columnar shape, clear crystal edges and planes, a complete crystal form, and discernible cylindrical and conical surfaces, which indicate that they are typical magmatic zircon grains. The CL images of the zircon grains (Figure 4) show that most of them have a typical oscillating zonal structure with a particle size of 80–150 μm and a length-to-width ratio between 1:1 and 1:3. All of the zircon grains are translucent or subtranslucent, and most have no small inclusions or internal cracks, while some contain small inclusions. The CL images show that most of the zircon grains had magmatic oscillation zones and that a few well-rounded zircon grains had developed growth edges.

Figure 4 The CL images and U–Pb ages (Ma) of zircon domains for the sample 19-6.
Figure 4

The CL images and U–Pb ages (Ma) of zircon domains for the sample 19-6.

Previous studies have demonstrated that zircons of different origins have different Th and U contents and Th/U ratios, zircon with Th/U values of <0.1 is most probably of metamorphic origin, whereas the origin of zircon with Th/U value of >0.1 needs to be determined by combining other tools, such as zircon inner structure [27,28]. The Th/U ratios of the zircon grains in sample 19-6 are in the range of 0.28–0.90, and the zircon grains show good crystal morphology and clear oscillatory zoning, which are consistent with the characteristics of magmatic zircon. The ages of the zircon grains were all distributed on the concordant line with a high degree of concordance; the distribution of their apparent ages is relatively concentrated with 206Pb/238U ages in the range of 398–513 Ma (concentrated in the range of 425–460 Ma) (Figure 5).

Figure 5 Concordia diagram and histogram of detrital zircon U–Pb ages of the samples.
Figure 5

Concordia diagram and histogram of detrital zircon U–Pb ages of the samples.

The zircon grains in sample 19-6 are almost all angular, which indicates that they have not undergone long-distance transportation and rounding. The petrographic thin sections reveal many tuffaceous components in the rocks and the volcanic ash interstitial material, which indicates that the magmatic zircon grains are mainly of volcanic origin. The zircon age of the primary magma in the volcanic ash can represent the strata deposition time.

There are two distinct age peaks of 426–425 Ma (No. 1, 5, 6, 8, 9 in Figure 4) and 441–439 Ma (3, 10, 12, 13, 26, 32, 33 in Figure 4) in 19-6. The zircon grains with ages of 426–425 Ma have a complete crystal structure and basically no breakage in appearance, slightly rounded compared to No. 2, Th/U ratios are all greater than 0.4, all have magmatic oscillation zones, No. 5, 8, and 9 have narrow bright metamorphic edges. In the group of 441–439 Ma, No. 10 is slightly rounded with the narrow metamorphic edge and No. 33 is moderately rounded with wider metamorphic edge. The roundness of zircons indicates that they have all undergone transportation and not directly deposited from volcanic ash. The lithology of this sample is tuff, and zircons from the directly deposited volcanic ash can represent the stratigraphic age. Moreover, the metamorphic edges in these two groups indicate that they have undergone later tectonic-thermal events. So both groups of 426–425 and 441–439 Ma are not sufficient to represent the latest age of the formation.

The youngest zircon grain is No. 2 (in Figure 4), with an age of 398 ± 11 Ma. The complete crystal structure and poor roundness indicate that it has not been transported over long distances. The CL image shows a distinct magmatic oscillation zone without metamorphic edges, and the Th/U ratio is 0.48, indicating magmatic origin. Therefore, the No. 2 (398 ± 11 Ma) should be a product of volcanic eruption at the same time as the formation, which can represent the sedimentary time of the strata.

5.2 Zircon dating of the Tielieketi Formation (16-3A)

Microscopic thin-section observation demonstrated that sample 16-3A has many tuffaceous components and that the interstitial material is volcanic ash, which indicates that the sample’s magmatic zircon grains were mainly from volcanic components.

A total of 88 zircon grains were selected from sample 16-3A (Tielieketi Formation). They had grain sizes of approximately 100–150 μm, mostly euhedral and subhedral long or short columnar shapes, clear crystal edges and planes, a complete crystal form, and discernible cylindrical and conical surfaces (Figure 6); all the grains lack roundness, which may indicate that the zircon grains in the rock originated mainly from magma and have not undergone long-distance transportation. The length-to-width ratio of the crystal is approximately 1:1.5–1:2. All of the zircon grains are translucent or subtranslucent, and only a few zircon grains have internal cracks or small inclusions. The CL images show that the zircon grains mostly have evident magmatic oscillation zones and alternating light and dark bands and three zircon grains (No. 27, 37, and 41 in Figure 6) have a core-mantle structure with narrow metamorphic edges, which is excluded from determining stratigraphic age.

Figure 6 The CL images and U–Pb ages (Ma) of zircon domains for the sample 16-3A in Tielieketi Formation.
Figure 6

The CL images and U–Pb ages (Ma) of zircon domains for the sample 16-3A in Tielieketi Formation.

The Th/U ratios of the zircon grains in sample 16-3A range from 0.35 to 1.10, only 2 grains (No. 55 and 90) are less than 0.4, and other 86 zircon grains are greater than 0.4. Since most zircon grains (exclude No. 27, 37, and 41) have the typical magmatic oscillation zone, it can be determined that these zircon grains are of magmatic origin and can be used to investigate the depositional period of the volcaniclastic rocks and the duration of the magmatism in the provenance area.

The apparent ages of the zircon grains in sample 16-3A indicate a relatively concentrated distribution, and all of them are distributed on the concordant line, which indicates a high degree of concordance. The ages of most of the zircon grains are distributed between 334 and 404 Ma, including 30% (26) in the early Carboniferous, 67% (58) in the range of 359–385 Ma (the Late Devonian), 2% (2) in the Middle Devonian, and 1% (1) in the Early Devonian. The two distinct peaks are 360–364 Ma (3, 18, 24, 28, 32, 36, 38, 59, 66, 71, 74, 80, 86) and 370–374 Ma (8, 10, 15, 16, 17, 20, 25, 46, 53, 58, 64, 68,72, 76, 78, 81), and the two lower peaks are 342–346 Ma (4, 29, 37, 39, 41, 73, 79) and 350–352 Ma (33, 40, 44, 57, 75, 82, 87, 88), indicating that the volcaniclastic rocks of the Tielieketi Formation have complex provenance.

The No. 55 zircon grain in sample 16-3A has the youngest age (314 ± 16 Ma), which is close to the bottom of the Late Carboniferous and is significantly younger than the other grains in the sample, its CL image shows a complex internal structure with inclusions, and the Th/U ratios is less than 0.4, which is likely due to the affected by intermediate-acid intrusive rocks developed in the same period [21]. The second youngest grain is No. 90 (334 + 12 Ma), with a complex internal structure and growth edge, which may be affected by later thermal events and should not be used to limit the age of the formation. Therefore, the No. 55 and 90 zircon grains are ignored during the analysis of the strata deposition time.

Excluding these two grains, the youngest group is 342–346 Ma (No. 4, 29, 37, 39, 41, 73, 79). The internal structures of 39 and 73 are complex, so they were excluded. The remaining five (No. 4, 29, 37, 41, 79) have simple internal structures, obvious magma bands, and no growth edges, indicating that they have not been disturbed by later thermal events, which can be used to determine the latest age of the strata. Therefore, the sedimentary age of this layer should not be earlier than the Visean of the Lower Carboniferous.

5.3 Zircon dating of the Qiaergaye Formation (sample 19-9)

Only a small amount of zircon was selected from the sample 19-9 (Qiaergaye Formation), a total of 31 zircon grains were tested. The zircon grains in this sample were heterogeneous in particle size and could be clearly divided into two groups based on the degree of euhedrality. The group of zircon grains is nearly equigranular with a low degree of euhedrality (No. 1, 3, 4, 5, 6, 12, 19, 21, 22, 25, 28, 30, 32, 34, 36 in Figure 7), with the size of approximately 50–75 μm, high roundness, an incomplete crystal form, a length-to-width ratio of approximately 1:1–1:1.2, a dark gray color, growth edges and indiscernible bands (in most zircon grains) on the CL images, and Th/U ratios less than 0.4. Therefore, the zircon grains in the low-euhedrality group are metamorphic zircon grains, and most of the apparent ages are greater than 900 Ma (except No. 3 and 34). The other group of zircon grains (No. 2, 8, 9, 10, 13, 15, 16, 17, 18, 20, 23, 24, 26, 29, 33, 35 in Figure 7) with a high degree of euhedrality has a grain size of approximately 75–100 μm, an angular shape, clear crystal edges and planes, a complete crystal form, a crystal length-to-width ratio of approximately 1:1–1:1.5, clear magmatic oscillation zones, no growth edge on the CL images (Figure 7), and Th/U ratios all exceeding 0.4. Therefore, the zircon grains in the high-euhedrality group are magmatic.

Figure 7 The CL images and U–Pb ages (Ma) of zircon domains for the sample 19-9 in Qiaergaye Formation.
Figure 7

The CL images and U–Pb ages (Ma) of zircon domains for the sample 19-9 in Qiaergaye Formation.

The zircon grains in sample 19-9 show a relatively scattered apparent age distribution and a high degree of concordance. The youngest zircon grain had an age of 306 ± 2 Ma (No. 34), showing a dark gray on the CL image, which is likely due to the influence of post-tectonic magmatism. Therefore, this zircon grain was ignored during the analysis of the strata deposition time. The ages of the remaining zircon grains show two peaks (which are basically consistent with the morphological grouping of the zircon grains): a maximum age peak between 418 and 445 Ma (No. 8, 13, 15, 16, 17, 18, 24, 26, 35). These zircon grains are all angular and have magmatic oscillation zones and Th/U ratio exceeding 0.4 with obvious characteristics of magmatic zircon. Therefore, the deposition age of this formation should not be earlier than 418 Ma. Since Middle and Upper Devonian zircon grains are found in large quantities in the neighboring Carboniferous system (16-3A) but are missing in this sample, it can be reasonably inferred that the deposition time of the Qiaergaye Formation is most likely the Early Devonian.

The second peak is between approximately 900 and 1,200 Ma and involves 7 zircon grains (No. 1, 4, 5, 6, 19, 28, 32). These zircon grains have an incomplete crystal form, good roundness, a dark gray, no magmatic oscillation zones on the CL images, and Th/U ratios are all less than 0.4. Therefore, they are metamorphic.

Sample 19-9 contains a large amount of pyroclastic components, among which the youngest group has a peak value of 418–445 Ma, with clear magmatic oscillation zones and their Th/U ratio are all greater than 0.4, indicating the origin of magmatic rocks. Moreover, these particles are angular, indicating that they were deposited in situ. Therefore, they were directly deposited after volcanic eruption, so it can be judged that the sedimentary time of the stratum is Late Silurian.

The two oldest zircon grains in the sample 19-9 have ages of 2,501 ± 12 and 3,193 ± 8 Ma (No. 25 and 21) and are not on the concordia line, with high roundness, and growth zoning, which indicates that they may be of metamorphic origin and may have experienced lead loss incidents. Previous studies have found that there are Archean (mostly Neoarchean) continental crustal materials in this area [29,30], and the oldest zircon ages found were 3,073 ± 10 Ma [31] and 3,022 ± 11 Ma [32]. The zircon ages of 3,193 ± 8 Ma found in this study indicate that the basement age in this area is more ancient.

Sample 19-9 (S4) contains many Precambrian zircon grains, indicating that Archean and Proterozoic basement terranes were exposed in the northwestern of the Junggar during Late Silurian.

6 Discussion and preliminary conclusion

Sample 16-3A was collected from the Tielieketi Formation in Lower Devonian. After excluding the influence of post-tectonic magmatism, the age of the youngest grains is 346–342 Ma, which may represent the eruption time of the volcaniclastics. Therefore, this formation should be dated in the Visean stage, Early Carboniferous rather than the Devonian. The zircon U–Pb age statistics shows that the sample 16-3A is mainly between 334 and 404 Ma. Correspondingly, the zircon age of rhyolite in the northeast of the Junggar Basin is 395 ± 3 and 387 ± 8 Ma [33], Hatu granite is 347 ± 4 Ma [34], and the Darlbut ophiolite is 391 Ma [35]. These magmatic rocks are all in the east of 16-3A, perhaps it can indicate that the material source was from the east in Early Carboniferous.

Sample 19-6 was collected from the Labahe Formation in Ordovician, but the youngest zircon grain is 398 Ma, and the age of the young grains should represent the eruption time of the volcanic rocks. Therefore, this formation should be dated to the Lower Devonian rather than the Ordovician. The age distribution of samples 19-6 ranges from 513 to 398 Ma, mainly from 460 to 425 Ma. Early Paleozoic ophiolites are distributed in the east of Junggar Basin, which partially extended to Devonian (523–397 Ma) [36], and should be the source of sample 19-6.

Sample 19-9 was collected from the Qiaergaye Formation in Lower Silurian. Excluding the influence of late magmatism, the peak age of the youngest zircon grains is 418–445 Ma. Therefore, it is reasonable to infer that the deposition time of this formation is most likely the late Silurian rather than the early Silurian. The sample 19-9 ranges from 3,193 to 418 Ma, mainly between 540 and 418 Ma, indicating that its provenance is complex. Previous studies have shown that there may be an ancient Precambrian crystalline basement in Junggar area. This study has obtained two Archean ages (2,501 ± 12 and 3,193 ± 8 Ma), which confirms this point, and 3,193 ± 8 Ma is the oldest age data found in this area at present.

Samples 19-6 (D1) and 19-9 (S4) are very close in position, and the oldest grain age in sample 19-6 is 513 ± 7 Ma; it lacks grains before Cambrian compared to sample 19-9, indicating that the Cambrian and previous old strata may have been denuded completely during the Carboniferous period.

A large amount of zircon Chronology has proved that the convergence of the Neoarchean Supercontinent mainly occurred at 2.7–2.5 Ga, with the peak age of 2.7Ga [37]. However, there is a lack of ancient crustal materials in the Junggar area, and only the Proterozoic strata are exposed in the south of Tianshan Mountains; Zhu et al. [29] have confirmed that there are a large number of Paleoproterozoic Neoarchean (2,536–1,883 Ma) magmatic zircons in the Cambrian pillow basalt in the Junngar area, which confirmed the existence of ancient Continental crust materials. The 3,193 ± 8 Ma zircon discovered in this article is very close to Paleoarchean, indicating that the basement age is older than previously thought.

Acknowledgments

This research was financially supported by the China Natural Science Foundation (41772220). The author thanks Dr. Yue Yahui from the State Key Laboratory of Tibetan Plateau Earth System, Environment and Resources (TPESER), Institute of Tibetan Plateau Research, Chinese Academy of Sciences, for her assistance in the sample testing and data processing.

  1. Conflict of interest: Author states no conflict of interest.

  2. Data availability statement: The datasets generated during and/or analysed during the current study are available from the corresponding author on reasonable request.

Appendix
Table A1

LA-ICP-MS zircon U–Pb analytical data for the samples

Spot no. 204Pb corrected ratio Calculated apparent age (Ma)
Th/U 207Pb/206Pb 207Pb/235U 206Pb/238U 207Pb/206Pb 207Pb/235U 206Pb/238U
Age ±1б Age ±1б Age ±1б
19-6-001 0.52 0.05538 0.51995 0.0681 428 99 425 19 425 6
19-6-002 0.48 0.05516 0.48471 0.06374 419 277 401 49 398 11
19-6-003 0.57 0.05573 0.54352 0.07075 442 103 441 21 441 7
19-6-004 0.59 0.05578 0.5557 0.07226 444 154 449 31 450 10
19-6-005 0.50 0.05554 0.52282 0.06828 434 180 427 34 426 9
19-6-006 0.60 0.05545 0.52097 0.06815 430 80 426 16 425 5
19-6-007 0.62 0.05646 0.58669 0.07538 471 59 469 13 468 5
19-6-008 0.44 0.05533 0.52098 0.0683 426 159 426 31 426 9
19-6-009 0.67 0.05535 0.52139 0.06833 426 99 426 20 426 6
19-6-010 0.59 0.05545 0.53275 0.06969 430 129 434 25 434 7
19-6-011 0.31 0.05755 0.65762 0.08289 513 97 513 22 513 7
19-6-012 0.54 0.05522 0.5344 0.0702 421 134 435 27 437 8
19-6-013 0.50 0.05557 0.53553 0.0699 435 105 435 21 436 6
19-6-014 0.47 0.05602 0.56728 0.07345 453 118 456 25 457 8
19-6-015 0.66 0.05604 0.56629 0.0733 454 113 456 23 456 7
19-6-016 0.68 0.05575 0.56566 0.0736 442 65 455 14 458 5
19-6-017 0.34 0.0564 0.58074 0.07468 468 69 465 15 464 5
19-6-018 0.77 0.05579 0.54835 0.07129 444 171 444 34 444 9
19-6-019 0.38 0.05592 0.57065 0.07402 449 118 458 25 460 8
19-6-020 0.41 0.05686 0.61744 0.07877 486 82 488 18 489 6
19-6-021 0.66 0.05592 0.55844 0.07244 449 100 451 20 451 6
19-6-022 0.41 0.05723 0.64218 0.08139 500 119 504 27 504 9
19-6-023 0.28 0.05647 0.61107 0.07849 471 110 484 24 487 7
19-6-024 0.47 0.05686 0.61013 0.07783 486 82 484 18 483 6
19-6-025 0.64 0.05552 0.54574 0.0713 433 98 442 20 444 6
19-6-026 0.48 0.05332 0.51578 0.07017 342 105 422 20 437 7
19-6-027 0.44 0.05594 0.55869 0.07244 450 187 451 36 451 9
19-6-028 0.39 0.0558 0.55669 0.07236 444 109 449 22 450 6
19-6-029 0.90 0.05568 0.55208 0.07192 440 85 446 18 448 6
19-6-030 0.34 0.05613 0.58589 0.07572 458 90 468 19 471 6
19-6-031 0.45 0.05565 0.54754 0.07137 438 140 443 28 444 9
19-6-032 0.40 0.05573 0.53711 0.06991 442 208 437 41 436 11
19-6-033 0.48 0.05535 0.5381 0.07051 426 77 437 16 439 5
19-6-034 0.48 0.05582 0.5492 0.07136 445 155 444 31 444 9
19-6-035 0.47 0.05568 0.54168 0.07057 440 117 440 23 440 7
19-6-036 0.34 0.05716 0.62621 0.07946 498 102 494 23 493 7
19-6-037 0.44 0.05681 0.61369 0.07835 484 107 486 24 486 8
19-6-038 0.73 0.05633 0.5663 0.07292 465 138 456 28 454 9
19-6-039 0.53 0.05599 0.56958 0.07378 452 134 458 27 459 8
19-6-040 0.36 0.05615 0.56831 0.07341 458 111 457 23 457 7
16-3A-001 0.35 0.05344 0.36772 0.04991 358 117 357 19 356 5
16-3A-002 0.36 0.05455 0.39972 0.05315 373 110 369 19 369 5
16-3A-003 0.40 0.05371 0.44086 0.05955 360 80 363 14 364 4
16-3A-004 0.42 0.05409 0.43429 0.05824 329 162 344 26 346 8
16-3A-005 0.43 0.05396 0.44325 0.05958 371 142 383 25 385 7
16-3A-006 0.43 0.05373 0.43716 0.05901 386 261 371 45 369 12
16-3A-007 0.45 0.05356 0.43941 0.0595 361 111 367 19 368 5
16-3A-008 0.45 0.05369 0.42215 0.05703 359 197 371 34 373 9
16-3A-009 0.45 0.05427 0.45083 0.06026 381 143 379 25 379 7
16-3A-010 0.46 0.05345 0.40356 0.05476 371 168 371 29 371 8
16-3A-011 0.47 0.05371 0.41359 0.05585 357 127 357 21 357 6
16-3A-012 0.48 0.05341 0.41163 0.0559 364 116 369 20 369 6
16-3A-013 0.49 0.05417 0.43074 0.05768 382 145 385 26 386 7
16-3A-014 0.52 0.05301 0.4033 0.05519 358 100 359 17 359 5
16-3A-015 0.52 0.05417 0.4399 0.0589 351 99 367 17 370 5
16-3A-016 0.53 0.05367 0.41209 0.0557 388 115 374 20 372 6
16-3A-017 0.53 0.05376 0.41461 0.05594 377 93 374 16 373 5
16-3A-018 0.53 0.05341 0.40171 0.05455 380 186 364 29 362 6
16-3A-019 0.53 0.05348 0.41165 0.05583 380 149 371 26 369 7
16-3A-020 0.54 0.05394 0.42803 0.05757 353 134 370 23 373 7
16-3A-021 0.54 0.05358 0.42596 0.05766 357 138 350 22 349 6
16-3A-022 0.55 0.05399 0.43633 0.05861 375 115 366 19 365 6
16-3A-023 0.55 0.0541 0.44481 0.05964 345 112 365 19 368 6
16-3A-024 0.56 0.05395 0.43221 0.05811 378 160 364 27 362 7
16-3A-025 0.57 0.05487 0.48938 0.06469 376 91 372 16 372 5
16-3A-026 0.58 0.05417 0.44234 0.05922 388 83 380 15 378 5
16-3A-027 0.58 0.05359 0.43633 0.05905 405 328 397 59 395 15
16-3A-028 0.58 0.05332 0.4257 0.05791 369 110 362 18 361 5
16-3A-029 0.58 0.054 0.45765 0.06149 369 152 348 24 345 7
16-3A-030 0.59 0.05437 0.44154 0.05892 352 226 355 37 356 10
16-3A-031 0.59 0.05375 0.43561 0.05879 390 89 369 15 366 5
16-3A-032 0.59 0.05442 0.44517 0.05935 359 110 360 19 360 5
16-3A-033 0.59 0.05338 0.43263 0.05879 350 126 351 21 351 6
16-3A-034 0.60 0.05382 0.43763 0.05899 382 132 378 23 377 6
16-3A-035 0.60 0.05426 0.46097 0.06163 353 110 358 18 359 5
16-3A-036 0.60 0.05418 0.44277 0.05927 369 163 365 27 364 7
16-3A-037 0.60 0.05349 0.41317 0.05603 346 155 346 25 346 7
16-3A-038 0.61 0.05425 0.45256 0.06052 358 189 362 31 363 8
16-3A-039 0.61 0.05401 0.4415 0.0593 346 291 343 46 342 12
16-3A-040 0.61 0.05412 0.44418 0.05953 361 126 352 21 351 6
16-3A-041 0.62 0.0538 0.41481 0.05592 340 196 344 32 345 9
16-3A-042 0.62 0.0544 0.45322 0.06043 343 93 352 15 354 5
16-3A-043 0.62 0.05422 0.4334 0.05797 344 195 353 31 354 8
16-3A-044 0.63 0.05356 0.40407 0.05472 346 173 350 28 351 8
16-3A-045 0.64 0.0534 0.40597 0.05514 365 245 356 41 355 11
16-3A-046 0.64 0.05405 0.43873 0.05889 378 108 372 19 371 5
16-3A-047 0.64 0.0542 0.45608 0.06104 339 125 347 20 348 6
16-3A-048 0.65 0.05394 0.40832 0.05491 371 114 368 19 367 6
16-3A-049 0.65 0.05415 0.45566 0.06103 358 164 358 27 358 8
16-3A-050 0.65 0.05375 0.42851 0.05783 353 133 360 22 361 6
16-3A-051 0.65 0.05373 0.42983 0.05804 364 75 366 13 366 4
16-3A-052 0.66 0.05403 0.43084 0.05784 350 120 356 20 357 6
16-3A-053 0.66 0.05352 0.43539 0.05901 360 130 368 22 370 6
16-3A-054 0.66 0.05422 0.43119 0.05769 372 102 364 17 362 5
16-3A-055 0.67 0.05371 0.42514 0.05741 348 372 318 62 314 16
16-3A-057 0.67 0.05323 0.40746 0.05552 361 163 352 27 351 7
16-3A-058 0.68 0.05483 0.478 0.06324 354 114 368 19 370 6
16-3A-059 0.68 0.0537 0.42071 0.05684 342 119 360 20 363 6
16-3A-060 0.69 0.05366 0.42168 0.05701 376 88 376 16 376 5
16-3A-062 0.70 0.05356 0.42319 0.05731 407 102 404 19 404 6
16-3A-063 0.70 0.05336 0.42286 0.05747 379 101 382 18 382 5
16-3A-064 0.71 0.05414 0.44488 0.05961 353 220 370 38 373 11
16-3A-065 0.71 0.05354 0.41874 0.05673 369 107 378 19 380 6
16-3A-066 0.71 0.05385 0.41991 0.05656 387 114 365 19 362 5
16-3A-067 0.71 0.05399 0.4265 0.0573 356 147 358 25 359 7
16-3A-068 0.72 0.05421 0.44046 0.05894 369 287 373 49 373 13
16-3A-069 0.72 0.05381 0.4168 0.05618 371 110 361 19 359 6
16-3A-070 0.72 0.05405 0.44202 0.05932 368 228 368 39 368 11
16-3A-071 0.74 0.05326 0.40316 0.05491 380 135 366 23 363 7
16-3A-072 0.74 0.05412 0.44818 0.06007 376 93 373 16 373 5
16-3A-073 0.75 0.05336 0.41554 0.05648 353 177 345 27 343 6
16-3A-074 0.75 0.05368 0.42822 0.05787 366 160 362 27 362 8
16-3A-075 0.77 0.05349 0.42037 0.057 363 96 354 16 352 5
16-3A-076 0.77 0.05396 0.45165 0.06071 379 93 372 16 371 5
16-3A-077 0.78 0.05364 0.42339 0.05725 378 106 370 18 369 5
16-3A-078 0.78 0.05392 0.43619 0.05867 379 85 373 15 372 5
16-3A-079 0.79 0.05419 0.44428 0.05946 348 171 344 28 344 8
16-3A-080 0.81 0.05356 0.44021 0.05963 361 105 362 18 362 5
16-3A-081 0.81 0.05445 0.43863 0.05843 373 93 372 16 371 5
16-3A-082 0.85 0.05396 0.43298 0.0582 359 148 351 24 350 7
16-3A-083 0.85 0.05383 0.43417 0.0585 369 147 365 25 365 7
16-3A-084 0.85 0.05438 0.43289 0.05774 375 113 374 20 373 6
16-3A-085 0.88 0.05334 0.41477 0.0564 377 139 381 24 382 7
16-3A-086 0.96 0.05388 0.4287 0.05771 344 132 358 22 360 6
16-3A-087 0.98 0.05377 0.41436 0.0559 363 170 352 27 351 7
16-3A-088 1.01 0.05411 0.44303 0.05939 349 146 350 24 350 7
16-3A-089 1.02 0.05376 0.45481 0.06136 361 221 381 39 384 11
16-3A-090 1.10 0.0537 0.4244 0.05733 394 293 341 47 334 12
19-9-001 1.3 0.07659 2.10975 0.19986 1111 13 1152 8 1175 7
19-9-002 1.03 0.05653 0.60047 0.07706 473 77 478 17 479 6
19-9-003 1.18 0.05718 0.6206 0.07874 498 45 490 11 489 4
19-9-004 36.67 0.08112 2.48716 0.22243 1224 18 1268 11 1295 9
19-9-005 2.97 0.07747 2.15851 0.20212 1133 17 1168 10 1187 8
19-9-006 2.87 0.08053 2.33077 0.20997 1210 19 1222 11 1229 9
19-9-008 1.21 0.05538 0.51198 0.06706 428 378 420 80 418 23
19-9-009 1.9 0.05578 0.55635 0.07234 444 90 449 19 450 6
19-9-010 1.74 0.06397 0.76479 0.08672 741 108 577 29 536 10
19-9-012 1.09 0.10189 4.495 0.31998 1659 19 1730 14 1790 14
19-9-013 1.07 0.0553 0.52373 0.06869 424 142 428 28 428 9
19-9-015 1.8 0.05557 0.54587 0.07124 435 101 442 21 444 7
19-9-016 1.73 0.05571 0.54861 0.07142 441 125 444 25 445 8
19-9-017 1.99 0.05555 0.53326 0.06962 434 76 434 15 434 5
19-9-018 0.98 0.05599 0.54712 0.07087 452 82 443 17 441 6
19-9-019 2.93 0.0725 1.56769 0.15683 1000 43 958 19 939 10
19-9-020 1.81 0.05716 0.62123 0.07882 498 105 491 24 489 8
19-9-021 16.14 0.25129 20.08243 0.57962 3193 8 3095 11 2947 21
19-9-022 3.27 0.10661 4.47225 0.30424 1742 8 1726 7 1712 9
19-9-023 2.04 0.05683 0.59034 0.07534 485 58 471 13 468 5
19-9-024 2.78 0.05586 0.53136 0.06899 447 353 433 71 430 20
19-9-025 1.59 0.1644 9.87444 0.43561 2501 12 2423 12 2331 17
19-9-026 0.79 0.06098 0.58827 0.06997 639 108 470 24 436 7
19-9-028 7.08 0.07052 1.43962 0.14807 944 23 906 10 890 6
19-9-029 1.86 0.05913 0.734 0.09004 572 141 559 34 556 10
19-9-030 1.28 0.09226 3.26769 0.25689 1473 51 1473 32 1474 22
19-9-032 1.74 0.0774 2.17824 0.20413 1132 13 1174 8 1197 7
19-9-033 0.95 0.06024 0.61888 0.07451 612 200 489 44 463 12
19-9-034 1.03 0.05475 0.36714 0.04864 402 32 318 5 306 2
19-9-035 0.87 0.05635 0.55104 0.07093 466 148 446 30 442 10
19-9-036 1.17 0.13683 7.35616 0.38997 2187 8 2156 9 2123 12

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Received: 2023-03-21
Revised: 2023-07-24
Accepted: 2023-08-08
Published Online: 2024-02-01

© 2024 the author(s), published by De Gruyter

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

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  65. Usability of PPGIS tools exemplified by geodiscussion – a tool for public participation in shaping public space
  66. Efficient development technology of Upper Paleozoic Lower Shihezi tight sandstone gas reservoir in northeastern Ordos Basin
  67. Assessment of soil resources of agricultural landscapes in Turkestan region of the Republic of Kazakhstan based on agrochemical indexes
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  69. Petrogenetic relationship between plutonic and subvolcanic rocks in the Jurassic Shuikoushan complex, South China
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  76. Application of the wavelet transform and Hilbert–Huang transform in stratigraphic sequence division of Jurassic Shaximiao Formation in Southwest Sichuan Basin
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  78. Distribution law of Chang 7 Member tight oil in the western Ordos Basin based on geological, logging and numerical simulation techniques
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  87. Prediction of formation fracture pressure based on reinforcement learning and XGBoost
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  102. Research on spatial correlation structure of war heritage based on field theory. A case study of Jinzhai County, China
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  105. Deeply buried clastic rock diagenesis evolution mechanism of Dongdaohaizi sag in the center of Junggar fault basin, Northwest China
  106. Application of LS-RAPID to simulate the motion of two contrasting landslides triggered by earthquakes
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  117. Predicting stability factors for rotational failures in earth slopes and embankments using artificial intelligence techniques
  118. Origin of Late Cretaceous A-type granitoids in South China: Response to the rollback and retreat of the Paleo-Pacific plate
  119. Modification of dolomitization on reservoir spaces in reef–shoal complex: A case study of Permian Changxing Formation, Sichuan Basin, SW China
  120. Geological characteristics of the Daduhe gold belt, western Sichuan, China: Implications for exploration
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  126. Detection of seepage zones in artificial levees: A case study at the Körös River, Hungary
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  128. Characteristics and control techniques of soft rock tunnel lining cracks in high geo-stress environments: Case study of Wushaoling tunnel group
  129. Influence of pore structure characteristics on the Permian Shan-1 reservoir in Longdong, Southwest Ordos Basin, China
  130. Study on sedimentary model of Shanxi Formation – Lower Shihezi Formation in Da 17 well area of Daniudi gas field, Ordos Basin
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  137. Erratum
  138. Erratum to “Random forest and artificial neural network-based tsunami forests classification using data fusion of Sentinel-2 and Airbus Vision-1 satellites: A case study of Garhi Chandan, Pakistan”
  139. Special Issue: Natural Resources and Environmental Risks: Towards a Sustainable Future - Part I
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  141. Exploring environmental awareness, knowledge, and safety: A comparative study among students in Montenegro and North Macedonia
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  143. Application of remote sensing in monitoring land degradation: A case study of Stanari municipality (Bosnia and Herzegovina)
  144. Optimizing agricultural land use: A GIS-based assessment of suitability in the Sana River Basin, Bosnia and Herzegovina
  145. Assessing risk-prone areas in the Kratovska Reka catchment (North Macedonia) by integrating advanced geospatial analytics and flash flood potential index
  146. Analysis of the intensity of erosive processes and state of vegetation cover in the zone of influence of the Kolubara Mining Basin
  147. GIS-based spatial modeling of landslide susceptibility using BWM-LSI: A case study – city of Smederevo (Serbia)
  148. Geospatial modeling of wildfire susceptibility on a national scale in Montenegro: A comparative evaluation of F-AHP and FR methodologies
  149. Geosite assessment as the first step for the development of canyoning activities in North Montenegro
  150. Urban geoheritage and degradation risk assessment of the Sokograd fortress (Sokobanja, Eastern Serbia)
  151. Multi-hazard modeling of erosion and landslide susceptibility at the national scale in the example of North Macedonia
  152. Understanding seismic hazard resilience in Montenegro: A qualitative analysis of community preparedness and response capabilities
  153. Forest soil CO2 emission in Quercus robur level II monitoring site
  154. Characterization of glomalin proteins in soil: A potential indicator of erosion intensity
  155. Power of Terroir: Case study of Grašac at the Fruška Gora wine region (North Serbia)
  156. Special Issue: Geospatial and Environmental Dynamics - Part I
  157. Qualitative insights into cultural heritage protection in Serbia: Addressing legal and institutional gaps for disaster risk resilience
https://doi.org/10.1515/geo-2022-0529
Keywords for this article
Junggar Basin; Paleozoic; pyroclastic rock; zircon U–Pb dating
Creative Commons
BY 4.0

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  110. Extreme hydroclimatic events and response of vegetation in the eastern QTP since 10 ka
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  122. Enhancing the total-field magnetic anomaly using the normalized source strength
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  128. Characteristics and control techniques of soft rock tunnel lining cracks in high geo-stress environments: Case study of Wushaoling tunnel group
  129. Influence of pore structure characteristics on the Permian Shan-1 reservoir in Longdong, Southwest Ordos Basin, China
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  137. Erratum
  138. Erratum to “Random forest and artificial neural network-based tsunami forests classification using data fusion of Sentinel-2 and Airbus Vision-1 satellites: A case study of Garhi Chandan, Pakistan”
  139. Special Issue: Natural Resources and Environmental Risks: Towards a Sustainable Future - Part I
  140. Spatial-temporal and trend analysis of traffic accidents in AP Vojvodina (North Serbia)
  141. Exploring environmental awareness, knowledge, and safety: A comparative study among students in Montenegro and North Macedonia
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  143. Application of remote sensing in monitoring land degradation: A case study of Stanari municipality (Bosnia and Herzegovina)
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  145. Assessing risk-prone areas in the Kratovska Reka catchment (North Macedonia) by integrating advanced geospatial analytics and flash flood potential index
  146. Analysis of the intensity of erosive processes and state of vegetation cover in the zone of influence of the Kolubara Mining Basin
  147. GIS-based spatial modeling of landslide susceptibility using BWM-LSI: A case study – city of Smederevo (Serbia)
  148. Geospatial modeling of wildfire susceptibility on a national scale in Montenegro: A comparative evaluation of F-AHP and FR methodologies
  149. Geosite assessment as the first step for the development of canyoning activities in North Montenegro
  150. Urban geoheritage and degradation risk assessment of the Sokograd fortress (Sokobanja, Eastern Serbia)
  151. Multi-hazard modeling of erosion and landslide susceptibility at the national scale in the example of North Macedonia
  152. Understanding seismic hazard resilience in Montenegro: A qualitative analysis of community preparedness and response capabilities
  153. Forest soil CO2 emission in Quercus robur level II monitoring site
  154. Characterization of glomalin proteins in soil: A potential indicator of erosion intensity
  155. Power of Terroir: Case study of Grašac at the Fruška Gora wine region (North Serbia)
  156. Special Issue: Geospatial and Environmental Dynamics - Part I
  157. Qualitative insights into cultural heritage protection in Serbia: Addressing legal and institutional gaps for disaster risk resilience
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