Abstract
A series of NE-to E-trending ductile shear zones are widely distributed in the Khondalite Belt, a Paleoproterozoic collisional orogen in the North China Craton. Available geochronological investigations have been mainly focused on metamorphic and magmatic events in the Khondalite Belt, but the deformation age of ductile shear zones remains poorly constrained. In this paper, we conducted field-based structural and U-Pb geochronological studies on the Helanshan ductile shear zones (HDSZ) and Qianlishan ductile shear zones (QDSZ) in the western Khondalite Belt. The results revealed that four pre-kinematic intrusions were reworked by the shear zones and yielded monazite U-Pb ages of 1954 ± 3 Ma, 1942 ± 10 Ma, 1925 ± 5 Ma and 1918 ± 4 Ma, suggesting that the HDSZ and QDSZ probably appeared at some time after ∼1918 Ma. In the HDSZ, a granitic mylonite gave titanite and apatite U-Pb ages of 1897 ± 32 Ma and 1866 ± 47 Ma. Similar apatite U-Pb ages of 1860 ± 78 Ma and 1823 ± 50 Ma were also reported from another two mylonitized rocks. Comparably, three mylonites from the QDSZ displayed apatite ages of 1878 ± 39 Ma, 1805 ± 16 Ma and 1801 ± 10 Ma. Notably, these titanite and apatite U-Pb ages of 1897–1801 Ma are in good agreement with those of 1904–1823 Ma obtained from zircon overgrowth rims in mylonites. We regard that the above-stated U-Pb ages of 1904–1801 Ma together recorded the timing of the shear zone activity in the western Khondalite Belt. Combined with previous structural and geochronological data, we propose that the post-collisional orogen-parallel ductile shear zones in the Khondalite Belt have developed at ca. 1.90–1.80 Ga.
1 Introduction
Assessment of the timing of high-temperature (T > 550°C) ductile shear zones has been one of the major challenges in geochronology, especially the early Precambrian shear zones that underwent long-term complex evolution history (; ; ; ; ; ; Zhang et al., 2022; ). Traditionally, K-Ar and Rb-Sr systems in K-bearing minerals (e.g., muscovite, biotite and hornblende) are used for medium-to low-temperature thermochronology, but they are easily perturbed by post-kinematic tectono-thermal events (; ; ). In contrast, U-Pb system is more effective to date shear zones under higher temperature conditions, and U-bearing minerals (e.g., zircon, monazite, titanite and apatite) are resistant to physical and chemical weathering (; ; ). In high-temperature shear zones, syn-kinematically (re) crystallized U-bearing minerals from mylonites have the potential to directly record the timing of shear deformation (; ; ). Additionally, zircon and monazite U-Pb geochronology is commonly applied to determine emplacement ages of pre-, syn- and post-kinematic intrusions in shear zones and adjacent blocks, which indirectly provide temporal constraints on shear zone activity (; ; ; ; ). Therefore, the integration of U-Pb ages from shear zone-related intrusions and mylonites can help to better understand the tectonic evolution of high-temperature ductile shear zones.
The Khondalite Belt has been proposed as an Orosirian collisional orogen in the northwestern North China Craton, one of the oldest continental blocks around the world (Figure 1; e.g.; Zhao et al., 2005; Zhao et al., 2012; Yin et al., 2009; Yin et al., 2011; ; Zhao and Zhai, 2013; ; Wei et al., 2023). This belt was inferred to result from the amalgamation of the Yinshan and Ordos Blocks at ∼1.95 Ga, and it experienced a protracted (>100 Myr) orogenic history, characterized by polyphase deformation, high-grade metamorphism and magmatism in the late Paleoproterozoic (Zhao et al., 2005; Zhao et al., 2012; Yin et al., 2020; Yin et al., 2023; ; ; ; ; Wu et al., 2024). Of particular interest is the development of a series of orogen-parallel ductile shear zones in the western Khondalite Belt (; ; ). However, available geochronological investigations were mainly focused on metamorphic and magmatic events in this region (e.g., Yin et al., 2009; Yin et al., 2011; Zhou and Geng, 2009; ; ; ; ; ; Wu et al., 2020; Wu et al., 2024), and comparatively the shear zone activity has attracted less attention. conducted biotite 40Ar/39Ar dating of a mylonite in the Helanshan Complex but failed to obtain a meaningful age. Recently, , carried out zircon U-Pb geochronological studies on mylonites in the western Khondalite Belt and interpreted that metamorphic ages of zircon overgrowth rims probably recorded the deformation age of shearing. There is still the problem whether these zircon U-Pb ages can solely represent the timing of shear zones. In this study, we conducted monazite, titanite and apatite U-Pb geochronology on shear zone-related intrusions and high-temperature mylonites in the Helanshan and Qianlishan Complexes. Combined with available data, these new results will shed light on the deformation history of the ductile shear zones in the western Khondalite Belt.
FIGURE 1
2 Geological setting and samples
The Khondalite Belt is regarded as a typical Paleoproterozoic continent-continent collisional orogen in the northwestern North China Craton, resulting from the final amalgamation of the Ordos Block in the south and the Yinshan Block in the north at ∼1.95 Ga (e.g., Zhao et al., 2005; Zhao et al., 2012; Yin et al., 2009; Yin et al., 2011; ; ; ; Wu et al., 2024; ). From west to east, this belt exposes the Helanshan, Qianlishan, Daqingshan-Wulashan and Jining Complexes (Figure 1; Zhao et al., 2005). Lithologically, these complexes are dominated by granulite-facies metasedimentary rocks, mainly including graphite-bearing sillimanite-garnet gneisses, felsic paragneisses, garnet-bearing quartzites, diopside-bearing marbles and calc-silicate rocks, collectively termed as “khondalites” (; Zhao et al., 2005; Zhai, 2022). The khondalites spatially occur in association with S-type granites, charnockites, tonalite-trondhjemite-granodiorite (TTG) gneisses and mafic granulites (; Zhao et al., 2005; Zhai, 2022). Available geochronological investigations unraveled that the protolith of the khondalites was approximately deposited at 2.00–1.95 Ga, and subsequently experienced high-grade metamorphism at 1.95–1.85 Ga (e.g., Xia et al., 2006a; Xia et al., 2006b; Wan et al., 2006; ; Wan et al., 2013; ; Yin et al., 2009; Yin et al., 2011; Zhou and Geng, 2009; ; ; ; ; ; ; ; ; ; Wang et al., 2017; ; Wu et al., 2020; Wu et al., 2024; ; ; Zhu et al., 2023). Noticeably, similar clockwise P-T paths with post-peak (near-) isothermal decompression have been obtained from medium- to high-pressure pelitic and mafic granulites, indicating orogenic processes that involved initial crustal thickening and then exhumation (e.g., Zhou et al., 2010; ; ; Yin et al., 2014; Yin et al., 2015; ; ; Xu et al., 2018; Xu et al., 2023; Wu et al., 2020). A series of orogen-parallel ductile shear zones are widespread throughout the Khondalite Belt, for example, the nearly E-W-striking Xiashihao-Jiuguan ductile shear zone in the Wulashan-Daqingshan Complex and the NE(E)-SW(W)-striking Xuwujia ductile shear zone in the Jining Complex (; ; ; Wang et al., 1999; ).
The Helanshan and Qianlishan Complexes are situated in the westernmost segment of the Khondalite Belt, and they were unconformably overlain by the Mesoproterozoic sedimentary rocks (the Changcheng-Jixian System) (Figure 2; ; Zhao et al., 2005; ). The Helanshan and Qianlishan Complexes contain typical rock assemblages of the khondalites, named the Helanshan and Qianlishan Group, respectively (Figure 2; ; Zhao et al., 2005; Yin et al., 2009; Yin et al., 2011). Available geochronological data reveal that U-Pb ages of detrital zircons from the Helanshan and Qianlishan Group mainly ranged from 2.20 Ga to 2.00 Ga, and yielded a single peak at ca. 2.03 Ga (e.g., Yin et al., 2009; Yin et al., 2011; ; ; ; Wu et al., 2020; Wu et al., 2024). Medium-to high-pressure pelitic and felsic granulites have been discovered in the studied area, and they mainly showed a major metamorphic age group at ca. 1.95 Ga (e.g., Yin et al., 2009; Yin et al., 2011; ; ; ; Xu et al., 2018; Xu et al., 2023; ; Wu et al., 2020; Wu et al., 2024). Multiple magmatic events in this region have been reported at ca. 2.06–2.00 Ga, 1.95 Ga, 1.93–1.90 Ga and 1.88–1.82 Ga (e.g., Yin et al., 2009; Yin et al., 2011; Yin et al., 2020; ; ; ; ; ; ). In addition, previous structural analyses show that NE- to E-trending ductile shear zones (i.e., HDSZ and QDSZ) commonly appeared in the Helanshan and Qianlishan Complexes, which are mainly characterized by intensive ductile deformation, high-temperature (T > 650°C) granitic, pelitic and felsic mylonites (; ; Yin et al., 2020; ; ; ; ).
FIGURE 2
Based on structural observations in the field, we have selected ten rock samples in the HDSZ and QDSZ for U-Pb geochronology, and the sample locations were presented in Figure 2. Of these, six samples were collected from high-temperature granitic mylonites (Samples 19HL03-1, 22HL08-3-1, 22HL10, 22QL13, 20QL02-1 and 22QL03-1). Their detailed outcrop descriptions and microtectonic features have been given in , . Other four samples (Samples 22HL08-5, 22HL15-3, 22QL10-2 and 22QL14) were collected from granitic dykes and plutons that have been variably reworked by the ductile shear zones (Figure 3), suggesting that they were pre-kinematic intrusions.
FIGURE 3
3 Analytical methods
Monazite, titanite and apatite have been extracted from ten rock samples by conventional heavy liquid and magnetic separation techniques. These grains were then handpicked, mounted in epoxy, polished and photographed in reflected and transmitted light. Subsequently, their internal textures were determined through cathodoluminescence (CL) and backscattered electron (BSE) images. U-Pb dating and trace element analyses were conducted by Laser Ablation Inductively Coupled Plasma Mass Spectrometry (LA-ICP-MS) at the Guangzhou Tuoyan Analytical Technology Co., Ltd., Guangzhou, China. Detailed analytical methods followed those described in and Xing et al. (2024). Test data were processed offline with the software Iolite4 (). Tera-Wasserburg diagrams and age calculations were made using IsoplotR (). The uncertainties on intercept age and weighted mean age were presented at the 95% confidence level (2σ). The monazite, titanite and apatite U-Pb data in this paper are provided in the Supplementary files (Supplementary Tables S1–S3).
4 U-Pb geochronology
4.1 Monazite from pre-kinematic intrusions
4.1.1 Sample 22HL15-3
Monazite from sample 22HL15-3 are euhedral in morphology and 150–200 μm in grain size. Meanwhile, these monazite grains mainly show gray homogeneous structures in the BSE images (Figure 4A). A total of eighteen analytical spots have been made in this sample, and the U-Pb data were presented in Supplementary Table S1. These spots yielded 207Pb/206Pb apparent ages from 1903 ± 23 Ma to 1931 ± 19 Ma, and they were plotted on the concordia line in the Tera-Wasserburg (T-W) diagram (Figures 4B,C). These data well defined a weighted mean 207Pb/206Pb age of 1918 ± 4 Ma (n = 18, MSWD = 0.71, Figure 4C).
FIGURE 4
4.1.2 Sample 22HL08-5
Monazite grains from sample 22HL08-5 are subhedral to anhedral in morphology, with sizes of 100–200 μm. BSE images reveal that most monazite grains are homogeneous, and some of them have low luminescent cores (Figure 4D). In this study, nineteen spots were analyzed on homogeneous zones of monazite grains. As shown in Supplementary Table S1 and Figures 4E,F, these data gave a weighted mean 207Pb/206Pb age of 1954 ± 3 Ma (MSWD = 0.74, n = 19).
4.1.3 Sample 22QL10-2
Monazite grains from sample 22QL10-2 generally show euhedral to anhedral in morphology, ranging in size from 50 to 100 μm. In the BSE images, they have homogeneous internal structures (Figure 5A). Fifteen monazite grains were analyzed in the sample and showed a weighted mean 207Pb/206Pb age of 1942 ± 10 Ma (n = 15, MSWD = 0.39, Figures 5B,C).
FIGURE 5
4.1.4 Sample 22QL14
Monazite from sample 22QL14 are euhedral to anhedral and vary from 50 to 150 μm in grain size. BSE images reveal that they displayed homogeneous gray structures (Figure 5D). A total of sixteen grains were conducted in this sample and yielded a weighted mean 207Pb/206Pb age of 1925 ± 5 Ma (n = 16, MSWD = 0.76, Figures 5E,F).
4.2 Titanite from granitic mylonite (Sample 19HL03-1)
Titanite in the sample 19HL03-1 are euhedral and vary from 50 to 150 µm in grain size. In the CL images, large titanite grains mainly contained dark cores with (out) some inclusions, surrounded by the luminescent homogeneous rims (Figure 6A). In contrast, small titanite grains displayed homogeneous internal structures (Figure 6A). A total of twenty-five spots were made on the titanite rims and homogeneous grains, and they defined a lower intercept age of 1897 ± 32 Ma in the T-W diagram (n = 25; MSWD = 0.9; Figure 6B; Supplementary Table S2).
FIGURE 6
4.3 Apatite from granitic mylonites
4.3.1 Sample 19HL03-1
The apatite in this sample are euhedral to subhedral in shape, with the grain size of 100–200 µm. Meanwhile, CL images reveal that apatite grains are low luminescent and inclusion-free (Figure 7A). As listed in Supplementary Table S3, fourteen data-points were performed on apatite from this sample, and they yielded a lower intercept age of 1866 ± 47 Ma in the Tera-Wasserburg diagram (n = 14; MSWD = 1.5; Figure 8A).
FIGURE 7
FIGURE 8
4.3.2 Sample 22HL08-3-1
Apatite grains separated from the sample 22HL08-3-1 (Figure 3C) are subhedral to anhedral and 50–150 µm in size. CL images reveal that almost all apatite grains in this sample are homogeneous (Figure 7B). Twenty-eight spots were analyzed in sample 22HL08-3-1, and these data defined a lower intercept age of 1860 ± 78 Ma in the Tera-Wasserburg diagram (n = 28; MSWD = 1.8; Figure 8B; Supplementary Table S3).
4.3.3 Sample 22HL10
Apatite grains are mainly euhedral to anhedral in morphology, with their grain size of 50–100 µm. Most of the apatite grains in this sample are homogeneous, and some of them have small dark cores (Figure 7C). Twenty-four spots were conducted on luminescent homogeneous zones of apatite grains, and yielded a lower intercept age of 1823 ± 50 Ma in the Tera-Wasserburg diagram (n = 24; MSWD = 0.86; Figure 8C; Supplementary Table S3).
4.3.4 Sample 22QL13
Apatite grains from sample 22QL13 are generally euhedral to anhedral in morphology, with grain sizes ranging from 50 to 100 µm. They commonly showed low-luminescent and homogenous internal structures (Figure 7D). As shown in Supplementary Table S3 and Figure 8D, sixteen data-points were obtained from sample 22QL13. They displayed a lower intercept age of 1878 ± 39 Ma in the T-W diagram (n = 16; MSWD = 0.5; Figure 8D).
4.3.5 Sample 20QL02-1
Most apatite grains in this sample (Figure 3F) are euhedral to subhedral, mainly with 200–250 µm in grain size. In the CL images, these apatite grains have low luminescent cores, surrounded by bright rims (Figure 7E). A total of thirty-two spots were analyzed on the apatite rims. In the Tera-Wasserburg diagram, these data yielded a well-constrained lower intercept age of 1805 ± 16 Ma (n = 32; MSWD = 1.8; Figure 8E; Supplementary Table S3).
4.3.6 Sample 22QL03-1
Apatite separated from the sample are euhedral and large, varying from 200 to 300 µm in grain size. CL images reveal that the apatite grains are characterized by clear core-rim textures, similar to those of Sample 20QL02-1 (Figures 7E,F). Meanwhile, thirty-four spots were totally made on high luminescent apatite rims, and they defined a well-constrained lower intercept age of 1801 ± 10 Ma in the Tera-Wasserburg diagram (n = 34; MSWD = 1.5; Figure 8F; Supplementary Table S3).
5 Discussion
5.1 Timing of orogen-parallel shear zones in the western Khondalite Belt
Based on detailed structural analyses, the crystallization ages of pre-, syn- and post-kinematic intrusions can place important constraints on the timing of development of HDSZ and QDSZ. As presented in Table 1 and Figure 9, we have summarized available shear zone-related geochronological data in the western Khondalite Belt. In the HDSZ, two pre-kinematic granitic dykes (Samples 22HL08-5 and 22HL15-3) were affected by ductile shear deformation and yielded monazite weighted mean 207Pb/206Pb ages of 1954 ± 3 Ma and 1918 ± 4 Ma (Figures 3A,B, 4). They were interpreted as emplacement ages of the dykes and provided a lower age limit of the shear zone activity. Similar ages of 1942 ± 10 Ma and 1925 ± 5 Ma were also obtained from the boudinaged and strongly folded dykes in the QDSZ (Samples 22QL10-2 and 22QL14; Figures 3D,E, 5). These monazite U-Pb ages of 1953–1918 Ma indicate that the HDSZ and QDSZ must have developed at some time after ∼1918 Ma (Figure 9). This inference is supported by magmatic zircon U-Pb ages of 1952–1920 Ma from pre-kinematic intrusions in studied area (Table 1; ; ). Two syn-kinematic granitic dykes have been reported in the HDSZ, and they showed zircon U-Pb ages of 1887 ± 21 Ma and 1871 ± 28 Ma (Figure 9; ). Notably, a post-kinematic undeformed leucocratic dyke clearly intruded the mylonites in the HDSZ, and it was dated at 1816 ± 28 Ma (), interpreted to approximately represent the upper bound of deformation age of shear zones. Taken together, the above-stated igneous zircon and monazite U-Pb ages of pre-, syn- and post-kinematic intrusions suggest that the ductile shear zone activity in the western Khondalite Belt took place at some time between 1918 ± 4 Ma and 1816 ± 28 Ma (Figure 9).
TABLE 1
| No.a | Sample | Rock type and structural feature | Age (Ma) | Typeb | n | MSWD | Interpretation | References |
|---|---|---|---|---|---|---|---|---|
| The Helanshan Complex | ||||||||
| 1 | 22HL15-2 | Sm-cutting undeformed leucocratic dyke in the DSZ | 1816 ± 28 | I/UI | 4 | 6.6 | Post-kinematic intrusion | |
| 2037–1949 | X/SG | 4 | - | Inheritance | ||||
| 2 | 22HL11-1 | Sm-parallel granitic dyke in the DSZ | 1871 ± 28 | I/UI | 5 | 3.4 | Syn-kinematic intrusion | |
| 2100–1934 | X/SG | 7 | - | Inheritance | ||||
| 3 | 22HL15-1 | Sm-parallel leucocratic dyke in the DSZ | 1887 ± 21 | I/UI | 5 | 10.1 | Syn-kinematic intrusion | |
| 2000–1938 | X/SG | 6 | - | Inheritance | ||||
| 4 | 22HL15-3 | Deformed leucocratic dyke in the DSZ | 1918 ± 4 | Mnz/WM | 18 | 0.71 | Pre-kinematic intrusion | This study |
| 5 | 22HL08-3-1 | Mylonitic granitic dyke | 1860 ± 78 | Ap/LI | 28 | 1.8 | Syn-kinematic metamorphism | This study |
| 6 | 22HL08-3 | Granitic dyke reworked by the DSZ | 1924 ± 5 | I/UI | 4 | 1.9 | Pre-kinematic intrusion | |
| 2063 ± 22 | X/SG | 1 | - | Inheritance | ||||
| 7 | 22HL10 | Boudinaged leucocratic dyke in the DSZ | 1823 ± 50 | Ap/LI | 24 | 0.86 | Syn-kinematic metamorphism | This study |
| 1826 ± 31 | M/UI | 6 | 6.8 | Syn-kinematic metamorphism | ||||
| 1934 ± 13 | I/UI | 5 | 5.7 | Pre-kinematic intrusion | ||||
| 2048 ± 25 | X/SG | 1 | - | Inheritance | ||||
| 8 | 22HL08-4 | Mylonitic granitic dyke | 1840 ± 13 | M/UI | 6 | 2.4 | Syn-kinematic metamorphism | |
| 1920 ± 24 | I/UI | 9 | 5.9 | Pre-kinematic intrusion | ||||
| 9 | 22HL08-5 | Granitoid pluton reworked by the DSZ | 1954 ± 3 | Mnz/WM | 19 | 0.74 | Pre-kinematic intrusion | This study |
| 10 | 19HL16 | Calc-mylonite in the DSZ | 1849 ± 29 | M/UI | 10 | 6.6 | Syn-kinematic metamorphism | |
| 1955 ± 14 | M/UI | 15 | 3.5 | Granulite-facies metamorphism | ||||
| 2110–2013 | D/SG | 15 | - | Inheritance | ||||
| 11 | HL07 | Mylonitic granitic pluton | 1866 ± 12 | M/UI | 33 | 1.6 | Syn-kinematic metamorphism | |
| 1951 ± 5 | I/WM | 6 | 0.22 | Pre-kinematic intrusion | ||||
| 12 | 19HL05 | Pelitic mylonite in the DSZ | 1888 ± 8 | M/UI | 31 | 4.5 | Syn-kinematic metamorphism | |
| 1943 ± 23 | M/UI | 16 | 2.0 | Granulite-facies metamorphism | ||||
| 2169–2040 | D/SG | 2 | - | Inheritance | ||||
| 13 | 19HL01-2 | Felsic mylonite in the DSZ | 1901 ± 7 | M/UI | 35 | 3.5 | Syn-kinematic metamorphism | |
| 1959 ± 15 | M/UI | 13 | 4.0 | Granulite-facies metamorphism | ||||
| 2053 ± 24 | D/SG | 1 | - | Inheritance | ||||
| 14 | 19HL03-1 | Mylonitic granitic pluton | 1866 ± 47 | Ap/LI | 14 | 1.5 | Syn-kinematic metamorphism | This study |
| 1897 ± 32 | Ttn/LI | 25 | 0.9 | Syn-kinematic metamorphism | This study | |||
| 1904 ± 11 | M/UI | 30 | 4.3 | Syn-kinematic metamorphism | ||||
| 1952 ± 19 | I/UI | 15 | 9.7 | Pre-kinematic intrusion | ||||
| 2067–2028 | X/SG | 2 | - | Inheritance | ||||
| The Qianlishan Complex | ||||||||
| 15 | 22QL03-1 | Mylonitic granitoid pluton | 1801 ± 10 | Ap/LI | 34 | 1.5 | Syn-kinematic metamorphism | This study |
| 1884 ± 12 | M/UI | 11 | 3.7 | Syn-kinematic metamorphism | ||||
| 1935 ± 18 | M/UI | 6 | 3.4 | Granulite-facies metamorphism | ||||
| 2044 ± 30 | I/UI | 5 | 4.2 | Pre-kinematic intrusion | ||||
| 16 | 20QL02-1 | Mylonitic granitoid pluton | 1805 ± 16 | Ap/LI | 32 | 1.8 | Syn-kinematic metamorphism | This study |
| 17 | 20QL02 | Granitoid pluton reworked by the DSZ | 2055 ± 17 | I/WM | 6 | 2.8 | Pre-kinematic intrusion | |
| 18 | - | Deformed meta-pelites | 1821 ± 32 | MIA | - | - | Shear zone-related process | Yan (1983) |
| 19 | N80-48 | Deformed meta-pelites | 1839 ± 10 | Bt/PA | - | - | Shear zone-related process | |
| 20 | 22QL13 | Mylonitic granitic dyke | 1878 ± 39 | Ap/LI | 16 | 0.5 | Syn-kinematic metamorphism | This study |
| 1902 ± 8 | M/UI | 9 | 2.0 | Syn-kinematic metamorphism | ||||
| 1947 ± 9 | I/UI | 5 | 1.9 | Pre-kinematic intrusion | ||||
| 21 | 22QL11 | Felsic mylonite | 1902 ± 26 | M/UI | 5 | 10.8 | Syn-kinematic metamorphism | |
| 2289–2016 | D/SG | 3 | - | Inheritance | ||||
| 22 | 22QL14 | Strongly folded granitic dyke in the DSZ | 1925 ± 5 | Mnz/WM | 16 | 0.76 | Pre-kinematic intrusion | This study |
| 23 | QL32-1 | Mylonitic granitic dyke | 1936 ± 28 | I/UI | 12 | 6.2 | Pre-kinematic intrusion | Yin et al. (2020) |
| 24 | 22QL10-2 | Boudinaged granitic dyke in the DSZ | 1942 ± 10 | Mnz/WM | 15 | 0.39 | Pre-kinematic intrusion | This study |
Summary of available shear zone-related geochronological data in the western Khondalite Belt.
Number also indicate the dating samples in Figure 9.
I, M, X and D denote igneous, metamorphic, xenocrystic and detrital zircon. Mnz, Ttn, Ap and Bt denote monazite, titanite, apatite and biotite. UI, LI, WM, SG, PA and MIA, indicate upper intercept age, lower intercept age, weighted mean age, single grain age, plateau age and mineral isochron age, respectively. Except for zircon single grain age (1σ), other ages are presented at 2σ.
Abbreviations: DSZ, ductile shear zone; MSWD, mean square weighted deviation.
FIGURE 9
Additionally, the timing of high-temperature ductile shear deformation (i.e., mylonitization) in the HDSZ and QDSZ can be also constrained by dating zircon, titanite and apatite from mylonites. reported that zircon metamorphic overgrowth rims from six mylonitized rocks in the HDSZ gave 207Pb/206Pb ages of 1904–1826 Ma (Table 1). Of particular interest is a 1952 ± 19 Ma granitic pluton underwent shear deformation to become mylonite (Sample 19HL03-1), and it contained zircon overgrowth rims with metamorphic ages of 1904 ± 11 Ma (). In the same sample, homogeneous grains and overgrowth rims of titanite gave similar age of 1897 ± 32 Ma (Figure 6). Meanwhile, apatite grains from this sample showed a younger lower intercept age of 1866 ± 47 Ma in the Tera-Wasserburg diagram (Sample 19HL03-1; Figures 7A, 8A). In the HDSZ, another two granitic dykes (1924 ± 5 Ma and 1934 ± 13 Ma; ) were affected by shear zone activity, and yielded apatite U-Pb ages of 1860 ± 78 Ma and 1823 ± 50 Ma (Samples 22HL08-3-1 and 22HL10; Figures 7B,C, 8B,C), of which the latter is coincident with metamorphic ages of 1826 ± 31 Ma from zircon rims in the same sample. Therefore, we believe that these U-Pb ages from zircon overgrowth rims, titanite and apatite together constrained the timing of the development of HDSZ at ca. 1904–1823 Ma (Figure 9).
In the QDSZ, a 1947 ± 9 Ma granitic dyke was subjected to the mylonitization and yielded U-Pb ages of 1902 ± 8 Ma and 1878 ± 39 Ma from zircon overgrowth rims () and apatite (Sample 22QL13; Figures 7D, 8D), respectively. Comparably, a metamorphic zircon U-Pb age of 1902 ± 26 Ma was also found in felsic mylonite in the Qianlishan Complex (). We regard that these ages of 1902–1878 Ma represented the timing of the onset of shear deformation of the QDSZ. In addition, an older 2044 ± 30 Ma granitoid pluton was observed to undergo regional high-grade metamorphism and coevally developed gneissosity at 1935 ± 18 Ma (). This gneissic pluton was subsequently reworked by a E-trending shear zone to become granitic mylonite, of which zircon overgrowth rims yielded a younger age group of 1884 ± 12 Ma (Sample 22QL03-1; ). Notably, apatite grains from this sample are characterized by core-rim textures (Figure 7F), and the rims were dated at 1801 ± 10 Ma (Figure 8F). A similar apatite U-Pb age of 1805 ± 16 Ma was reported from a granitic mylonite in another outcrop of the same shear zone (Sample 20QL02-1; Figures 7E, 8E). These apatite U-Pb ages of 1805–1801 Ma are largely consistent with the Rb-Sr mineral isochron age of 1821 ± 32 Ma (Yan, 1983) and biotite Ar-Ar age of 1839 ± 10 Ma (), obtained from deformed meta-pelites in studied area. Based on these data, we propose that the shear zone activity in the Qianlishan Complex probably continued to ∼1801 Ma (Figure 9). It is worth noting that the above-stated U-Pb ages from the QDSZ are comparable with those from the HDSZ, and they are further inferred to record the deformation age of the orogen-parallel shear zones in the western Khondalite Belt at ca. 1904–1801 Ma (Table 1; Figure 9).
5.2 Tectonic implications
Orogen-parallel ductile shear zones are conspicuous structures throughout the Khondalite Belt, and a robust reconstruction of temporal framework of these structures needs to combine geochronological data that were obtained from different segments of this belt by multiproxy approaches. In the Wulashan-Daqingshan Complex, several pre-kinematic gabbro and granitic dykes were reworked by the nearly E-trending ductile shear zones, four of which displayed magmatic zircon ages ranging from 1987 ± 19 Ma to 1951 ± 9 Ma (; Wan et al., 2013). In the Jining Complex, the Xuwujia norite dyke that underwent ductile shear deformation yielded a crystallization age of 1931 ± 8 Ma (; ). The above-stated emplacement ages of 1987–1931 Ma were largely comparable with those igneous zircon and monazite U-Pb ages of 1954–1918 Ma from intrusions that predated the HDSZ and QDSZ in the western Khondalite Belt (Table 1; Figure 9). These U-Pb ages were considered to provide a maximum age limit on the development of orogen-parallel shear zones at ∼1.92 Ga. Meanwhile, syn-kinematic granitic dykes with zircon U-Pb ages of 1887–1858 Ma were reported in the Helanshan and Wulashan-Daqingshan Complexes (; ). Later, a post-kinematic undeformed granitic dyke (1816 ± 28 Ma; ) intruded the mylonite in the HDSZ, constraining the minimum deformation age of shearing at ∼1.82 Ga. This inference is supported by the observation that the Xiashihao-Jiuguan shear zone in the Wulashan-Daqingshan Complex was cut by an 1819 ± 3 Ma undeformed granite (Wang et al., 1999). A similar magmatic zircon U-Pb age of 1822 ± 17 Ma from a post-kinematic granite was also obtained in this region (). Consequently, these available geochronological data from shear zone-related igneous rocks unravel that orogen-parallel shear zones have approximately developed in the period between ∼1.92 Ga and ∼1.82 Ga.
In addition to the HDSZ and QDSZ, previous investigations have conducted geochronological studies on the ductile shear zones in the Wulashan-Daqingshan Complex, and metamorphic zircons from five mylonites gave U-Pb ages between 1906 ± 13 Ma and 1853 ± 6 Ma (; Wan et al., 2013). A mylonitic metapelite in the Jining Complex consistently presented a metamorphic zircon U-Pb age of 1866 ± 22 Ma (). Comparably, these ages of 1906–1853 Ma showed similarities with those of 1904–1826 Ma and 1902–1884 Ma in the Helanshan and Qianlishan Complexes, respectively (; ). The zircon U-Pb data indicate that the ductile shear zones in the Khondalite Belt probably started to deform at ∼1.90 Ga. This is also evidenced by the titanite U-Pb age of 1897 ± 32 Ma from granitic mylonite in the HDSZ (Table 1; Figure 9). Moreover, postulated that the shear deformation was likely to begin at ∼1.89 Ga and continued to ∼1.81 Ga, inferred from three biotite Ar-Ar ages (1885 ± 20 Ma, 1819 ± 14 Ma and 1814 ± 13 Ma) from mylonites in the Wulashan-Daqingshan Complex. In this study, we obtained similar apatite U-Pb ages of 1878–1801 Ma from six mylonites in the HDSZ and QDSZ, of which the youngest two were dated at 1805 ± 16 Ma and 1801 ± 10 Ma (Table 1; Figure 9). Coupled with those Ar-Ar ages, we consider that they possibly constrained the end of the shear zone activity at ∼1.80 Ga. In summary, the above-stated geochronological data reveal that orogen-parallel ductile shear zones in the Khondalite Belt most likely developed at 1.90–1.80 Ga.
The Khondalite Belt has been considered as the result of the collision between the northern Yinshan Block and the southern Ordos Block, and the timing of the final amalgamation was constrained at ∼1.95 Ga, mainly evidenced by metamorphic ages of high-pressure pelitic and mafic granulites (e.g., Zhao et al., 2005; Zhao et al., 2012; Yin et al., 2009; Yin et al., 2011; Yin et al., 2023; ; ; ; ; Wu et al., 2020; ). Collision-induced Paleoproterozoic polyphase deformation have also been recognized in the Khondalite Belt (e.g., ; ; ; Yin et al., 2020; ; ). For instance, three major phases of deformation (D1–D3) were proposed in the western Khondalite Belt (; Yin et al., 2020; ; ). The D1 deformation primarily produced overturned to recumbent isoclinal folds at small scale, originally (sub-) horizontal penetrative transposition foliations and NNE-SSW mineral lineations, and these D1 structures were inferred to occur at some time from ∼1976 Ma to ∼1932 Ma (; Yin et al., 2020; ). The D2 deformation was featured by NW(W)-SE(E)-trending tight to open doubly plunging upright folds, and they probably developed in the period between ∼1932 Ma and ∼1899 Ma (; ). Subsequently, the D3 deformation gave rise to the development of nearly NE-to E-trending shear zones at ca. 1904–1801 Ma (; ; ; This study). Similar D1–D3 structures were commonly observed in the middle and eastern Khondalite Belt (e.g., ; ; ). Notably, the widespread D3-related ductile shear zones have intensively reworked the previous D1–D2 structures and influenced the main tectonic framework of the Khondalite Belt (; ; Yin et al., 2020; ; ; ; ). As mentioned above, these orogen-parallel ductile shear zones underwent long-term evolution at 1.90–1.80 Ga (Figure 9), probably related to post-collisional orogenic processes between the Yinshan and Ordos Blocks, and they have played an important role in accommodating post-collisional deformation and tectonic exhumation of the khondalites (e.g., ; ; ; Yin et al., 2020; ; ).
6 Conclusion
The nearly NE- to E-trending ductile shear zones commonly occurred in the Helanshan and Qianlishan Complexes of the western Khondalite Belt. Pre-kinematic intrusions yielded monazite U-Pb ages of 1953–1918 Ma, indicating that the shear zones probably appeared after ∼1918 Ma. Titanite and apatite U-Pb ages of 1897–1801 Ma were obtained from mylonites, considered to record the timing of shear zone activity. Combined with previous data, we proposed that the Khondalite Belt remarkably developed a series of post-collisional orogen-parallel ductile shear zones at 1.90–1.80 Ga.
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The original contributions presented in the study are included in the article/Supplementary Material, further inquiries can be directed to the corresponding authors.
Author contributions
HQ: Writing – original draft, Writing – review and editing, Conceptualization, Data curation, Funding acquisition, Investigation, Methodology, Supervision. ML: Investigation, Writing – original draft. CD: Investigation, Writing – original draft. SW: Funding acquisition, Investigation, Writing – original draft, Writing – review and editing.
Funding
The author(s) declare that financial support was received for the research and/or publication of this article. This study was supported by the Science & Technology Department of Sichuan Province (Grant No. 2024ZYD0085), National Natural Science Foundation of China (Grant No. 42302222), Leshan Normal University (Grant No. KYCXTD2023-2, KYPY2023-0006 and RC202009), Provincial Natural Science Foundation of Hunan (Grant No. 2024JJ6102) and the Scientific Research Fund of Hunan Provincial Education Department (Grant No. 22A0499).
Acknowledgments
The editors and reviewers are thanked for their helpful and constructive comments on the manuscript.
Conflict of interest
The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.
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Supplementary material
The Supplementary Material for this article can be found online at: https://www.frontiersin.org/articles/10.3389/feart.2025.1603597/full#supplementary-material
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Summary
Keywords
shear zone, mylonite, U-Pb geochronology, Orosirian, Khondalite Belt, North China Craton
Citation
Qiao H, Liu M, Dai C and Wu S (2025) Dating the Orosirian orogen-parallel shear zones in the western Khondalite Belt, North China Craton: new constraints from monazite, titanite and apatite U-Pb ages. Front. Earth Sci. 13:1603597. doi: 10.3389/feart.2025.1603597
Received
31 March 2025
Accepted
24 April 2025
Published
14 May 2025
Volume
13 - 2025
Edited by
Xiaoguang Liu, Shandong University of Science and Technology, China
Reviewed by
Chen Zhao, Shenyang Center of China Geological Survey, China
Qiang Shi, Liaoning Technical University, China
Updates
Copyright
© 2025 Qiao, Liu, Dai and Wu.
This is an open-access article distributed under the terms of the Creative Commons Attribution License (CC BY). The use, distribution or reproduction in other forums is permitted, provided the original author(s) and the copyright owner(s) are credited and that the original publication in this journal is cited, in accordance with accepted academic practice. No use, distribution or reproduction is permitted which does not comply with these terms.
*Correspondence: Hengzhong Qiao, qiaohzh@lsnu.edu.cn; Shangjing Wu, wushj25@hynu.edu.cn
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