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Article

Ocean–Continent Conversion in Beishan Orogenic Belt: Evidence from Geochemical and Zircon U-Pb-Hf Isotopic Data of Luotuoquan A-Type Granite

by
Wenliang Chen
1,
Minjie Zhang
2,3,*,
Guanghuo Tao
1,
Xiaofeng Li
1,
Qian Yu
2,3,
Xiaojie Fan
2,3 and
Jingwei Zhang
2,3
1
Hebei Institute of Geological Survey, Shijiazhuang 050000, China
2
Hebei Key Laboratory of Strategic Critical Mineral Resources, Hebei GEO University, Shijiazhuang 050031, China
3
College of Resources, Hebei GEO University, Shijiazhuang 050031, China
*
Author to whom correspondence should be addressed.
Minerals 2023, 13(11), 1411; https://doi.org/10.3390/min13111411
Submission received: 5 September 2023 / Revised: 26 October 2023 / Accepted: 1 November 2023 / Published: 4 November 2023
(This article belongs to the Special Issue Tectonic–Magmatic Evolution and Mineralization Effect in the Southern Central Asian Orogenic Belt)
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Abstract

:
Devonian magmatism is one of the most important tectonothermal events in the Central Asian Orogenic Belt (CAOB). However, little is known regarding the petrogenesis and geodynamic setting of the widely distributed Devonian granitoids in the eastern Southern Beishan Orogenic Belt (SBOB). Early-Devonian granitic magmatism has been recognized from the Luotuoquan area, and the granites were emplaced between 404.9 Ma and 399.4 Ma according to LA-ICPMS zircon U–Pb dating. Geochemically, the granites exhibit high SiO2 and Al2O3 contents and are enriched in light rare earth elements as well as Rb, Th, Nd, Zr, and Hf, while being depleted in heavy rare earth elements and Ba, U, Sr, and Ti, with distinct rare earth element fractionation and pronounced negative Eu anomalies. According to the comprehensive analysis, they closely resemble the features typically associated with A-type granites. The zircons εHf(t) values are within the range of +0.90–+5.19 (averaged 3.23) for the monzogranite and syenogranite, whereas their TDM2 values fall between 1.05 and 1.34 Ga, suggesting that the magma source of the monzogranite–syenogranite originated from the partial melting of the Mesoproterozoic crust dominated by metagreywackes. Furthermore, the monzogranite and syenogranite exhibit high temperatures (average 782 °C), thin crustal thickness (average 30 km), and A-type characteristics, suggesting their formation in post-collision extensional settings. We propose the closure of the Beishan Ocean occurred before the early Devonian, followed by a transition in the Southern Beishan Orogenic Belt from a compressional to an extensional setting.

1. Introduction

The Central Asian Orogenic Belt (CAOB) is formed by the sequential accretion of multiple microcontinents, island arcs, seamounts, oceanic plateaus, and accretionary complexes from the early Neoproterozoic to the late Paleozoic [1,2,3]. The Beishan Orogenic Belt (BOB) connects the Tarim, Kazakhstan, and North China cratons [4,5,6] (Figure 1a) and is considered a critical southern Central Asian Orogenic Belt segment, vital for understanding crustal growth and tectonic evolution [5,6,7,8,9,10,11,12,13,14,15,16]. The Southern Beishan Orogenic Belt (SBOB), primarily consisting of the Shuangyingshan and Huaniushan units (Figure 1), is thought to record the collision and subduction among ancient microcontinents with Mesoproterozoic to Neoproterozoic basements [17,18,19,20,21]. However, the tectonic and thermal evolution of the SBOB remains unclear, particularly the timing of the Beishan Ocean closure during the early Paleozoic. Current views suggest the closure occurred in the later Silurian–early Devonian [22,23,24,25], Carboniferous [25], early Permian [26], or after the late Permian [27,28,29]. Thus, the Paleozoic crustal growth and geodynamics of the SBOB are rather controversial compared to those of the Mesozoic [11]. Further investigation of the tectonic and crustal development of the SBOB during the early–late Paleozoic is needed.
Herein, we present comprehensive whole-rock geochemical, in situ zircon U–Pb geochronology, and Hf isotopic data of A-type granites from the Luotuoquan complex. In addition to previously published findings, we discuss the genetic mechanism and tectonic settings of the early Paleozoic granitoids of the SBOB, elucidating their significant implications for understanding the tectonic evolution during this period in the BOB while also providing valuable insights into Beishan Ocean closure.

2. Geological Setting

The BOB comprises a complex assemblage of blocks, magmatic arcs, and ophiolitic mélanges that were formed through the subduction–accretion process of the Paleo–Asian Ocean [5]. Based on the spatial and temporal distributions of the ophiolitic mélanges and rock associations, the BOB is divided into several arcs [5], comprising (from north to south) the Queershan, Heiyingshan, Hanshan, Mazongshan, Shuangyingshan, Huaniushan, and Shibanshan arcs, which are separated by the Hongshishan, Shibanjing, Hongliuhe, and Liuyuan ophiolitic mélanges, respectively (Figure 1b).
The SBOB is situated within the Hongliuhe and Liuyuan ophiolitic mélanges [10] (Figure 1b) and comprises the Shuangyingshan and Huaniushan Units. In addition, the southern Beishan has recorded the subduction and collision of several microcontinental fragments and is characterized by early Paleozoic volcanic–sedimentary formations and intrusive plutons generated during early Paleozoic subduction [20,22,36,37]. Recent geochronological studies in the region reveal three stages of pluton emplacement in the Mid-Ordovician to late Silurian [6,23,38,39,40], early Devonian [4,6,40,41,42], and Late Devonian to early Carboniferous [6,38].
The Luotuoquan complex is situated in the eastern segment of the SBOB (Figure 1b) and intrudes into Silurian granitoids (Figure 2). It primarily consists of monzogranite, syenogranite, and minor basic rock. Field observations reveal that the syenogranite exhibits weak mylonitization and has intruded into the monzogranite (Figure 2). The Devonian samples are derived from the Luotuoquan granite complex, comprising five monzogranite samples (PM03-2, PM03-26, PM03-41, PM12-20, and PM17-4 and three syenogranite samples (D5195, D8373, and PM06-34). The monzogranite samples display medium- to coarse-grained massive rocks, primarily composed of quartz (20–25 vol%), K-feldspar (35–40 vol%), plagioclase (30–35 vol%), and orientated biotite and/or muscovite (5 vol%) (Figure 3a,b). The syenogranite samples exhibit well-developed mylonitization and a granoblastic texture. They predominantly consist of K-feldspar (55–60 vol%), plagioclase (10–15 vol%, An = 5–10), and quartz (20–25 vol%) with minor biotite (5 vol%) (Figure 3c,d).

3. Analytic Methods

3.1. Zircon Dating and CL Imaging

Zircons were separated from the granite samples PM06-34 and PM12-20 of the Luotuoquan complex for laser ablation inductively coupled plasma mass spectrometry (LA-ICP-MS) U–Pb dating. Zircon grains were extracted using standard density and magnetic separation techniques. The selected zircon grains were handpicked under a stereoscopic microscope and mounted in epoxy resin before being polished to dissect the crystals in half for analysis. Cathodoluminescence (CL) and reflected-light photomicrographic analysis of the prepared sample targets were utilized to image the morphology and internal structure of the zircons to aid in selecting zircon grains for U–Pb dating. Zircon U–Pb dating analyses were conducted on a quadrupole inductively coupled plasma mass spectrometer (ICP-MS) (THERMO-ICAPRQ) coupled to a 193-nm ArF Excimer laser (Resolution-LR, Applied Spectra, West Sacramento, CA, USA) at Hebei Key Laboratory of Strategic Critical Mineral Resources. The laser spot size was set to 29 μm, the laser energy density was 3 J/cm2, and the repetition rate was 8 Hz. Each analysis comprised a 10 s blank, a 40 s sampling ablation, and a 20 s sample-chamber flushing after the ablation. The ablated material was carried into the ICP-MS by the high-purity helium gas stream with a flux of 0.4 L/min. The whole laser path was fluxed with argon (0.9 L/min) to increase energy stability. A zircon 91,500 standard was used for external age calibration, and a zircon GJ–1 standard was used as a secondary standard to supervise the deviation of age calculation. Calibrations for trace element concentration were carried out using NIST SRM610 as an external standard and Si as the internal standard. ICPMSDataCal (Ver. 4.6) [43] and Isoplot 3.0 [44] programs were used for data reduction.

3.2. In Situ Lu-Hf Isotopes

In situ zircon Lu–Hf isotopic analyses were performed using a Neptune Plus MC–ICP–MS (Thermo Fisher Scientific, Brunswick, Germany) equipped with a Geolas 2005 excimer ArF laser ablation system (LambdaPhysik, Göttingen, Germany). All data on zircon were acquired in a single-spot ablation mode at a spot size of 44 μm. The energy density of laser ablation used in this study was ~7.0 J/cm−2. Each measurement consisted of a 20-s acquisition of the background signal, followed by a 50-s acquisition of ablation signals. Instrumental conditions and data acquisition were as described by Wu et al. (2006) [45]. Zircon 91,500 was used as the reference standard. The chondritic ratios of 176Hf/177Hf = 0.282772 and 176Lu/177Hf = 0.0332 were used in our calculation of εHf(t) values [46]. Single-stage model ages (TDM1) were calculated by reference to depleted mantle with a present day 176Hf/177Hf ratio of 0.28325 and 176Lu/177Hf ratio of 0.0384 [47]. The two-stage Hf model age (TDM2), also interpreted as crust formation age, was calculated by projecting the zircon 176Hf/177Hf (t) back to the depleted mantle model growth curve, assuming a mean crustal value for Lu/Hf (176Lu/177Hf = 0.015) [48].

3.3. Whole-Rock Geochemical Analysis

Whole-rock geochemical analyses were performed at the Institute of Regional Geology Survey of Hebei Province. Fresh chips of whole-rock samples were powdered to 200 mesh using a tungsten carbide ball mill. Major and trace elements were analyzed by X-ray fluorescence (Axios X; PANalytical B.V.) and inductively coupled plasma mass spectrometry (XSeries II; Thermo Fisher Scientific), respectively. The analytical precision is generally better than 2% for major elements. For trace element analyses, sample powders were digested using HF + HNO3 mixture in high-pressure Teflon bombs at 190 °C for 48 h or longer. The analytical precision is generally better than 5% for trace elements.

4. Result

4.1. Zircon U-Pb Dating and Lu-Hf Isotope Compositions

The zircons from monzogranite (PM12-20) and syenogranite (PM06-34) are similar in crystal morphology with sizes ranging from 80 to 200 μm and aspects ratios of 2:1–3:1. The CL images reveal oscillatory zoning and rare inherited cores (Figure 4). The Th/U ratios are >0.1, indicating magmatic origin (Table 1). Sixteen analyses from sample PM12-34 (monzogranite) were concordant and yielded a weighted mean age of 404.9 ± 1.4 Ma (Figure 4a). Sixteen spots were analyzed for dating from sample PM06-12, apart from six spots (RZ7, RZ9-11, RZ13, and RZ15), which represent the age of the inherited core, the remaining ten analyses yielded a weighted mean age of 399.4 ± 5.1 Ma (Figure 4b).
The analytical results are presented in Table 2, including εHf(t) values and model ages calculated using 206Pb/238U ages. The 32 spots from the Luotuoquan granites exhibit initial 176Hf/177Hf ratios ranging from 0.282205 to 0.282415 and positive εHf(t) values of +0.90–+5.19. Furthermore, the TDM2 model ages range from 1.05 to 1.34 Ga.

4.2. Major and Trace Elements

The whole-rock major and trace element compositions of the five monzogranite samples and three syenogranite samples were analyzed, and the results are presented in Table 3.

4.2.1. Major Elements

The samples possess high SiO2 (71.04–76.00 wt.%), K2O (4.02–5.59 wt.%), and K2O + Na2O (7.04–8.62 wt.%); however, they possess low Al2O3 (12.10–14.30 wt.%), MgO (0.07–0.63 wt.%), and CaO (0.76–2.53 wt.%). In the SiO2 versus K2O + Na2O diagram (Figure 5a), the samples are plotted within the granitoid fields, which is consistent with the petrographic observations. They further display low A/CNK values (molar Al2O3/(CaO + Na2O + K2O)) ranging from 0.85 to 1.08 and exhibit peraluminous and high K characteristics (Figure 5).

4.2.2. Trace Elements

In the chondrite-normalized rare earth element patterns, the samples exhibit relative enrichment of light rare earth elements (LREE)([La/Yb]N = 2.63–16.87) and significant negative Eu anomalies (Eu/Eu* = 0.23–0.45), while the REE abundances range from 161.2 to 459.7 ppm (Figure 6a). All samples are depleted in Ba, U, Sr, P, and Ti and enriched in Rb, Th, Nd, Zr, and Hf relative to the primitive mantle (Figure 6b).

5. Discussion

5.1. Devonian Magmatism in the Southern Beishan Orogenic Belt

The LA–ICP–MS zircon U–Pb ages obtained in this study (404–399 Ma) are consistent with the timing of pluton emplacement in the SBOB, including the Liuyuan monzogranite (397 ± 7 Ma) [40], Shuangfengshan A-type granites (415 ± 3 Ma) [4], Huitongshan K-feldspar granite (397 ± 3 Ma) [42], and Shijinpo granitoid (404 ± 2 Ma) [53]. Previous studies have established that the Silurian–Devonian was a crucial period of magmatism in the BOB (Figure 1a), with age peaks of 440, 420, and 400 Ma. The Luotuoquan granites, as products of Devonian magmatism, offer valuable insights into the geodynamic evolution of the BOB during the mid-Paleozoic.

5.2. Petrogenesis and Magma Sources

The syenogranite samples in this study have undergone mylonitization, as evidenced by petrographic observation (Figure 2d). Therefore, it is imperative to evaluate the impact of alteration on both major and trace elements before discussing their petrogenesis [55]. Our samples demonstrate differentiated correlations between “immobile alteration” elements (e.g., Zr) and the other trace elements (Figure 7), where Nb, Ta, Th, and Hf display a stronger correlation with Zr than Rb and Ba, suggesting that this alteration has less effect on these elements. Consequently, the subsequent discussion will primarily focus on more immobile elements such as Nb, Ta, Zr, and REEs.
The Luotuoquan monzogranite and syenogranite exhibit similar geochemical characteristics and are discussed together. They have high SiO2 (71.04–76.00 wt.%) and K2O + Na2O (7.04–8.62 wt.%) but low Al2O3 (mean of 13.36 wt.%), MgO (mean of 0.03 wt.%), and CaO (mean of 1.64 wt.%), indicating A-type granite geochemical characteristics. Nevertheless, highly fractionated I-type and S-type granites also share similarities with A-type granites. Highly fractionated S-type granites tend to exhibit higher P2O5 (mean of 0.14 wt.%) and lower Na2O (mean of 2.81 wt.%) than A-type granites [56]. The monzogranite–syenogranite displays low P2O5 (mean of 0.11 wt.%) and high Na2O (mean of 3.09 wt.%), indicating it does not belong to the highly fractionated S-type granite. Compared with highly fractionated I-type granite, A-type granite shows iron enrichment and magnesium depletion with higher Fe2O3T/MgO ratios. The Fe2O3T/MgO value of Luotuoquan granite ranges from 2.95 to 24.28 (mean of 6.95), which is significantly greater than that of highly fractionated I-type granite (2.27) and S-type granite (2.38) [57,58]. Additionally, typical A-type granites are enriched in trace elements such as Th, Nb, Ta, Zr, Hf, Ga, and Y while being depleted in Sr, Ti, P, Cr, Co, Ni, V, etc., with obvious negative Eu anomaly [57,59]. All samples exhibit high Th, Zr, K, Ga, Y, and Yb but low Sr, P, Eu, and Ti, which also implies that Luotuoquan granite had A-type geochemical features. Previous studies suggested that A-type granitoids share similar geochemistry characteristics of high 10,000× Ga/Al values (>2.6) and Zr + Nb + Ce + Y (>350 ppm) [57]. The discrimination diagrams (Figure 8) demonstrate that the majority, if not all, of the samples are plotted within the A-type granite field. We, therefore, conclude that the Luotuoquan monzogranite–syenogranite pluton are typical A-type intrusions.
Various petrogenetic models have been proposed for A-type granites: (1) high crystallization differentiation of mantle-derived basaltic magma [60,61,62,63]; (2) mixing of mantle-derived and crustal materials [64,65,66,67]; (3) Partial melting of lower crustal material: partial melting of granulite facies remnants after granitic magma extraction [55,56,59,68], and partial melting of calc-alkaline tonalite-granodiorite [69]; (4) the melting of lower crustal rocks due to heating by mantle magma underplating [58,70,71]. Mafic rocks contemporaneous with A-type granite are rare in the study area, and no mafic microgranular enclaves are found in the granites, indicating little crust–mantle mixing. Experimental petrology shows residual granulite facies in the lower crust are low in K, Si and high in Ca, Al, and Mg [69], which cannot explain the production of Luotuoquan A-type granite rich in Si, alkali, low in Al and Mg by partial melting.
The CaO/Na2O ratios distinguish between pelite-derived melts (CaO/Na2O < 0.5) and melts derived from greywackes or igneous sources (CaO/Na2O = 0.3–1.5) [72]. High-temperature melts generally exhibit lower Al2O3/TiO2 ratios than low-temperature melts [73]. The monzogranite–syenogranite is characterized by high CaO/Na2O ratios (mean of 0.53) and low Al2O3/TiO2 ratios (mean of 63.73), suggesting a source of metagreywackes or metamorphic igneous rock. The samples are all plotted within the field of partial melts derived from metagreywackes in the molar Al2O3/(MgO + FeOT) vs. molar CaO/(MgO + FeOT) and molar K2O/Na2O vs. molar CaO/(MgO + FeOT) diagrams (Figure 9). Therefore, the granitic magma source is likely related to partial melts from metagreywackes.
The Hf isotope analysis of U-Pb dated zircon grains can trace the original magma sources and distinguish between the reworking of continental crust and the remelting of juvenile crust [74,75]. In this study, the early Devonian Luotuoquan monzogranite–syenogranite has considerably positive zircon εHf(t) of +0.9–+5.2 (Figure 10) and slightly young two-stage Hf model ages of 1.05–1.34 Ga (Figure 10). The SBOB is thought to have developed abundant Mesoproterozoic to Neoproterozoic basement complex, which is a suite of metamorphosed clastic rock [17,18,20,37]. The significantly positive εHf(t) values and relatively young two-stage Hf model ages suggest that the granitic rocks originated from either the depleted mantle or through partial melting of recently accreted juvenile crustal material within the depleted mantle. Relevant mafic rocks are rarely contemporaneous, and the absence of mafic microgranular enclaves suggests limited direct involvement of newly derived mantle magma in granite formation. Therefore, the early Devonian granitoids from the SBOB primarily originated from partial melting of the overlying Mesoproterozoic crust facilitated by the underplating of mantle-derived magma.
Minerals 13 01411 g009
Figure 9. Discrimination diagrams of the source area of the Luotuoquan monzogranite and syenogranite. (a) molar Al2O3/(MgO + FeOT) vs. molar CaO/(MgO + FeOT) [76]; (b) molar K2O/Na2O vs. molar CaO/(MgO + FeOT) [77].
Figure 9. Discrimination diagrams of the source area of the Luotuoquan monzogranite and syenogranite. (a) molar Al2O3/(MgO + FeOT) vs. molar CaO/(MgO + FeOT) [76]; (b) molar K2O/Na2O vs. molar CaO/(MgO + FeOT) [77].
Minerals 13 01411 g009

5.3. Geodynamic Evolution

Recent research suggests that the BOB is an accretionary orogen with multiple island arcs and mélange belts that experienced subduction–collision during the Paleozoic [5,12,28,30,37]. The zircon U–Pb age of the ophiolite complexes in the central part of the BOB is 536–519 Ma [7,79,80,81], and the lower Cambrian Shuangyingshan Formation unconformable overlies the Neoproterozoic Xichangjing Formation [38], indicating the Beishan Ocean was formed before the Cambrian. Previous studies have proposed that the magmatic effects of slab windows vary dramatically during ridge subduction, forming adakitic magmas due to slab melting and A-type magmas resulting from asthenosphere upwelling through the slab window [54,82]. Widespread early Paleozoic magmatic rocks (464–424 Ma) [6,10,16,32,37,40,83,84] and ophiolitic mélange (462–420 Ma) [9,13,39,85] in the BOB indicate slab subduction setting during the Ordovician to Devonian.
The A-type granite has garnered significant attention due to its distinctive tectonic background. The Luotuoquan A-type granites fall within the volcanic arc and within-plate granites on tectonic discrimination diagrams (Figure 11a,b) rather than pertaining to ocean ridge granites. The studied granites are generally plotted within the A2 field (Figure 11c,d). The A2-type granitoids represent magmas sourced from the underplated crust or continental crust that has experienced a cycle of island-arc magmatism or continent-continent collision [86]. We propose that their potential origins were associated with island-arc magmatism. The monzogranite in the Hongliuhe ophiolite has a weighted age of 412.4 ± 2.9 Ma, indicating that the closure of the oceanic basin was completed prior to this event [41]. The granites from the Liuyuan area, with ages ranging from 436-423 Ma [40], 415 Ma [42], and 397 Ma [4,40], represent post-collision background products that are possibly associated with subduction plate detachment. Moreover, recent discoveries have revealed the presence of early Devonian post-collision granites in the middle of BOB. U–Pb dating has determined that these granites range in age from 402 to 387 Ma [15,31,35,52]. The aforementioned evidence suggests that the formation of Luotuoquan A-type granites can be attributed to a post-collision tectonic setting.
Whole-rock geochemical data of 460–390 Ma granites from the SBOB were collected to calculate zircon saturation temperatures (ln DZr = (10,108 ± 32)/T(K) − (1.16 ± 0.15)(M − 1) − (1.48 ± 0.09)) [87], M = (Na + K + 2Ca)/(Al × Si)(mol)) [88] and crustal thickness (H = [Sr/Y + (42.03 ± 6.28)]/(1.49 ± 0.15)) [89,90]. During the early Paleozoic, a significant increase in crustal growth occurred due to the melting of subducting oceanic crust, resulting in the emplacement of large amounts of granitoids in the SBOB from 452 to 424 Ma [6]. This process was accompanied by a gradual decrease in zircon saturation temperatures and an increase in crustal thickness (Figure 11). The A-type granites, which were formed between 415 and 397 Ma [4,42], exhibit a higher Zr saturation temperature range of 755–831 °C and a thinner crust thickness ranging from 32 to 28 km (Figure 12). These findings suggest that the SBOB had already transitioned into an extensional setting during the early Devonian.
In summary, the Luotuoquan A-type granites yield U-Pb ages of approximately 404–399 Ma, indicating post-collision extensional setting during the early Devonian. This evidence indicates a post-collision extension setting in the early Devonian and implies the closure of the Beishan Ocean prior to this time.

6. Conclusions

(1) The zircon U–Pb ages of the Luotuoquan monzogranite and syenogranite are 399.4 ± 5.1 Ma and 404.9 ± 1.4 Ma, respectively.
(2) The petrographic and geochemical signatures of the Luotuoquan monzogranite and syenogranite indicate they are A-type granites and were emplaced in a post-collision extensional setting. Furthermore, these granites are the result of partial melting primarily from Mesoproterozoic crusts composed mainly of metagreywackes.
(3) The occurrence of early Devonian granitoids suggests that SBOB had already undergone extensional tectonics following the closure of the Beishan Ocean during this period.

Author Contributions

Conceptualization: W.C. and M.Z.; Data curation: Q.Y., X.F. and J.Z.; Investigation: W.C., G.T. and X.L.; Methodology: M.Z. and G.T.; Resources: W.C. and M.Z.; Writing–original draft preparation: W.C., M.Z. and G.T.; Writing–review and editing: W.C. and M.Z.; Visualization: Q.Y. and X.F.; Supervision: X.L.; Project administration: M.Z. and Q.Y. All authors have read and agreed to the published version of the manuscript.

Funding

This research was supported by the Natural Science Foundation of Hebei Province (D2020403044) and the Opening Foundation of Hebei Key Laboratory of Strategic Critical Mineral Resources (HGU-SCMR2304).

Data Availability Statement

All the data are presented in the paper.

Acknowledgments

We sincerely appreciate the editors and reviewers for their constructive comments, which helped to significantly improve the manuscript.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. (a) Tectonic setting of the BOB (modified after [5]). (b) Simplified tectonic map of the Beishan orogenic collage and its adjacent area showing the tectonic subdivisions (modified after [5,13]). The zircon U-Pb age data of granitoids in (b) are from previous studies [4,6,10,30,31,32,33,34,35].
Figure 1. (a) Tectonic setting of the BOB (modified after [5]). (b) Simplified tectonic map of the Beishan orogenic collage and its adjacent area showing the tectonic subdivisions (modified after [5,13]). The zircon U-Pb age data of granitoids in (b) are from previous studies [4,6,10,30,31,32,33,34,35].
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Figure 2. Geological map of the mafic–ultramafic intrusions and granite plutons in the Luotuoquan area.
Figure 2. Geological map of the mafic–ultramafic intrusions and granite plutons in the Luotuoquan area.
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Figure 3. Field and microscopic photos of the Luotuoquan monzogranite (a,b) and syenogranite (c,d). Qtz-quartz; Pl-plagioclase; Kfs-potassium feldspar; Bt-biotite.
Figure 3. Field and microscopic photos of the Luotuoquan monzogranite (a,b) and syenogranite (c,d). Qtz-quartz; Pl-plagioclase; Kfs-potassium feldspar; Bt-biotite.
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Figure 4. U–Pb concordia diagrams of zircons from Luotuoquan monzogranite (a) and syenogranite (b). The yellow line circle represents the spot of LA-ICP-MS analysis for U–Pb dating. The red dashed line circle represents the spot of LA-MC-ICP-MS analysis for Lu–Hf isotope compositions.
Figure 4. U–Pb concordia diagrams of zircons from Luotuoquan monzogranite (a) and syenogranite (b). The yellow line circle represents the spot of LA-ICP-MS analysis for U–Pb dating. The red dashed line circle represents the spot of LA-MC-ICP-MS analysis for Lu–Hf isotope compositions.
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Figure 5. (a) Total alkalis (Na2O + K2O) vs. SiO2 diagram [49]; (b) K2O vs. SiO2 diagram [50]; (c) A/NK vs. A/CNK diagram [51]. Published data of the early Devonian granitoids in the Beishan area are from [4,6,30,31,42,52,53].
Figure 5. (a) Total alkalis (Na2O + K2O) vs. SiO2 diagram [49]; (b) K2O vs. SiO2 diagram [50]; (c) A/NK vs. A/CNK diagram [51]. Published data of the early Devonian granitoids in the Beishan area are from [4,6,30,31,42,52,53].
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Figure 6. Chondrite-normalized REE element patterns (a) and primitive mantle-normalized trace element spider diagrams (b) for the Luotuoquan granites. Normalization values are from [54].
Figure 6. Chondrite-normalized REE element patterns (a) and primitive mantle-normalized trace element spider diagrams (b) for the Luotuoquan granites. Normalization values are from [54].
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Figure 7. Trace elements vs. Zr for Luotuoquan A-type granites.
Figure 7. Trace elements vs. Zr for Luotuoquan A-type granites.
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Figure 8. Discrimination diagrams for early Devonian granitoids from BOB. Zr (a) and Nb (b) vs. 10,000 ∗ Ga/Al and (K2O + Na2O)/CaO (c) and FeOT/MgO (d) vs. Ce + Nb + Zr + Y diagrams [57]. Published data are from the same references as in Figure 5.
Figure 8. Discrimination diagrams for early Devonian granitoids from BOB. Zr (a) and Nb (b) vs. 10,000 ∗ Ga/Al and (K2O + Na2O)/CaO (c) and FeOT/MgO (d) vs. Ce + Nb + Zr + Y diagrams [57]. Published data are from the same references as in Figure 5.
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Figure 10. Zircon εHf(t) vs. Age (Ma) diagrams of granitoids from the SBOB (base map after [75]). Published data of granitoids from [6,42]. The data on Tarim, North China, and Yangtze blocks were from [78].
Figure 10. Zircon εHf(t) vs. Age (Ma) diagrams of granitoids from the SBOB (base map after [75]). Published data of granitoids from [6,42]. The data on Tarim, North China, and Yangtze blocks were from [78].
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Figure 11. Nb vs. Y (a), Ta vs. Yb (b), Nb-Y-Ce (c), Nb-Y-3Ga (d) tectonic discriminant diagrams of the early Devonian granitoids from BOB ((a,b) modified after [56], (c,d) modified after [86]). Syn-COLG-syn-collision granites; VAG-volcanic arc granites; WPG-within plate granites; ORG-ocean ridge granites; post-COLG-post collision granites. Published data are from the same references as in Figure 5.
Figure 11. Nb vs. Y (a), Ta vs. Yb (b), Nb-Y-Ce (c), Nb-Y-3Ga (d) tectonic discriminant diagrams of the early Devonian granitoids from BOB ((a,b) modified after [56], (c,d) modified after [86]). Syn-COLG-syn-collision granites; VAG-volcanic arc granites; WPG-within plate granites; ORG-ocean ridge granites; post-COLG-post collision granites. Published data are from the same references as in Figure 5.
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Figure 12. Tzr vs. Age (a) and Crustal thickness vs. Age (b) plots for Paleozoic granitoids in the SBOB. Published data from [4,6,42].
Figure 12. Tzr vs. Age (a) and Crustal thickness vs. Age (b) plots for Paleozoic granitoids in the SBOB. Published data from [4,6,42].
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Table 1. LA-ICP-MS zircon U–Pb dating results of the Luotuoquan granites.
Table 1. LA-ICP-MS zircon U–Pb dating results of the Luotuoquan granites.
NoPbUIsotopic RatiosIsotopic Age (Ma)
(ppm)207Pb/206Pb1σ207Pb/235U1σ206Pb/238U1σ207Pb/206Pb1σ207Pb/235U1σ206Pb/238U1σ
PM12-20: monzogranite
RZ1752940.05290.00280.47540.02340.06540.001132412039516.14097.2
RZ21014570.05560.00260.49580.02130.06450.000943910440914.54036.1
RZ3844200.05390.00200.48510.01790.06470.00103658840212.34046.5
RZ4693600.05400.00210.48450.01780.06480.00093728740112.24056.3
RZ51205290.05540.00200.50260.01880.06540.001142881.541312.74086.6
RZ6722960.05510.00280.49220.02440.06460.001241711540616.64037.1
RZ7743000.05570.00260.49390.02140.06470.001044399.140814.64046.4
RZ81104860.05490.00200.4920.01720.06450.000940681.540611.74036.2
RZ960.63300.05100.00280.46510.02570.06510.001223913038817.84067.1
RZ102339000.05590.00220.50740.01880.06460.001045682.441712.74036.3
RZ1156.32310.05480.00260.48780.02110.06450.001046710640314.44036.4
RZ1234.41490.05510.00480.49740.04080.06510.001541319341027.74069.4
RZ131275300.05440.00190.48820.01710.06440.001038781.540411.74026.8
RZ14863880.05450.00220.49120.01890.06510.000939190.740612.84075.2
RZ15763260.05500.00320.49880.02890.06540.001141313141119.64087.3
RZ16823600.05240.00210.47290.01840.06510.000930692.639312.74076.1
PM06-34: syenogranite
RZ148.32130.05540.00250.47700.02210.0620.001142810439615.23876.4
RZ251.22270.05490.00290.47190.02340.06270.001240611739216.13927.3
RZ346.11920.05670.00310.49250.02550.06350.001348011440717.43978.1
RZ41144220.05460.00220.47980.01980.06230.001039490.739813.63906.1
RZ51235850.05370.00210.47850.01820.06370.001036788.939712.53986.2
RZ6923050.05740.00260.50680.02120.06370.001250610041614.33987.2
RZ7773370.05650.00280.52970.02660.06680.001147210543217.74177.0
RZ861.63840.05850.00220.50460.01900.06200.001255083.341512.83887.1
RZ9853980.06230.00260.57500.02350.06600.001168788.946115.14127.2
RZ10984470.05700.00220.51920.01930.06560.001150083.342512.94106.1
RZ1154.22780.05470.00250.50560.02270.06720.00123989941515.34197.5
RZ1252.62410.05470.00250.47200.02040.06300.001139810239314.13947.2
RZ1339.91680.06540.00380.59960.03770.06610.001478712247723.94128.1
RZ14752670.05570.00270.48140.02140.06340.001243910739914.73967.2
RZ15954240.05570.00230.51920.02330.06700.001243994.442515.64187.3
RZ1645.22200.05640.00270.48730.02260.06220.001347810340315.43898.0
Table 2. In situ zircon Hf isotopic results of the Luotuoquan granites.
Table 2. In situ zircon Hf isotopic results of the Luotuoquan granites.
NoAge (Ma)176Yb/177Hf176Lu/177Hf176Hf/177Hf2σεHf(0)εHf(t)2σTDM1 (Ma)f(Lu/Hf)TDM2 (Ma)
PM12-20: monzogranite
RZ14090.0148560.0005300.2822420.000015−18.73.720.51894−0.981160
RZ24030.0315340.0011730.282400.000017−13.22.960.59927−0.961204
RZ34040.0254780.0008560.282380.000018−13.93.820.64876−0.971150
RZ44050.0418850.0014180.2823810.000014−13.83.390.49895−0.961178
RZ54080.0301060.0010310.2823370.000015−15.43.510.51887−0.971173
RZ64030.0404900.0013740.2823180.000015−16.13.710.54873−0.961156
RZ74040.0481240.0017110.2823500.000017−14.94.120.59884−0.951131
RZ84030.0347570.0011740.2823340.000014−15.52.320.51934−0.961244
RZ94060.0283900.0009620.2822790.000014−17.43.120.51902−0.971196
RZ104030.0324150.0011070.2823600.000015−14.62.660.54914−0.971223
RZ114030.0335780.0011250.2823190.000014−16.03.300.50889−0.971182
RZ124060.0542880.0019870.2823170.000014−16.13.880.49879−0.941148
RZ134020.0084800.0002660.2822050.000016−20.13.580.55907−0.991164
RZ144070.0290750.0009760.2824150.000014−12.64.340.49873−0.971119
RZ154080.0546990.0018280.2823990.000015−13.23.740.54875−0.941158
RZ164070.0296100.0010110.2823480.000016−15.04.570.58847−0.971105
PM06-34: syenogranite
RZ13870.0320290.0010970.2823170.000018−16.12.960.64890−0.971192
RZ23920.0112100.0003520.2822540.000018−18.35.190.64814−0.991054
RZ33970.0453440.0015020.2823430.000015−15.22.520.54914−0.951227
RZ43900.0288690.0009860.2823210.000019−15.94.660.67831−0.971086
RZ53980.0315340.0011730.2824000.000015−13.22.390.51922−0.961236
RZ63980.0254780.0008560.2823800.000017−13.92.310.59928−0.971241
RZ74170.0418850.0014180.2823810.000016−13.80.950.58998−0.961341
RZ83880.0301060.0010310.2823370.000014−15.42.920.51893−0.971195
RZ94120.0404900.0013740.2823180.000014−16.11.810.51958−0.961283
RZ104100.0481240.0017110.2823500.000014−14.90.900.50993−0.951339
RZ114190.0347570.0011740.2823340.000014−15.54.300.49862−0.961131
RZ123940.0283900.0009620.2822790.000014−17.42.110.50927−0.971250
RZ134120.0324150.0011070.2823600.000013−14.62.980.46910−0.971209
RZ143960.0335780.0011250.2823190.000013−16.04.680.47833−0.971090
RZ154180.0542880.0019870.2823170.000017−16.12.910.61922−0.941218
RZ163890.0084800.0002660.2822050.000016−20.13.120.58884−0.991183
Table 3. Major and trace element compositions of the Luotuoquan granites.
Table 3. Major and trace element compositions of the Luotuoquan granites.
SamplesMonzogranirteSyenogranite
PM03-2PM03-26PM03-41PM12-20PM17-4D5195D8373PM06-34
SiO271.0471.8074.9572.8074.1071.6076.0072.30
TiO20.290.320.140.290.120.490.180.17
Al2O314.2014.3013.2013.6014.1013.3012.1012.10
TFe2O32.412.611.112.571.083.631.701.86
MnO0.060.060.010.050.010.030.010.03
MgO0.550.630.270.410.300.620.070.63
CaO2.161.980.761.331.292.001.032.53
Na2O3.453.493.033.103.513.012.462.69
K2O4.294.025.594.934.874.034.894.89
P2O50.120.120.030.090.040.110.040.29
LoI1.520.770.760.920.511.231.432.48
Total100.07100.0799.85100.0399.99100.0699.9399.99
Rb211.0132.0167.0177.0215.0112.0114.0134.0
Ba406.0444.0398.0345.0466.0556.0499.0755.0
Th28.6011.5011.3020.7016.7029.2021.2024.80
U4.812.412.232.951.762.101.301.90
Ta1.100.760.901.080.800.810.400.72
Nb14.009.539.5611.5010.1015.105.1312.40
Sr90.5050.1060.4065.8084.5086.0059.0079.00
Zr333.0202.0245.0259.0236.0365.0147.0275.0
Hf10.906.988.408.908.0112.506.109.50
Y55.5257.8858.6443.6144.5147.4043.4037.70
Ga19.1018.2014.3017.0020.6025.4021.7017.20
La40.2825.9319.7547.5642.2393.6048.6068.20
Ce93.3056.6545.19108.983.71189.089.60140.0
Pr10.977.515.8714.3011.2025.6012.9019.20
Nd43.7731.1424.0655.8044.4794.9050.9074.00
Sm9.627.696.2511.469.1217.2011.5014.10
Eu1.130.960.861.371.001.221.181.20
Gd7.846.185.119.077.4515.109.3511.50
Tb1.611.441.331.621.422.111.531.80
Dy9.849.669.578.498.519.628.139.20
Ho1.871.891.891.501.531.641.501.70
Er4.684.724.753.753.814.564.354.00
Tm0.840.930.960.630.690.660.730.60
Yb4.875.525.383.574.113.984.673.70
Lu0.850.960.890.660.750.540.640.50
∑REE231.5161.2131.9268.7220.0459.7245.6349.7
LREE/HREE6.144.153.418.176.7811.006.959.57
δEu 0.390.410.450.400.360.230.340.27
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Chen, W.; Zhang, M.; Tao, G.; Li, X.; Yu, Q.; Fan, X.; Zhang, J. Ocean–Continent Conversion in Beishan Orogenic Belt: Evidence from Geochemical and Zircon U-Pb-Hf Isotopic Data of Luotuoquan A-Type Granite. Minerals 2023, 13, 1411. https://doi.org/10.3390/min13111411

AMA Style

Chen W, Zhang M, Tao G, Li X, Yu Q, Fan X, Zhang J. Ocean–Continent Conversion in Beishan Orogenic Belt: Evidence from Geochemical and Zircon U-Pb-Hf Isotopic Data of Luotuoquan A-Type Granite. Minerals. 2023; 13(11):1411. https://doi.org/10.3390/min13111411

Chicago/Turabian Style

Chen, Wenliang, Minjie Zhang, Guanghuo Tao, Xiaofeng Li, Qian Yu, Xiaojie Fan, and Jingwei Zhang. 2023. "Ocean–Continent Conversion in Beishan Orogenic Belt: Evidence from Geochemical and Zircon U-Pb-Hf Isotopic Data of Luotuoquan A-Type Granite" Minerals 13, no. 11: 1411. https://doi.org/10.3390/min13111411

APA Style

Chen, W., Zhang, M., Tao, G., Li, X., Yu, Q., Fan, X., & Zhang, J. (2023). Ocean–Continent Conversion in Beishan Orogenic Belt: Evidence from Geochemical and Zircon U-Pb-Hf Isotopic Data of Luotuoquan A-Type Granite. Minerals, 13(11), 1411. https://doi.org/10.3390/min13111411

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