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Article

Hadean–Neoarchean Crustal Evolution of the Northeastern North China Craton: Evidence Derived from the Zircon U–Pb–Hf Isotopes of Supracrustal Rock from the Jiapigou Terrane

by
Nan Tian
1,
Jilong Han
2,3,*,
Xueni Zhang
1,*,
Yong Zhang
1 and
Shu Wang
4
1
Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing 100037, China
2
Key Laboratory of Metallogenic Prediction of Nonferrous Metals and Geological Environment Monitoring, Central South University, Ministry of Education, Changsha 410083, China
3
State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, Beijing 100083, China
4
College of Earth Sciences, Jilin University, Changchun 130061, China
*
Authors to whom correspondence should be addressed.
Minerals 2026, 16(2), 176; https://doi.org/10.3390/min16020176
Submission received: 14 December 2025 / Revised: 25 January 2026 / Accepted: 28 January 2026 / Published: 6 February 2026
(This article belongs to the Special Issue Petrochronology of Zircon: Recent Development, Data Interpretation, and Implications)
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Abstract

The North China Craton (NCC), one of the oldest cratons worldwide, may provide information on the evolution and geodynamic processes of the early Earth, especially during the pre-Mesoarchean period. Many ancient zircons have been discovered in the Jiapigou terrane of the northeastern NCC on the basis of our recent studies, providing an excellent opportunity to trace the early crustal evolution trend of the NCC. Here, we present a detailed study of the petrography, mineralogy, zircon U–Pb dating and Lu–Hf isotopes of supracrustal rocks (biotite schist) obtained from the Jiapigou terrane. Geochronology combined with the internal structures and Th/U ratios of the zircons reveal that the zircons acquired from the supracrustal rock can be divided into the following two types: magmatic zircons and metamorphic zircons. Among the magmatic zircons, the youngest zircon age (2.49 Ga) is considered to represent the time at which the protolith of the supracrustal rock (i.e., Neoarchean) crystallized, whereas the others were likely captured or inherited from their magma sources. The zircon Hf isotopes reveal that unexposed Hadean–Paleoarchean crust (4.18–3.57 Ga) is present beneath the Jiapigou terrane, and its growth history can be traced back to the Hadean period. Moreover, the evidence derived from this and previous studies indicates that the Jiapigou terrane underwent two crustal recycling events (3.37–3.20 Ga and ~2.96 Ga) during the Paleoarchean, two crustal reworking episodes (2.53 Ga and 2.49 Ga) during the Neoarchean, and later metamorphism at 2.41 Ga. Thus, the Jiapigou terrane has undoubtedly recorded multiple episodes of early crustal growth and/or reworking that are similar to, but not limited to, those of the northern and southern margins of the NCC.

1. Introduction

The formation, composition, and evolution of ancient continental crust are frontier domains in Earth sciences, and research on these themes can provide important information about the evolution and geodynamic processes exhibited by the early Earth ([1,2,3,4] and the references therein). The oldest parts of the present-day continental crust are represented mainly by Archean cratons and crystalline basement [4,5]. Numerous studies have revealed that the formation scale of continental crust reached 70%–80% of the cratons (typified by tonalitic–trondhjemitic–granodioritic (TTG) gneisses, supracrustal rocks and K-rich granites) during the late Mesoarchean to the Neoarchean (3.0–2.5 Ga) ([4,6] and the references therein), making this period the most critical period for global crustal growth (i.e., [4,7,8,9]). The extremely limited records of the crustal evolution processes that occurred during the Eoarchean to the early Mesoarchean (4.0–3.0 Ga) are concentrated mainly in a few cratons, such as the Tanzania Craton in Tanzania [10], Zimbabwe Craton in Zimbabwe [11,12], Pilbara Craton in Australia [13,14], Bundelkhand, Singhbhum, Bastar and Dharwar cratons in India [15,16,17,18,19,20,21], gneiss terrane in Greenland [22], Kaapvaal Craton in South Africa [23] and North China Craton in China [24], and exhibit a progressive transition in their compositions from ultramafic–mafic rocks to TTG gneisses and then to K-rich granites [4,22], corresponding to the multistage evolution and growth of Archean cratons.
Globally, research on the evolution and formation models of the Hadean continental crust relies largely on detrital and/or xenocrystic zircons with ages older than 4.0 Ga derived from rare Archean cratons worldwide. For example, both detrital zircons in quartzites from the Limpopo Belt (4.01 Ga [10,25]) and from the Barberton Greenstone Belt (4.0~4.20 Ga [26,27]) are present in southern Africa. The detrital zircons from Mesoarchean quartzites in the Tanzania Craton (4.01 Ga [10]), detrital zircons from tonalitic orthogneiss in southern West Greenland (4.08 Ga [28]), detrital zircons from paragneiss in East Antarctica (4.05~3.94 [29]), and xenocrystic zircons from tonalitic gneiss in East India (4.24~4.03 Ga [30,31]). Both xenocrystic zircon hosted within amphibolite from the North China Craton (4.17 Ga [32]) and xenocrystic zircon within granodiorite from the Yangtze Block (4.1 Ga [33]) are present in China. Thus, compared with regions that are characterized by abundant rock exposures, areas with limited restricted pre-Neoarchean rock exposures pose a formidable challenge for exploration, and any new discoveries of ancient crustal material (especially Eoarchean rocks and/or Hadean zircons) significantly increase our understanding of Earth’s early evolutionary history.
As one of the oldest cratons (>3.8 Ga), the NCC has been the focus of investigations related to the Precambrian crustal evolution process (Figure 1, [34,35]). Many studies have revealed that the NCC formed at approximately 4.0–3.8 Ga (Figure 1 [4,7,34]). Recent research increasingly supports the establishment of crustal thickening and evolution at approximately 3.2 Ga [5,16,36,37], with global plate tectonics progressively established during the late Archean period (ca. 3.0–2.5 Ga [16,38,39,40,41,42]). The time of cratonization can differ, but the process of cratonization is essentially the same. The late Neoarchean tectono-magma event in the NCC was very strong, suggesting that it completed cratonization in the late Neoarchean (~2.5 Ga [4]). Detrital zircon grains with ages > 3.6 Ga were found in the southern and northeastern margins of the NCC (Figure 1B; i.e., the Anshan area (4.17 Ga [32]) and eastern Hebei (4.0–3.9 Ga [43]), indicating its multiphase episodic crustal growth. Nevertheless, this geological evidence regarding the Precambrian geological evolution of the NCC is mostly fragmented and has been reported from different locations [43]; additionally, in most cases, these studies generally lack isotopic evidence (i.e., Hf and O isotopes) for tracing the formation mechanism of the NCC. The Jiapigou terrane, which is located on the northeastern margin of the NCC, holds Neoarchean TTG gneisses and supracrustal rocks with ages ranging from 2.7–2.5 Ga ([44] and the references therein). In particular, a 3.8 Ga xenocrystic zircon hosted in the mafic dike of this district has been discovered [45], offering an opportunity to trace the Archean (especially pre-Mesoarchean) crustal evolution process of the NCC. Fortunately, substantial amounts of xenocrystic zircon grains with ages ranging from 3.57–2.96 Ga have been discovered in supracrustal rock derived from this district on the basis of our recent studies [9,45], providing an excellent opportunity to trace the early crustal evolution process of the NCC.
In this paper, we conduct detailed petrography, mineralogy, zircon U–Pb dating and Lu–Hf isotope studies of supracrustal rocks (biotite schist) acquired from the Jiapigou terrane. On the basis of our results and previous observations, we evaluate the episodes and mechanisms of crustal growth in the Jiapigou terrane and discuss their implications for the early crustal evolution process of the NCC.

2. Regional Geology and Sampling

Tectonically, the Jiapigou terrane comprises the northeastern margin of the NCC (locally named the Longgang terrane) and the eastern margin of the Central Asian Orogenic Belt (CAOB), and it is bordered by the NE-trending Huifahe fault and NW-trending Jinyinbie fault (Figure 2, [44]). This terrane may have experienced the formation of cratonic nuclei and cratonization during the Archean period [9,61], followed by metamorphism in the early Paleoproterozoic, as well as multiple tectonic transformation events since the Phanerozoic [9,44]. In the Jiapigou terrane, Archean units (Figure 2) are represented by extensive granitoid gneisses, supracrustal rocks of the Jiapigou Group and K-rich granites, along with ultramafic–mafic dikes. The supracrustal rocks of the Jiapigou Group occur mainly as lenticular xenoliths within granitoid gneisses and are composed mainly of ~2588–2536 Ma metavolcanic rocks (i.e., amphibolite and biotite schist) and metasedimentary rocks (i.e., felsic gneiss and magnetite-quartzite) [61,62]. Granitoid gneisses (2578–2524 Ma) are widely distributed in the Longgang terrane, consisting of TTG gneisses and granitic gneisses, and no distinct boundaries exist between the different lithofacies [9,61]. The granitoid gneisses and supracrustal rocks have undergone different degrees of greenschist–amphibolite facies metamorphism [9,44]. K-rich granites and ultramafic–mafic dikes with minor granodioritic gneiss formed during 2523–2480 Ma and intruded into the granitoid gneisses and supracrustal rocks [9,62]. In addition, the Archean units in the Jiapigou terrane host a dozen Mesozoic mesothermal gold deposits and were intruded by synchronic intrusions [44,63,64].
The supracrustal rock sampled in this study was obtained from the southern part of the Jiapigou terrane (Figure 2; location: 42°42′44.64″ N, 127°21′44.63″ E) and is composed mainly of biotite schist. It is approximately 15 m wide, extends in the NE direction, and occurs as lenticular xenoliths within the granodioritic gneiss (Figure 3A). The biotite schist has a schistose structure (Figure 3B,C), along with scaly granular metamorphic textures (Figure 3C), and mainly consists of biotite (30–35 vol%), plagioclase (35–40 vol%), quartz (15–20 vol%) and ilmenite (~5 vol%) (Figure 3C), with minor accessory zircon and apatite. Plagioclase and biotite have experienced alterations to different degrees, producing sericite and chlorite, respectively. The above petrographic characteristics of the biotite schist, coupled with the lack of remnant sedimentary texture, confirm its nature as a volcanic rock. Additionally, the biotite schist has been crosscut by later carbonate veins (Figure 3B).

3. Analytical Methods

Zircon separation was conducted at the Langfang Regional Geological Survey, Hebei Province, China, while cathodoluminescence (CL) images were obtained with a JEOL scanning electron microscope at Nanjing Hongchuang Exploration Technology Service Co. Ltd., Nanjing, China. After the CL images were obtained, the zircon grains were subjected to in situ U–Pb analyses. U–Pb analyses were performed using multicollector laser ablation inductively coupled plasma mass spectrometry (LA–ICP–MS) at the Key Laboratory of Mineral Resources Evaluation in Northeast Asia, Ministry of Natural Resources, Jilin University, China, and the Ministry of Natural Resources (MNR) Key Laboratory of Metallogeny and Mineral Assessment, Institute of Mineral Resources, Chinese Academy of Geological Sciences (CAGS), Beijing. Distinct domains within the zircon grains were selected for analysis purposes on the basis of the CL images. During the analyses, the spot size was 32 μm, and high-purity He gas was used to transfer the ablated materials. The NIST SMR610 glass [44] was used as an external standard for conducting a trace element analysis, while the 91500 and GJ-1 zircons [44] were used as the external standard for age calibration. Details on the employed procedural methods and instrumental settings can be found in the work of Song et al. [65] and Griffin et al. [66]. The isotope ratios and U–Pb ages were calculated using the GLITTER (Ver. 4.0, Macquarie University [67]) and Isoplot (Ver. 3.0 [68]) programs, respectively.
In situ zircon Lu–Hf isotope measurements were conducted with a Neptune Plus MC–ICP–MS instrument (Thermo Fisher Scientific, Dreieich, Germany) at the MNR Key Laboratory of Metallogeny and Mineral Assessment, Institute of Mineral Resources, CAGS, Beijing. Zircon Lu–Hf isotope measurements were performed on the same zircon grains that were previously analyzed for U–Pb dating, with the ablation pits measuring 32 μm. The reference zircon, i.e., Mud Tank (176Hf/177Hf = 0.282507 ± 6), and the standard zircon, namely, 91500, were used to monitor the performance conditions and analytical accuracy. All the Lu–Hf isotope results are reported with 2σ uncertainties. The instrumental conditions and data acquisition procedures were similar to those described by Hu et al. [69].

4. Results

4.1. Zircon U–Pb Ages

The zircon grains derived from the supracrustal rock (sample 20TD-1) were generally subrounded to rounded in shape and were 50–150 μm in length, with length/width ratios of 1:1–1:3 (Figure 4). Most zircon grains exhibit core-to-rim zoning, which is characterized by a common inherited core with oscillatory zoning and a structureless metamorphic rim (Figure 4). On the basis of the CL images, Th/U ratios and U–Pb ages, the zircons can be roughly divided into six groups: 3.57, 3.37–3.20, 2.96, 2.53, 2.49 and 2.41 Ga.
The zircon cores in Group 1 (3.57 Ga) exhibited oscillatory zoning and had Th/U ratios of 0.54–1.07 (Table 1), indicating a magmatic origin. The 207Pb/206Pb ages determined from the 5 analytical points in Group 1 ranged from 3632–3455 Ma and yielded a weighted mean age of 3565 ± 85 Ma (mean square weighted deviation (MSWD) = 8.0; n = 5; Figure 5). The zircon cores in Groups 2 and 3 (3.37–3.20 Ga and 2.96 Ga, respectively) had relatively homogeneous internal structures and Th/U ratios of 0.21–0.67, indicating that they were derived from mafic magma [3]. The 207Pb/206Pb ages determined from 3 analytical spots in Group 2 ranged from 3369–3198 Ma, whereas a single zircon age of 2960 Ma was obtained in Group 3 (Figure 4 and Figure 5). Despite the significant variation in the grain sizes of the zircons in Group 4 (2.53 Ga), their cores exhibited a magmatic origin characterized by weak zoning (Figure 4) and relatively high Th/U ratios (0.35–0.90) (Table 1). The 207Pb/206Pb ages determined from 8 analytical spots in Group 4 ranged from 2534–2521 Ma and yielded a weighted mean age of 2529±15 Ma (MSWD = 0.03; n = 8; Figure 5). The internal structures (Figure 4) and Th/U ratios (0.35–0.90; except for sample #7) of the zircon cores in Group 5 (2.49 Ga) were similar to those of Group 4. The 207Pb/206Pb ages determined from 5 analytical points in Group 5 yielded a weighted mean age of 2498±19 Ma (MSWD = 0.29; n = 5; Figure 5). Although the zircons of Group 6 (2.41 Ga) exhibited core–rim structures, they featured structureless metamorphic rims, residual cores (e.g., #14), and lower Th/U ratios (e.g., 0.05 of #16), indicating that they may have been extensively modified by metamorphic fluids. Therefore, the weighted mean age of 2409 ± 23 Ma (MSWD = 0.69; n = 3; Figure 5) obtained from this group can represent the timing of a metamorphic event.

4.2. Zircon Hf Isotopic Compositions

In situ Hf isotope analyses of the zircons derived from Groups 1–2 and 4–5 for the supracrustal rock (sample 20TD-1) are shown in Figure 6 and summarized in Table 2.
The zircons derived from the supracrustal rock had initial 176Hf/177Hf ratios of 0.2820408~0.281132. In accordance with the characteristics of the εHf(t) values and two-stage Hf model ages (TDM2), the Hf isotopic compositions of the zircons from Group 1 clearly defined two subgroups (Figure 4 and Figure 6A). One subgroup was characterized by high εHf(t) values and young TDM2 ages (εHf(t) = +4.1, TDM2 = 3.58 Ga), whereas the other subgroup exhibited low εHf(t) values and old TDM2 ages (εHf(t) = −2.9~−2.7, TDM2 = 4.18~4.16 Ga) (Table 2). Only one zircon from Group 2 had an εHf(t) value of +1.7 and a TDM2 value of 3.54 Ga (Table 2). The zircons derived from Groups 4–5 had lower εHf(t) values and younger TDM2 ages. The εHf(t) values of Groups 4 and 5 ranged from −1.3 to -4.3 and −3.1 to −4.4, respectively, whereas the TDM2 ages of these zircons ranged from 3.58–3.47 Ga and from 3.60–3.34 Ga, respectively (Table 2).

5. Discussion

5.1. Existence of Unexposed Hadean–Paleoarchean Crust Beneath the Jiapigou Terrane

Most Archean units in the Jiapigou terrane formed during the Neoarchean and are characterized by abundant granitoid gneisses (2578–2524 Ma [9,61]), supracrustal rocks (~2588–2536 Ma metavolcanic rocks [61,62]) and K-rich granites (2523–2480 Ma [9,62]) (Figure 2). Although no rocks older than the pre-Neoarchean have been found in the district thus far, a 3.8 Ga xenocrystic zircon hosted in the mafic dike within this district has been discovered [45], which sparked our interest in tracing the early crustal components.
The first three groups of zircon cores (≥2.96 Ga) derived from the supracrustal rock in this study exhibited oscillatory zoning (Figure 4) and high Th/U ratios (0.21–1.07; Table 1), indicating a magmatic origin. Given the absence of pre-Neoarchean geological units (i.e., intrusions and/or sedimentary rocks) within the Jiapigou terrane [9,44] and even in wider regions (i.e., the Helong, Tonghua, and Baishan areas [62,71]), it is unlikely that these zircons were captured from wall rocks in the shallow crust during the ascent of their primary magma. Instead, they were likely captured or inherited from their magma source [45,72], which allows us to better understand the early crust in the Jiapigou terrane by examining these valuable zircons obtained from the supracrustal rocks.
Two analyses of zircon cores (#10 and #S3) from Group 1 (3.57 Ga) revealed enriched Hf isotopes (εHf(t) = −2.9~−2.7) and ancient TDM2 ages (4.18~4.16 Ga), indicating that this zircon likely formed through the reworking of preexisting Hadean crustal materials. The TDM2 ages of 4.18–4.16 Ga determined for this zircon core reveal that the oldest continental crust in the Jiapigou terrane was extracted from the depleted mantle at least 4.18–4.16 Ga. Like Jiapigou, no Hadean rocks (>4.0 Ga) have been found in the interior and margins of the NCC [4]; however, several Hadean zircons have been reported in recent years, e.g., 4.17 Ga xenocrystic zircon from the Anshan area [32], 4.0–3.9 Ga detrital zircons from the eastern Hebei area [43], and 4.1–4.0 Ga detrital zircons from the southern margins of the NCC [57]. Combined with the above evidence, we thus speculate that the evolutionary history of the NCC can be traced back to the Hadean, when continental crust growth had already occurred in the Jiapigou terrane and other areas in the NCC.
Moreover, two analyses of other zircon cores (#12 and #S5; Figure 4) derived from this group revealed depleted Hf isotopes (εHf(t) = +4.1) and younger TDM2 ages (~3.58 Ga), which were close to the crystallization age (3.57 Ga). These results indicate that juvenile crustal growth occurred at ~3.58 Ga and that nearly simultaneous reworking occurred at ~3.57 Ga in the Jiapigou terrane. Furthermore, abundant 3.5 Ga rocks and/or detrital zircons are widely distributed in the northern and southern margins of the NCC, including the 3.8–3.1 Ga Hujiamiao Complex and the 3.5–3.4 Ga Waitoushan Complex in the Anshan–Benxi areas [73,74], 3.8–3.6 Ga granitoids from the Labashan Complex in the eastern Hebei area ([75] and the references therein) and 3.6–3.3 Ga detrital zircons from the Tietonggou Formation in the southern margin of the NCC [76]. Thus, the Paleoarchean was also a significant period for continental crustal growth in the NCC.
Combined with the above evidence, we propose that an unexposed Hadean–Paleoarchean crust (4.18–3.57 Ga) exists in the Jiapigou terrane and that it has undergone multiple episodes of crustal growth similar to, but not limited to, those of the northern and southern margins of the NCC.

5.2. Multiple Paleo–Neoarchean Crustal Reworking Events in the Jiapigou Terrane

The zircon cores of Groups 2–6 derived from the supracrustal rock in this study recorded five tectonic–thermal events at 3.37–3.20, 2.96, 2.53, 2.49 and 2.41 Ga.
Only one result of Group 2 (3.37–3.20 Ga) obtained in this study revealed that this zircon had depleted Hf isotopes (εHf(t) = +1.7) and a younger TDM2 age (3.54 Ga) (Table 2). The TDM2 age of 3.54 Ga for this zircon was close to the crystallization age of the zircons in Group 1 (3.57 Ga). This evidence indicates that the zircons of Group 2 likely formed through further reworking of Paleoarchean crustal materials (3.58–3.57 Ga). The third group of zircons (2.96 Ga) represents only a Mesoarchean tectonic–thermal event, as no Hf isotope data were obtained in this study.
As described above, the zircons of Group 5 (2.49 Ga) exhibited a magmatic origin and had the youngest age (2498 ± 19 Ma; Figure 5), which was considered to represent the crystallization timing of the protolith of the supracrustal rock (i.e., Neoarchean). Although the zircon age of Group 5 (2.49 Ga) was younger than that of Group 4 (2.53 Ga), both groups had similar enriched Hf isotopes (εHf(t) = −4.4~−1.3) and ancient TDM2 ages (3.60–3.34 Ga) (Table 2). Akin to Group 2, the TDM2 ages of 3.60–3.34 Ga for both groups were close to the crystallization age of the zircons from Group 1 (3.57 Ga), indicating that the zircons of Groups 4–5 likewise originated from multiple reworkings of Paleoarchean crustal materials (3.58–3.57 Ga). Rocks with ages similar to those of Groups 4–5 have been extensively identified in the Jiapigou terrane, including 2.58–2.52 Ga granitoid gneisses, 2.59–2.54 Ga metavolcanic rocks and 2.52–2.48 Ga K-rich granites ([9,62] and the references therein). However, the zircons in these rocks had depleted Hf isotopes (Figure 6A) and younger TDM2 ages (2.6–2.9 Ga; Figure 6B,C) ([62] and the references therein), which were completely different from those of the zircons derived from Groups 4–5, indicating that they likely originated from the reworking of Neoarchean juvenile crustal materials (2.6–2.9 Ga) and recorded the most significant crustal growth in this district (Figure 6B,C). In addition, the zircon age of 2.41 Ga determined from Group 6 (Figure 5) represents a regional metamorphic event, which was also recorded by late Archean units with metamorphic ages of 2.40–2.35 Ga in the Jiapigou terrane [62,77].
In summary, the evidence obtained from this work and previous studies indicates that the Jiapigou terrane underwent multiple episodes of crustal evolution during the Paleo–Neoarchean, including Paleoarchean crustal recycling events at 3.37–3.20 Ga and 2.96 Ga in the Paleo–Mesoarchean, multiple episodes of Paleo- and/or Neoarchean crustal reworking at 2.53 Ga and 2.49 Ga in the Neoarchean, and later metamorphism at 2.41 Ga.

6. Conclusions

Comprehensive zircon U–Pb and Lu–Hf isotope analyses of the supracrustal rock contained in the Jiapigou terrane, along with previous observations, yielded the following main conclusions.
(1)
The geochronology results, combined with the internal structures and Th/U ratios of the tested zircons, reveal that the zircons derived from the supracrustal rock can be divided into two types: magmatic zircons with ages of 3.57, 3.37–3.20, 2.96, 2.53, and 2.49 Ga and metamorphic zircons with ages of 2.41 Ga. For the magmatic zircons, the youngest zircon age (2.49 Ga) is considered to represent the crystallization timing of the protolith of the supracrustal rock (i.e., Neoarchean), whereas the others were likely captured or inherited from their magma sources.
(2)
In conjunction with the zircon Hf isotopes, we propose that unexposed Hadean–Paleoarchean crust (4.18–3.57 Ga) occurs beneath the Jiapigou terrane and that its growth history can be traced back to the Hadean period.
(3)
The evidence obtained in this work and in previous studies indicates that the Jiapigou terrane underwent multiple episodes of crustal evolution during the Paleo–Neoarchean, including Paleoarchean crustal recycling events from 3.37–3.20 Ga and at 2.96 Ga during the Paleo–Mesoarchean, multiple episodes of Paleo- and/or Neoarchean crustal reworking at 2.53 Ga and 2.49 Ga during the Neoarchean, and later metamorphism at 2.41 Ga.

Author Contributions

Conceptualization, N.T. and J.H.; methodology, N.T. and J.H.; software, N.T. and J.H.; validation, S.W.; formal analysis, S.W.; investigation, J.H., N.T. and S.W.; resources, J.H. and X.Z.; data curation, J.H.; writing—original draft preparation, N.T. and J.H.; writing—review and editing, X.Z. and Y.Z.; visualization, S.W.; supervision, J.H. and X.Z.; project administration, J.H. and X.Z.; funding acquisition, J.H. and X.Z. All authors have read and agreed to the published version of the manuscript.

Funding

This research was financially supported by the National Natural Science Foundation of China (Grant Nos. 42172095, 42303037, 42202068, and 42302103) and the China Postdoctoral Science Foundation (2023M743306) and the Chinese Geological Survey Programme (No. DD20242072) and was funded by the Open Research Fund Program of Key Laboratory of Metallogenic Prediction of Nonferrous Metals and Geological Environment Monitoring (Ministry of Education), Central South University (No. 2025YSJS09).

Data Availability Statement

The authors confirm that the data supporting the findings of this study are available in the manuscript. The data in this study are unpublished and have not been submitted to any other journal for review.

Acknowledgments

We are very grateful to the editor and two anonymous reviewers for their criticism and constructive comments and suggestions, which helped to significantly improve this paper.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. (A) Schematic tectonic map of the Eurasian continent (modified on the basis of the work of Kröner et al. [46]) showing the major tectonic entities and location of Figure 1B. (B) Tectonic map of the North China Craton showing the major Precambrian basement and the distributions of ancient zircons (modified based on the work of Zhao et al. [47] and Wang et al. [45]). The references for the chronological data presented in the map can be found in the work of Wang et al. [45], Wan et al. [48] and the references therein [24,32,49,50,51,52,53,54,55,56,57,58,59,60]. Abbreviations: CAOB—Central Asian Orogenic Belt.
Figure 1. (A) Schematic tectonic map of the Eurasian continent (modified on the basis of the work of Kröner et al. [46]) showing the major tectonic entities and location of Figure 1B. (B) Tectonic map of the North China Craton showing the major Precambrian basement and the distributions of ancient zircons (modified based on the work of Zhao et al. [47] and Wang et al. [45]). The references for the chronological data presented in the map can be found in the work of Wang et al. [45], Wan et al. [48] and the references therein [24,32,49,50,51,52,53,54,55,56,57,58,59,60]. Abbreviations: CAOB—Central Asian Orogenic Belt.
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Figure 2. Regional geological map of the Jiapigou terrane displaying the sampling position (modified according to the work of Han et al. [63]).
Figure 2. Regional geological map of the Jiapigou terrane displaying the sampling position (modified according to the work of Han et al. [63]).
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Figure 3. Representative photographs showing the features of the occurrence and petrographic characteristics of the supracrustal rock derived from the Jiapigou terrane. (A) Biotite schist occurs as lenticular xenoliths within the granodioritic gneiss. (B,C) Field and microscopy images of the studied biotite schist. Abbreviations: Pl—plagioclase; Bi—biotite; Qtz—quartz; Ilm—ilmenite.
Figure 3. Representative photographs showing the features of the occurrence and petrographic characteristics of the supracrustal rock derived from the Jiapigou terrane. (A) Biotite schist occurs as lenticular xenoliths within the granodioritic gneiss. (B,C) Field and microscopy images of the studied biotite schist. Abbreviations: Pl—plagioclase; Bi—biotite; Qtz—quartz; Ilm—ilmenite.
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Figure 4. Cathodoluminescence images and ages of representative analyzed zircons derived from the supracrustal rock of the Jiapigou terrane. The U–Pb dating and Lu–Hf spot data are denoted by red and yellow circles, respectively.
Figure 4. Cathodoluminescence images and ages of representative analyzed zircons derived from the supracrustal rock of the Jiapigou terrane. The U–Pb dating and Lu–Hf spot data are denoted by red and yellow circles, respectively.
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Figure 5. Zircon U–Pb concordia diagrams for the supracrustal rock derived from the Jiapigou terrane. (A) Group 1~6 zircon data; (B) Group 4~6 zircon data.
Figure 5. Zircon U–Pb concordia diagrams for the supracrustal rock derived from the Jiapigou terrane. (A) Group 1~6 zircon data; (B) Group 4~6 zircon data.
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Figure 6. Plot of εHf(t) versus zircon age (A) and histograms of the U–Pb ages (B) and TDM2 ages (C) of zircons derived from the supracrustal rock of the Jiapigou terrane. The early Precambrian crustal growth curves of the North China Craton are shown in (B,C). The published data for the TTG gneisses, supracrustal rocks and K-rich granites in the Jiapigou terrane are obtained from Guo et al. [61,62]. Calculation based on Belousova et al. [70] and Wang et al. [42].
Figure 6. Plot of εHf(t) versus zircon age (A) and histograms of the U–Pb ages (B) and TDM2 ages (C) of zircons derived from the supracrustal rock of the Jiapigou terrane. The early Precambrian crustal growth curves of the North China Craton are shown in (B,C). The published data for the TTG gneisses, supracrustal rocks and K-rich granites in the Jiapigou terrane are obtained from Guo et al. [61,62]. Calculation based on Belousova et al. [70] and Wang et al. [42].
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Table 1. Zircon U–Pb data obtained for the supracrustal rock acquired from the Jiapigou terrane via LA–ICP–MS.
Table 1. Zircon U–Pb data obtained for the supracrustal rock acquired from the Jiapigou terrane via LA–ICP–MS.
Sample No.GroupContent (ppm)Isotopic RatiosIsotopic Ages (Ma)
ThUTh/U207Pb/206Pb1s207Pb/235U1s206Pb/238U1s207Pb/206Pb1s207Pb/235U1s206Pb/238U1s
20TD-1-144409600.460.167170.0018311.008880.146910.477650.00608253018252412251727
20TD-1-263729030.410.156970.002178.429140.131800.389490.00518242323227814212124
20TD-1-343183550.900.166280.0022411.017570.169540.480590.00640252122252514253028
20TD-1-441502030.740.167460.0024411.096240.180950.480630.00655253224253115253029
20TD-1-541502790.540.167160.0023611.065510.176410.480160.00649252924252915252828
20TD-1-643555190.680.166850.0018611.062500.148940.480920.00616252619252813253127
20TD-1-75975090.190.164790.0018610.604160.143980.466740.00600250619248913246926
20TD-1-841321570.840.167090.0024511.043890.181080.479430.00657252924252715252529
20TD-1-941352650.510.167600.0020211.119640.157500.481260.00627253420253313253327
20TD-1-1012222071.070.307920.0047030.726890.527260.723840.01089351123351017351041
20TD-1-1152312650.870.162570.0021410.496970.157960.468380.00623248322248014247627
20TD-1-1211081700.640.333230.0038634.793510.482850.757410.01014363218363314363537
20TD-1-1341092340.470.166990.0020211.064370.157070.480630.00630252820252913253027
20TD-1-1461462710.540.156720.002169.453210.146890.437580.00588242123238314234026
20TD-1-1551673300.510.162310.0019810.513150.149940.469860.00616248020248113248327
20TD-1-1665912550.050.154250.001598.493490.107970.399460.00508239417228512216723
20TD-1-1711131810.620.310900.0051233.318030.759530.771480.01552351826358323368858
20TD-1-1851351840.730.162470.0024210.531250.174070.470260.00650248225248315248529
20TD-1-1952472800.880.162890.0021910.474190.160010.466510.00628248623247814246828
20TD-1-2023315230.630.261810.0027623.671340.304960.655970.00846325816325513325233
20TD-1-S122105890.360.254870.0064824.973201.153260.697300.01953319843327651339975
20TD-1-S221442160.670.281840.0035625.482010.510570.649550.01156336920332220322245
20TD-1-S31771420.540.299650.0074131.500661.328980.747580.01878345538351442359069
20TD-1-S431064950.210.219230.0056017.143100.535160.560230.01099296045293931286445
20TD-1-S511151670.690.325070.0060233.163411.044320.734190.01789359029357831354166
Table 2. In situ zircon Hf isotope data for the supracrustal rock acquired from the Jiapigou terrane.
Table 2. In situ zircon Hf isotope data for the supracrustal rock acquired from the Jiapigou terrane.
Sample NameAge (Ma)176Yb/177Hf2σ176Lu/177Hf2σ176Hf/177Hf2σ176Hf/177HfiεHf(0)εHf(t)TDM1 (Ma)TDM2 (Ma)fLu/Hf
20TD-1-125290.0276850.0000580.0007300.0000020.2811220.0000140.281087−58.4−2.929463479−0.98
20TD-1-325290.0204090.0001570.0006640.0000050.2810790.0000210.281047−59.9−4.329993600−0.98
20TD-1-525290.0590450.0004220.0022450.0000180.2811710.0000250.281063−56.6−3.829983553−0.93
20TD-1-825290.0267380.0003070.0008350.0000140.2811210.0000170.281081−58.4−3.129563498−0.97
20TD-1-1035650.0317110.0005240.0009560.0000210.2804800.0000160.280415−81.0−2.738264156−0.97
20TD-1-S335650.0418360.0003120.0015270.0000100.2805130.0000330.280408−79.9−2.938394176−0.95
20TD-1-1124890.0169970.0000740.0005490.0000030.2811240.0000170.281098−58.3−3.529313499−0.98
20TD-1-1235650.0335360.0002940.0011700.0000100.2806850.0000190.280604−73.84.135733583−0.96
20TD-1-S535650.0328310.0002660.0011940.0000080.2806880.0000170.280606−73.74.135713578−0.96
20TD-1-1325290.0216930.0001670.0007320.0000050.2811670.0000150.281132−56.8−1.328863341−0.98
20TD-1-S131980.0120630.0001050.0003910.0000020.2808030.0000150.280779−69.61.733463537−0.99
20TD-1-1824890.0828640.0019440.0030470.0000750.2812510.0000250.281106−53.8−3.129493473−0.91
20TD-1-1924890.0349210.0002640.0008710.0000050.2811120.0000150.281071−58.7−4.429713582−0.97
The 207Pb/206Pb ages of the zircon grains were used to calculate the values of εHf(t), TDM1 and TDM2.
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Tian, N.; Han, J.; Zhang, X.; Zhang, Y.; Wang, S. Hadean–Neoarchean Crustal Evolution of the Northeastern North China Craton: Evidence Derived from the Zircon U–Pb–Hf Isotopes of Supracrustal Rock from the Jiapigou Terrane. Minerals 2026, 16, 176. https://doi.org/10.3390/min16020176

AMA Style

Tian N, Han J, Zhang X, Zhang Y, Wang S. Hadean–Neoarchean Crustal Evolution of the Northeastern North China Craton: Evidence Derived from the Zircon U–Pb–Hf Isotopes of Supracrustal Rock from the Jiapigou Terrane. Minerals. 2026; 16(2):176. https://doi.org/10.3390/min16020176

Chicago/Turabian Style

Tian, Nan, Jilong Han, Xueni Zhang, Yong Zhang, and Shu Wang. 2026. "Hadean–Neoarchean Crustal Evolution of the Northeastern North China Craton: Evidence Derived from the Zircon U–Pb–Hf Isotopes of Supracrustal Rock from the Jiapigou Terrane" Minerals 16, no. 2: 176. https://doi.org/10.3390/min16020176

APA Style

Tian, N., Han, J., Zhang, X., Zhang, Y., & Wang, S. (2026). Hadean–Neoarchean Crustal Evolution of the Northeastern North China Craton: Evidence Derived from the Zircon U–Pb–Hf Isotopes of Supracrustal Rock from the Jiapigou Terrane. Minerals, 16(2), 176. https://doi.org/10.3390/min16020176

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