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Article

Detrital Zircon U-Pb Age Data and Geochemistry of Clastic Rocks in the Xiahe–Hezuo Area: Implications for the Late Paleozoic–Mesozoic Tectonic Evolution of the West Qinling Orogen

1
Xi’an Center of Mineral Resources Survey, China Geological Survey, Xi’an 710100, China
2
Technology Innovation Center for Gold Ore Exploration, China Geological Survey, Xi’an 710100, China
3
Third Institute of Geological and Mineral Exploration, Gansu Bureau of Geology and Mineral Resources, Lanzhou 730050, China
*
Author to whom correspondence should be addressed.
Geosciences 2025, 15(10), 384; https://doi.org/10.3390/geosciences15100384
Submission received: 4 August 2025 / Revised: 30 August 2025 / Accepted: 16 September 2025 / Published: 3 October 2025
(This article belongs to the Special Issue Detrital Minerals Geochronology and Sedimentary Provenance)

Abstract

The West Qinling Orogenic Belt (WQOB) contains a sedimentary succession that is approximately 15 km thick, spanning from the Carboniferous to the Jurassic period. This succession offers critical insights into the tectonic evolution of the Paleo-Tethys Ocean. While previous models have suggested various depositional environments, the late Paleozoic to Mesozoic tectonic evolution of the WQOB is still not fully understood. In this study, we incorporate new detrital zircon U-Pb age data and whole-rock geochemical analyses from six stratigraphic units, dating back to the Carboniferous to Triassic periods in the Xiahe–Hezuo region, alongside existing datasets. The detrital zircon age spectra from the WQOB reveal three distinct groups: Devonian–Carboniferous strata exhibit dominant Neoproterozoic (~800–900 Ma) zircon populations, whereas Permian–Triassic rock samples show prominent Paleoproterozoic (1840–1880 Ma) and Archean (2450–2500 Ma) peaks. A minor Neoproterozoic component in Permian spectra disappears by the Triassic, while Jurassic–Cretaceous assemblages lack Precambrian grains. These trends reflect evolving source terranes linked to Paleo-Tethyan subduction dynamics. Furthermore, the geochemical signatures of the Devonian–Triassic clastic rocks align with the composition of upper continental crust, indicating a tectonic relationship with continental island arcs and active continental margins. By synthesizing these findings with established detrital zircon ages, magmatic records, and geophysical data, we propose that the WQOB underwent pre-Triassic tectonic evolution that was marked by pre-Triassic subduction and localized extension during the process of continental underthrusting.

1. Introduction

The Qinling Orogenic Belt (QOB), situated within the Central Orogenic Belt of China, was formed during the Paleozoic to Mesozoic period via the closure of the Shangdan and Mianlue oceans, branches of the Proto-Tethys and Paleo-Tethys separating the North China Block (NCB) and the South China Block (SCB) (Figure 1a) [1,2,3,4,5,6,7,8]. Despite extensive research on the tectonic evolution of the QOB in the Phanerozoic era, important aspects of its geodynamic development remain debated, particularly the pre-collisional processes that led to the termination of the Paleo-Tethyan regime in the Permian to Early Jurassic periods.
The West Qinling Orogenic Belt (WQOB) features an exceptionally well-preserved sedimentary succession that is approximately 15 km thick, spanning from the Carboniferous to the Jurassic period, with a predominant focus on the Triassic. This geological record provides essential detrital archives for reconstructing the orogen’s tectonic history [9,10,11,12,13]. Four competing models have been proposed to explain its depositional setting: (1) Flysch accumulation in a remnant oceanic basin during the collision of the NCB and the SCB [14,15,16]; (2) Syn-orogenic sedimentation related to continental convergence [17]; (3) the development of a foreland basin associated with the East–West Kunlun orogenic system [18,19,20,21]; (4) deposition occurring in an extensional back-arc rift basin, driven by the rollback of the Paleo-Tethyan slab [13]. Notably, Early Triassic–Early Jurassic magmatism in the WQOB coincides with widespread fold-thrust deformation in Lower Triassic strata, suggesting a dynamic interplay between magmatism and crustal shortening [22,23,24,25,26].
Figure 1. (a) Structural framework and research area location of China (according to Qiu et al. [7]); (b) geological units and gold deposit distribution map of the WQMB (according to Li et al. [27]).
Figure 1. (a) Structural framework and research area location of China (according to Qiu et al. [7]); (b) geological units and gold deposit distribution map of the WQMB (according to Li et al. [27]).
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In this study, we investigated the detrital sequences from the Carboniferous to Jurassic periods, which are exposed along a north–south transect in the Xiahe–Hezuo region of the WQOB. We present new U-Pb age indications and geochemical data of detrital zircon grains from six formations spanning the Carboniferous to Triassic periods, which help us constrain their provenance and tectonic relationships. By integrating our results with existing data on detrital zircon, magmatism, paleontological stratigraphy, and geophysics, we re-evaluate the evolution of the Paleo-Tethyan Ocean from the Late Paleozoic to the Late Mesozoic in the QOB.

2. Geological Background

The QOB is situated in the center of the Central Orogenic Belt, which is connected with the following orogenic belts: Kunlun in the west, Dabie-Sulu in the east, Qilian and NCB in the north and Songpan–Ganzi and the SCB in the south (Figure 1a) [28,29,30]. Structurally, the QOB is divided into several units by three major fault zones: Kuanping, Shangdan, and the Mianlue. These faults separate the QOB into the southern margin of the NCB, the North Qinling Block, the SCB, and the northern margin of the SCB [6,7] (Figure 1b). Geographically, the QOB is further divided into East Qinling metallogenic belt and West Qinling metallogenic belt by Huicheng Basin, Foping Dome, or the Baoji-Chengdu railway [31,32,33].
The WQOB as a composite collisional orogenic belt has undergone multiple phases of tectonic activity and a complex evolutionary history since the Archean. Previous studies indicate that the tectonic evolution of the WQOB, and its adjacent regions can be broadly divided into the following five stages: basement evolution, supercontinent breakup and ocean–continent evolution, collisional orogeny, intraplate extension, and intracontinental orogeny [34,35]. The process of oceanic subduction led to the closure of the Proto-Tethys and Paleo-Tethys oceans, ultimately resulting in the formation of the Triassic QOB [36,37].
The WQMB is primarily covered by Devonian to Cretaceous sedimentary rock sand the Precambrian basement is rarely exposed [38,39,40]. These provided critical insights into the region’s tectonic and depositional evolution. The Late Paleozoic strata comprise the Upper Devonian Dacaotan Formation (D3dc), Lower Carboniferous Badu Formation (C1b), Upper Carboniferous Xiajialing Formation (C2x), and Permian Shilidun Formation (Psl). To the south of the Minxian–Hezuo Fault, the Triassic units consist of the Lower Triassic Jiangligou Formation (T1j), Middle Triassic Guanggaishan Formation (T2gg), and Upper Triassic Daheba Formation (T3d). More recent deposits include the Lower Cretaceous Mogou Formation (K1m), the Neogene Linxia Formation (Nl), and Quaternary sediments (Q) [12] (Figure 2).
Recent investigations have documented that the early Mesozoic igneous rocks within the WQMB can be chronologically categorized into two distinct magmatic phases: (1) a Middle Triassic phase (246–234 Ma), predominantly exposed in the central and western sectors of the WQMB [41,42,43] and (2) a Late Triassic phase (228–205 Ma), which exhibits widespread distribution across the entire WQMB [44,45,46] (Figure 1b). Regarding the petrogenesis of the Middle Triassic magmatism in the WQMB, two principal genetic models have been proposed: (a) an active continental margin model, suggesting magma generation, was associated with the subduction of the A’nimaque oceanic slab [41,47]; and (b) an early post-collisional model, which attributes the magmatism to either the delamination of thickened lithosphere or the break-off of the subducted A’nimaque oceanic slab following the collision between the WQMB and the Songpan–Ganze block [42,48,49]. These differing hypotheses highlight the ongoing debate about the specific geodynamic mechanisms behind the Middle Triassic magmatic events in this composite orogenic belt.

3. Sample Selection and Analytical Methods

3.1. Sample Selection

The Xiahe–Hezuo region is a representative area for gold concentration within the late Paleozoic–Mesozoic strata of the WQOB. The Carboniferous–Triassic strata in this area exhibit good continuity in their exposure (see Figure 2 and Figure 3). For this study, we collected six clastic rock samples from the Xiahe–Hezuo region (Figure 2 and Figure 3). The samples include: (1) an arkose (TW-1) from the lower part of the C1b strata, (2) a sandy slate (TW-2) from the upper part of the C2x strata, (3) a fine sandstone (TW-6) from the upper Permian of the Psl strata, (4) two arkose (TW-8 and TW-9) from the upper Triassic of the T1j strata, and (5) a siltstone (TW-12) from the upper Triassic of the T3d strata. Each sample weighed over 2.5 kg to ensure there was sufficient material for subsequent analyses.

3.2. Methods

3.2.1. Zircon U-Pb Dating

For U-Pb geochronology, zircon grains were isolated through conventional magnetic and heavy liquid separation techniques, embedded in epoxy resin, and polished to expose flat internal surfaces. Cathodoluminescence (CL) imaging and subsequent U–Pb dating were conducted at the State Key Laboratory of Continental Dynamics, Northwest University, China. The internal structures of zircon grains were examined through a Mono CL3+ microprobe prior to analysis. In situ U–Pb isotopic measurements employed laser ablation inductively coupled plasma mass spectrometry (LA-ICP-MS) with a spot size of 32 μm. The analyses utilized an Agilent 7900 ICP-MS system coupled to a 193 nm laser. Operational conditions were optimized by ablating the NIST SRM 610 reference glass to achieve high signal sensitivity for high-mass isotopes, minimal oxide production, and stable background levels. Quantification of U, Th, and Pb concentrations relied on 29Si as an internal standard and NIST SRM 610 as the reference material. Isotopic ratios (207Pb/206Pb and 206Pb/238U) were processed through GLITTER 4.0 software and corrected against the well-characterized zircon reference materials 91500 and PLV. Concordia diagrams and kernel density estimation (KDE) diagrams were generated through the IsoplotR 4.2 software, which also facilitated their visualization [50]. Representative CL images of zircon grains are presented in Figure 4. The zircon U-Pb isotopic data are presented in Table S1.

3.2.2. Whole-Rock Major and Trace Element Analysis

The major and trace element analyses were conducted at the State Key Laboratory of Continental Dynamics, Northwest University. Fresh, unaltered samples were carefully selected during field collection. Sample preparation involved initial coarse crushing using a jaw crusher to ~5 mm particles, followed by pulverization to 200-mesh powder for subsequent analyses.
Whole-rock major elements were analyzed through X-ray fluorescence spectrometry (XRF; Rigaku RIX2100). Sample preparation followed the fusion method: 0.7000 g of powdered sample was thoroughly mixed with 5.200 ± 0.001 g Li2B4O7, 0.4000 ± 0.001 g LiF, and 0.3000 ± 0.001 g NH4NO3, then fused in platinum crucibles to produce homogeneous glass beads. Analytical quality was monitored through international standards (BCR-2, GBW07105) and replicate analyses (performed every 10 samples), with analytical uncertainties within ±2% [51].
Trace elements were determined by solution ICP-MS. For digestion, 50 mg samples were loaded into Teflon bombs with 1.5 mL ultrapure HNO3-HF (with 0.01 mL HClO4) and evaporated to dryness. After redissolution in 1.5 mL HF-HNO3, sealed bombs were heated at 190 °C for 48 h. The final solutions were transferred to acid-cleaned PET bottles, spiked with 1 μg Rh internal standard, and diluted to 80 g with 1% HNO3 for measurement. International reference materials (AGV-1, BHVO-1) yielded relative errors and standard deviations <5% for most elements [52]. The whole-rock geochemical data are presented in Table S2.

4. Results

4.1. Detrital Zircon U-Pb Age Data

Zircon grains from sample TW-1 (arkose) are euhedral to rounded with grain lengths of 70–120 μm, and zircon grains display typical magmatic crystallization zoning (Figure 4a). All the data show high concordance (90–100%; Figure 5a). Forty-one spots define three dominant age populations at 440–480 Ma, 920–950 Ma and 1820–1850 Ma in the kernel density estimation (KDE) plots (Figure 6a). The dominant age populations are Mesoproterozoic at 433–474 Ma with a peak at 460 Ma, which represent the youngest zircon population. The oldest zircon population age from 2447 to 2593 Ma, with a peak at 2473 Ma. A small number of zircon grains exhibit overgrowths and recrystallized core-rim structures.
Zircons from sample TW-2 (sandy slate) are subhedral prismatic crystals up to 120 μm long, and zircons display typical magmatic crystallization zoning. A few grains are rounded with unzoned rims (Figure 4b). Of the fifty-six analytical spots, fifty-five are within 5% of concordia (Figure 5b). Most grains from this sample are clustered in the 452–987 Ma age range (Figure 6b). Two prominent KDE peaks characterize populations at 445 Ma and 961 Ma defined, with less prominent peaks at 616 Ma, 784 Ma and 1090 Ma. The youngest zircon population yielded 425–467 Ma with peaks at 445 Ma. The oldest zircon age population from 2414 to 2462 Ma, which peak at 2438 Ma.
Zircon grains from sample TW-6 (fine sandstone) are subhedral prismatic crystals up to 100 μm long. Most grains have typical magmatic-metamorphism zoning, while a few have homogeneous internal structures and no zoning (Figure 4c). All analytical spots are within 5% of concordia (Figure 5c). Analyzed zircon grains range from 261 Ma to 2621 Ma with Th/U ratios ranging from 0.13 to 3.31. The data define three dominant age populations at 262–383 Ma, 1805–1898 Ma and 2402–2533 Ma. KDE plots show three dominant peaks at 312 Ma, 1861 Ma and 2496 Ma, with a subsidiary peak at 422 Ma (Figure 6c).
Zircon grains from Sample TW-8 (siltstone) are euhedral to rounded and with typical magmatic oscillatory zoning (Figure 4d). Eighty of the ninety analytical spots are within 5% of concordia (Figure 5d). U-Pb analyses yielded age values between 1329 and 1873 Ma with a wide range of U contents (19–692 ppm), Th/U ratios yielded an average of 0.64 (range 0.17–1.79). Three dominant age populations are identified at 1540–1310 Ma, 1820–1700 Ma and 2710–2600 Ma, with peaks at 1416 Ma, 1732 Ma and 2690 Ma (Figure 6d).
Zircon grains from sample TW-9 (siltstone) are subhedral prismatic crystals up to 120 μm long, and they display typical magmatic-metamorphism crystallization zoning. A few grains are rounded with unzoned rims (Figure 4e). Most grains from this sample are clustered in the 253–2484 Ma age range (Figure 6e). Four prominent KDE peaks characterize populations at 262 Ma, 408 Ma, 1281 Ma and 1986 Ma defined, with less prominent peaks at 2328 and 2486 Ma. The youngest zircon population yielded 253–268 Ma with peaks at 262 Ma. The oldest zircon age population from 2395 to 2574 Ma, which peak at 2486 Ma.
Zircon grains from sample TW-12 (feldspathic quartz sandstone) are subhedral prismatic crystals up to 120 μm long and display typical magmatic crystallization zoning (Figure 4f). Of the forty-eight analytical spots, forty-four are within 10% of concordia (Figure 5f). Most grains from this sample are clustered in the 231–483 Ma age range. Two prominent KDE peaks characterize populations at 263 and 421 Ma defined, with less prominent peaks at 932 and 1677 Ma. The youngest zircon population yielded 231–353 Ma with peaks at 263 Ma (Figure 6f).

4.2. Clastic Rock Petrographic Features

The arkose (TW-1) displays a medium-to-fine sandy texture with massive to medium-thick bedding. It is grain-supported, featuring contact cementation and linear grain contacts. The clasts consist of 99% grains, primarily quartz (80%), feldspar (15%), biotite (4%), and trace amounts of heavy minerals such as zircon and epidote. The matrix accounts for 1% and is composed of sericitized and biotitized fine silt-clay. The grains are moderately sorted and exhibit subangular to subrounded morphology (Figure 7a). The sandy slate (WT-2) has a microlepidoblastic texture with relict laminations and weak foliation. It is compositionally heterogeneous, containing detrital quartz (Qz) concentrated in light-colored laminae aligned parallel to bedding (S0), along with neoblastic sericite (Ser) and feldspar showing incipient foliation (S1) that is oblique to S0. High magnification reveals abundant cryptocrystalline residues, likely of siliciclastic origin (Figure 7b). The fine sandstone (TW-6) exhibits a fine-grained sandy texture and massive structure, primarily composed of quartz (69%), feldspar (15%), and calcareous cement (8%). The detrital grains make up 89% of the rock and include subangular to subrounded quartz (0.03–0.18 mm), altered feldspar (sericitized plagioclase, kaolinized orthoclase), lithic fragments, and minor micas (Figure 7c). Arkose samples (TW-8, TW-9) feature a medium-to-fine sandy texture with thin bedding, consisting of quartz (55%), feldspar (25%), lithics (8%), and minor micas. Detrital grains (92%) are subangular and poorly sorted, with quartz exhibiting undulose extinction and feldspars undergoing sericitization or kaolinization. The matrix (8%) includes calcite cement (micritic-sparitic), chloritized and sericized groundmass, and iron oxides. The rock is grain-supported with point contacts and pore-filling cementation (Figure 7d,e). The gray rock presents a silt-sized texture and a massive structure, predominantly composed of quartz (60%), feldspar (15%), calcite (10%), and a clay matrix (5%). Detrital grains (including quartz, feldspar, and lithics) are subangular to subrounded and poorly sorted, with feldspars showing signs of sericitization and argillization. Calcite occurs as anhedral grains with high iron content. Phyllosilicates (sericite, chlorite) exhibit a weak preferred orientation (Figure 7f).

4.3. Whole-Rock Geochemical Data

The six whole-rock geochemical samples analyzed correspond to the geochronological samples. The major oxide compositions show the following weight percentages: SiO2 ranges from 67.64% to 90%, Al2O3 from 4.39% to 16.04%, Fe2O3T from 1.12% to 4.25%, and MgO from 1.16% to 4.60%. These compositions closely resemble the average upper continental crust as reported by Taylor and McLennan (Figure 8a) [53], suggesting that there has been no significant alteration, transport, or reworking that would enhance the sample’s maturity.
The six samples exhibit moderate total rare earth element (REE) contents, with ΣREE ranging from 102.34 to 201.93 × 10−6. The LREE/HREE ratios vary between 7.69 and 11.36, while the La/Yb ratios range from 7.69 to 11.36. The chondrite-normalized REE patterns (Figure 8a) display pronounced rightward inclination, indicating significant light rare earth element (LREE) enrichment, consistent with the distribution characteristics of the upper continental crust (Figure 8b) [53,54]. All samples show enrichment of large ion lithophile elements (LILEs) (e.g., Rb and U) and light rare-earth elements (LREE), and depletion of HFSEs (e.g., Nb and Ta). They show slightly negative Eu and Sr anomalies.
Figure 8. (a) Primitive mantle-normalized trace clement spider diagrams; (b) chondrite-normalized REE diagram (chondrite values according to [53]); (c) La/Th vs. Hf diagram to discriminate the source rocks according to [55]; (d) Ti/Zr vs. La/Sc diagram to discriminate the tectonic setting according to [56]. C—Carboniferous, P—Permian, T—Triassic, UCC—upper continental crust.
Figure 8. (a) Primitive mantle-normalized trace clement spider diagrams; (b) chondrite-normalized REE diagram (chondrite values according to [53]); (c) La/Th vs. Hf diagram to discriminate the source rocks according to [55]; (d) Ti/Zr vs. La/Sc diagram to discriminate the tectonic setting according to [56]. C—Carboniferous, P—Permian, T—Triassic, UCC—upper continental crust.
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5. Discussion

5.1. Provenance of Detrital Zircon Grains

Integrated with our detrital zircon results, we have systematically compiled and analyzed Devonian to Cretaceous detrital zircon data from the WQOB. By comparing the magmatic age spectra of the NCB, SCB, North Qinling Orogen, and South Qinling Orogen, we have constructed Kernel Density Estimation (KDE) plots and magmatic activity diagrams for the WQOB during the Devonian to Cretaceous (Figure 9).
In contrast to the Permian–Triassic detrital zircon populations, the Devonian–Carboniferous spectra exhibit a prominent Neoproterozoic (~800–900 Ma) signature. Whereas, the Permian–Triassic spectra are characterized by distinct Paleoproterozoic (1840–1880 Ma) and Archean (2450–2500 Ma) age peaks. Notably, while the Permian and Triassic detrital zircon age distributions are broadly similar, the Permian spectra retain a minor Neoproterozoic (~900 Ma) component, whereas this feature is nearly absent in the Triassic record. Furthermore, Jurassic detrital zircon assemblages lack significant Precambrian-aged grains, whereas the Cretaceous spectra display a wide distribution across multiple age clusters (Figure 9).
Meanwhile, we have conducted a multi-dimensional scaling (MDS) analysis in the WQOB (Figure 10). In our 3-D MDS Shepard plot, most data points are positioned close to the 1:1 line and the stress is 0.188, indicating good fit (range 0–1 with 0 = perfect fit; Figure 9b). We correlate the Devonian to Cretaceous sedimentary strata across the WQMB and divided them into three distinct groups.
Group-1 predominantly comprises Devonian, Carboniferous, and partial Cretaceous strata, which are collectively characterized by a pronounced Neoproterozoic-Mesoproterozoic detrital zircon age spectrum (Figure 9a). Given that the North China Craton is notably deficient in Mesoproterozoic detrital zircon [64,65,66], as well as zircon grains with almost no roundness (Figure 4a,b,f), we propose that the primary provenance of these strata likely derives from the SCB or the QOB itself.
The MDS diagram clearly shows a distinct separation between Group-1 and Group-2, with the latter being primarily composed of Permian and Triassic strata. Both Group-1 and Group-2 are characterized by the absence of Neoproterozoic and Mesoproterozoic detrital zircon age spectra and the presence of prominent Archean detrital zircon signatures, as well as Permian–Triassic flysch depositional assemblages [67].
Field geological observations indicate that the Devonian to Cretaceous succession in the WQMB demonstrates continuous sedimentation (Figure 3). However, by integrating the detrital zircon characteristics of Groups-1 and 2 with substantial evidence of extensional features documented in previous studies on Triassic tectono-magmatism in the Xiahe–Hezuo region [33,40,42,44,47,68,69], we propose that a significant tectonic transition likely occurred in the WQMB from the Carboniferous to the Triassic period. This transition marks a shift from a subduction-related compressional setting during the Carboniferous to Early Permian to an extensional regime that prevailed from the Late Permian to the Triassic.
Group-3 is primarily found above Group-2 and mainly consists of detrital zircon from Jurassic strata, uppermost Triassic detrital zircon (specifically sample TW-12 in this study), and Triassic magmatic rocks with protolith age data of approximately 1.8 Ga from the Xiahe–Hezuo region (N55) [6,8,47,69]. This suggests a close genetic relationship between the Group-3 and the Group-2, while showing no affinity with the Group-1 regarding provenance. Additionally, field geological observations indicate that the Jurassic strata represent continuous deposition over the Permian–Triassic sequences. The absence of Precambrian detrital zircon suggests a relatively closed sedimentary environment.

5.2. Sedimentary Environment and Tectonic Background

The chemical composition of sedimentary rocks provides valuable insights into the tectonic setting of their source areas as well as characteristics of the parent rocks. Thus, the features of major, trace, and rare earth elements in fine-grained clastic rocks, such as mudstones and fine sandstones, are often used to trace their provenance and infer the nature of the source rocks [70,71,72,73].
In the La/Th-Hf diagram [55], most samples predominantly plot within the felsic upper crustal source field, while a subset falls into the felsic provenance domain (Figure 8c). One Triassic sample is located in the zone of increased ancient sedimentary components, indicating that all samples exhibit a source affinity unrelated to mafic materials. The elevated ancient sedimentary signature observed in the Triassic sample aligns with detrital zircon characteristics, likely reflecting the incorporation of ancient materials during the transition from a compressional to extensional tectonic regime. All samples demonstrate La, Ce, ΣREE concentrations and LREE/HREE ratios that closely approximate the characteristic values of active continental margins. Similar geochemical signatures are observed for immobile trace elements including Th, Zr, Ti, Co, and Ni. In the La/Sc-Ti/Zr discrimination diagram, all samples consistently plot within the oceanic island arc field (Figure 8d). Together, these geochemical characteristics collectively suggest that the Carboniferous–Jurassic clastic rocks in the WQOB were predominantly derived from a continental island arc and active continental margin setting.

5.3. Tectonic Evolution of the WQMB from Late Paleozoic to Mesozoic

The terminal closure of the eastern Paleo-Tethys Ocean during the Triassic period was characterized by continental collision between the NCB and the SCB [74,75]. Current tectonic models consistently indicate that the SCB did not directly collide with the NCB during the clockwise closure of the Paleo-Tethys Ocean in the QOB [35,76]. This interpretation is supported by the presence of Upper Ordovician-Early Permian marine sedimentary sequences in the WQMB [12,13,33,75], along with detrital zircon age spectra and geochemical signatures in this study. However, the relationship between Early Triassic flysch sedimentation and deformation and the onset of Triassic magmatic activity remains poorly understood.
On the basis of the following evidence, we propose that the WQOB experienced a tectonic evolution characterized by pre-Triassic subduction and localized extension during the Triassic subduction process: (1) the clearly distinguishable three-group characteristics of detrital zircon age spectra in Figure 8 and Figure 9; (2) detrital sediments indicative continental provenance (Figure 8); (3) detrital zircon from Jurassic strata in the WQOB displaying age spectra characteristic of convergent tectonic environments, while Carboniferous, Devonian and Cretaceous groups record collisional signatures. In contrast, Permian and Triassic detrital zircon reflect an extensional tectonic regime (Figure 11); (4) extensive magmatic studies, including the coexistence of crust-derived and mantle-derived magmas in the Jianzha–Tongren area [26], the presence of typical calcium-rich almandine garnets in the Sangke–Sai’erqinggou region [40], and the characteristic rapakivi texture of Shehaliji quartz monzonite, representing Early to Middle Triassic extensional processes [68]; (5) evidence of Permian–Triassic bathyal-abyssal trace fossils in the Gannan area [75]; and (6) the hypothesized branch of the Paleo-Tethys Ocean inferred from seismic interpretation profiles of the Western Qinling Orogenic Belt [13]. This evidence collectively supports our proposition concerning the tectonic evolution of the WQOB.
On the basis of the constraints outlined above, we present a brief model for the tectonic evolution of the WQOB during the Early to Middle Triassic, as illustrated in Figure 12. We propose that the WQOB likely represented a forearc setting during the Early Triassic.

6. Conclusions

(1)
The Devonian–Carboniferous strata in the WQOB are dominated by Neoproterozoic (~800–900 Ma) zircon populations, whereas the Permian–Triassic strata exhibit prominent Paleoproterozoic (1840–1880 Ma) and Archean (2450–2500 Ma) age peaks.
(2)
The clastic rocks from the Devonian to Triassic periods in the WQOB show geochemical signatures that are comparable to the composition of the upper continental crust. This suggests that they formed in a continental island arc and active continental margin setting.
(3)
By integrating our findings with existing datasets from studies of detrital zircon age dating, volcanic and plutonic activity, ancient rock layer sequences, and geophysical investigations, we propose that the WQOB underwent a tectonic evolution during the Triassic characterized by pre-Triassic subduction and localized extension during the subduction process.

Supplementary Materials

The following supporting information can be downloaded at: https://www.mdpi.com/article/10.3390/geosciences15100384/s1: Table S1: Detrital zircon U-Pb analysis data; Table S2: Whole rock geochemical data.

Author Contributions

Conceptualization, K.Y. (Kang Yan); Methodology, H.L. and K.Y. (Kang Yan); Software, H.G.; Validation, K.Y. (Kang Yan); Formal analysis, K.Y. (Kang Yan); Investigation, H.L., K.L., B.F., Z.X. and L.C.; Resources, B.F.; Data curation, H.L. and H.G.; Writing—original draft, H.L.; Writing—review & editing, H.L. and K.Y. (Kang Yan); Visualization, L.C.; Supervision, K.L. and K.Y. (Ke Yang); Project administration, K.L. and K.Y. (Ke Yang). All authors have read and agreed to the published version of the manuscript.

Funding

This research received external funding by the Project of China Geological Survey (DD20242984, DD20240019, DD20220975), Shaanxi Provincial Natural Science Basic Research Young Scientists Program (2025JC-YBQN-402) and the Science and Technology Support Program of the Ministry of Natural Resources of the People’s Republic of China (ZKKJ202414).

Data Availability Statement

Data will be available upon request.

Conflicts of Interest

The authors declare no conflicts of interest.

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Figure 2. Regional geological maps of the Xiahe–Hezuo area in WQMB (after Yu et al. [8], modified).
Figure 2. Regional geological maps of the Xiahe–Hezuo area in WQMB (after Yu et al. [8], modified).
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Figure 3. Stratigraphic profile of late Paleozoic–Mesozoic sedimentary rocks in the WQOB shows the location of samples and representative field photos.
Figure 3. Stratigraphic profile of late Paleozoic–Mesozoic sedimentary rocks in the WQOB shows the location of samples and representative field photos.
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Figure 4. Cathodoluminescence (CL) images of representative zircon crystals with locations of LA-ICP-MS analyses from this study. The 207Pb/206Pb age values are used for zircons older than 1000 Ma; otherwise, the 206Pb/238U age values are presented. The white circle with the size of the laser spot beam is 32 μm. The ruler is on the side of each image. (a) sample TW-1; (b) sample TW-2; (c) sample TW-6; (d) sample TW-8; (e) sample TW-9; (f) sample TW-12.
Figure 4. Cathodoluminescence (CL) images of representative zircon crystals with locations of LA-ICP-MS analyses from this study. The 207Pb/206Pb age values are used for zircons older than 1000 Ma; otherwise, the 206Pb/238U age values are presented. The white circle with the size of the laser spot beam is 32 μm. The ruler is on the side of each image. (a) sample TW-1; (b) sample TW-2; (c) sample TW-6; (d) sample TW-8; (e) sample TW-9; (f) sample TW-12.
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Figure 5. Zircon U-Pb concordia diagrams show U-Pb age dates of detrital zircon grains from clastic rocks in the Xiahe–Hezuo region of the WQMB. Zircon ages with >90% discordance are represented by red circles on the figure. (a) sample TW-1; (b) sample TW-2; (c) sample TW-6; (d) sample TW-8; (e) sample TW-9; (f) sample TW-12.
Figure 5. Zircon U-Pb concordia diagrams show U-Pb age dates of detrital zircon grains from clastic rocks in the Xiahe–Hezuo region of the WQMB. Zircon ages with >90% discordance are represented by red circles on the figure. (a) sample TW-1; (b) sample TW-2; (c) sample TW-6; (d) sample TW-8; (e) sample TW-9; (f) sample TW-12.
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Figure 6. Zircon U-Pb Kernel density estimation diagrams show U-Pb dating of detrital zircon grains from metasedimentary rocks in the Xiahe–Hezuo region of the WMQB. Plotted using Isoplot R [53] with a kernel bandwith of 50 Ma and a bin size of 40 Ma. The gray shaded area represents the Meso-Neoproterozoic age range. (a) sample TW-1; (b) sample TW-2; (c) sample TW-6; (d) sample TW-8; (e) sample TW-9; (f) sample TW-12.
Figure 6. Zircon U-Pb Kernel density estimation diagrams show U-Pb dating of detrital zircon grains from metasedimentary rocks in the Xiahe–Hezuo region of the WMQB. Plotted using Isoplot R [53] with a kernel bandwith of 50 Ma and a bin size of 40 Ma. The gray shaded area represents the Meso-Neoproterozoic age range. (a) sample TW-1; (b) sample TW-2; (c) sample TW-6; (d) sample TW-8; (e) sample TW-9; (f) sample TW-12.
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Figure 7. Photomicrographs of the Carboniferous–Permian rock samples (ac) and the Triassic samples (df). Pl = plagioclase, Ser = sericite, Qz = quartz, Sy = Sedimentary crystalline, Ms = muscovite, Bt = biotite, Cc = calcite, Kfs = K-feldspar.
Figure 7. Photomicrographs of the Carboniferous–Permian rock samples (ac) and the Triassic samples (df). Pl = plagioclase, Ser = sericite, Qz = quartz, Sy = Sedimentary crystalline, Ms = muscovite, Bt = biotite, Cc = calcite, Kfs = K-feldspar.
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Figure 9. Detrital zircon U-Pb age spectra from the Phanerozoic strata in the WQMB. The zircon U-Pb age spectra of the potential sources with their peaks are also shown. (a) Devonian [57,58,59]; (b) Carboniferous ([59,60], this study); (c) Permian ([59,61,62], this study); (d) Triassic ([8,61,63], this study); (e) Jurassic [61]; (f) Cretaceous [21,64]. Data of North China Block, Yangtze Block, North Qinling Terrane and South Qinling Terrane are from Yu et al. [8] and references therein.
Figure 9. Detrital zircon U-Pb age spectra from the Phanerozoic strata in the WQMB. The zircon U-Pb age spectra of the potential sources with their peaks are also shown. (a) Devonian [57,58,59]; (b) Carboniferous ([59,60], this study); (c) Permian ([59,61,62], this study); (d) Triassic ([8,61,63], this study); (e) Jurassic [61]; (f) Cretaceous [21,64]. Data of North China Block, Yangtze Block, North Qinling Terrane and South Qinling Terrane are from Yu et al. [8] and references therein.
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Figure 10. Detrital zircon age values from the WQMB. (a) Multi-dimensional scaling (MDS) plot of sample age likenesses colored by stratigraphic located region. Solid and dashed gray lines indicate nearest and next-nearest neighbors. (b) Shepard for the three-dimensional MDS.
Figure 10. Detrital zircon age values from the WQMB. (a) Multi-dimensional scaling (MDS) plot of sample age likenesses colored by stratigraphic located region. Solid and dashed gray lines indicate nearest and next-nearest neighbors. (b) Shepard for the three-dimensional MDS.
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Figure 11. Sedimentary basin tectonic setting discrimination plot On the basis of the distribution of difference between the crystallization age (CA) of individual zircon grains and the depositional age (DA) of succession in which they deposit [76]. A (red field), B (blue field) and C (green field) stand for convergent, collisional and extensional basins, respectively.
Figure 11. Sedimentary basin tectonic setting discrimination plot On the basis of the distribution of difference between the crystallization age (CA) of individual zircon grains and the depositional age (DA) of succession in which they deposit [76]. A (red field), B (blue field) and C (green field) stand for convergent, collisional and extensional basins, respectively.
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Figure 12. Pre-Triassic subduction and localized extension during the Triassic subduction process model of the WQOB. (a) Subduction of the Mianlue Ocean commenced prior to the Early Triassic.; (b) Sedimentation in a post-subduction extensional setting during the Middle Triassic.; (c) As detailed in Section 5.3, the Silurian-Triassic sedimentary phenomena in the WQMB are displayed in Figure 12b. Red circles represent granitic magmatism, green circles represent mafic magmatism, and white arrows indicate the extension direction. Notes: NCB = the North China Block; S-WQOB = the south of the West Qinling orogenic belt; N-WQOB = the north of the West Qinling orogenic belt, SCB = the South China Block.
Figure 12. Pre-Triassic subduction and localized extension during the Triassic subduction process model of the WQOB. (a) Subduction of the Mianlue Ocean commenced prior to the Early Triassic.; (b) Sedimentation in a post-subduction extensional setting during the Middle Triassic.; (c) As detailed in Section 5.3, the Silurian-Triassic sedimentary phenomena in the WQMB are displayed in Figure 12b. Red circles represent granitic magmatism, green circles represent mafic magmatism, and white arrows indicate the extension direction. Notes: NCB = the North China Block; S-WQOB = the south of the West Qinling orogenic belt; N-WQOB = the north of the West Qinling orogenic belt, SCB = the South China Block.
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Li, H.; Yan, K.; Li, K.; Yang, K.; Fan, B.; Xue, Z.; Chen, L.; Guo, H. Detrital Zircon U-Pb Age Data and Geochemistry of Clastic Rocks in the Xiahe–Hezuo Area: Implications for the Late Paleozoic–Mesozoic Tectonic Evolution of the West Qinling Orogen. Geosciences 2025, 15, 384. https://doi.org/10.3390/geosciences15100384

AMA Style

Li H, Yan K, Li K, Yang K, Fan B, Xue Z, Chen L, Guo H. Detrital Zircon U-Pb Age Data and Geochemistry of Clastic Rocks in the Xiahe–Hezuo Area: Implications for the Late Paleozoic–Mesozoic Tectonic Evolution of the West Qinling Orogen. Geosciences. 2025; 15(10):384. https://doi.org/10.3390/geosciences15100384

Chicago/Turabian Style

Li, Hang, Kang Yan, Kangning Li, Ke Yang, Baocheng Fan, Zhongkai Xue, Li Chen, and Haomin Guo. 2025. "Detrital Zircon U-Pb Age Data and Geochemistry of Clastic Rocks in the Xiahe–Hezuo Area: Implications for the Late Paleozoic–Mesozoic Tectonic Evolution of the West Qinling Orogen" Geosciences 15, no. 10: 384. https://doi.org/10.3390/geosciences15100384

APA Style

Li, H., Yan, K., Li, K., Yang, K., Fan, B., Xue, Z., Chen, L., & Guo, H. (2025). Detrital Zircon U-Pb Age Data and Geochemistry of Clastic Rocks in the Xiahe–Hezuo Area: Implications for the Late Paleozoic–Mesozoic Tectonic Evolution of the West Qinling Orogen. Geosciences, 15(10), 384. https://doi.org/10.3390/geosciences15100384

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