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Article

Late Paleozoic–Mesozoic Tectonic Evolution of the Mudanjiang Ocean: Constraints from the Zircon U-Pb and Ar-Ar Chronology of the Heilongjiang Complex, NE China

by
Jianxin Xu
1,2,3,4,
Peiyuan Hu
1,*,
Wendong Wang
2,3,
Hongyu Guo
2,3 and
Xin Zhang
2,3
1
Institute of Geology, Chinese Academy of Geological Sciences, Beijing 100037, China
2
Harbin Center for Integrated Natural Resources Survey, China Geological Survey, Harbin 150086, China
3
Observation and Research Station of Earth Critical Zone in Black Soil, Harbin, Ministry of Natural Resources, Harbin 150086, China
4
Northeast Geological S&T Innovation Center of China Geological Survey, Shenyang 110034, China
*
Author to whom correspondence should be addressed.
Minerals 2025, 15(5), 517; https://doi.org/10.3390/min15050517
Submission received: 26 February 2025 / Revised: 12 May 2025 / Accepted: 13 May 2025 / Published: 14 May 2025
(This article belongs to the Special Issue Geochronological Methods Applied to the Exploration of Tectonic and Geological Processes)
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Abstract

:
The Heilongjiang Complex provides a crucial geological record of the evolutionary history of the Mudanjiang Ocean, making it significant for understanding the accretion process between the Jiamusi Block and the Songliao Block. In this study, we analyzed samples from the Heilongjiang Complex in the Huanan region using zircon U-Pb and 40Ar/39Ar isotopic dating. The LA-ICP-MS U-Pb dating results show that the deposition time of the mica quartz schist is Late Triassic (237–207 Ma), while the protolith age of the amphibolite is Middle Triassic (245.5 ± 1.2 Ma). Detrital zircon ages from the mica quartz schist reveal four groups: 155–229 Ma, 237–296 Ma, 485–556 Ma, and 585–2238 Ma. The provenances are related to the magmatic and metamorphic activities at the junction of the Jiamusi Block and Songliao Block. 40Ar/39Ar isotopic dating yielded a plateau age of 183.40 ± 1.83 Ma for phengite in the mica quartz schist, with the metamorphic ages obtained from zircon U-Pb dating. We identify three major metamorphic events in the Heilongjiang Complex: (1) ~229 Ma, marking the earliest tectonic thermal disturbance in the complex; (2) 207–202 Ma, corresponding to the metamorphic event related to the collision between the Jiamusi Block and Songliao Block; and (3) ~183 Ma, indicating the closure of the Mudanjiang Ocean. Integrating these new findings with the results of previous research on magmatism and metamorphism, we reconstruct the tectonic evolution of the Mudanjiang Ocean from the Late Paleozoic to the Mesozoic. During the Early Permian, the Mudanjiang Ocean had already opened. Between the Middle Permian and Middle Triassic, bidirectional subduction occurred. In the Late Triassic, the Mudanjiang Ocean entered a subduction dormancy period. By the Early to Middle Jurassic, the Mudanjiang Ocean closed due to continental collision, leading to the final positioning of the Heilongjiang Complex.

1. Introduction

The Northeast China region is in the eastern segment of the Central Asian Orogenic Belt, situated between the Siberian Craton, the North China Craton, and the Western Pacific Plate, characterized by the interweaving of several microcontinents and suture zones. It comprises the Jiamusi–Khanka, Songliao, Xingan, and Erguna blocks (Figure 1, [1,2]). The Jiamusi Block, positioned at the easternmost edge of Northeast China, marks the site of direct interaction between the subduction of the ancient Pacific Plate and adjacent microcontinents. It is a core region for the superposition and transition of multiple ancient oceanic tectonic domains [3]. The “Mudanjiang Ocean”, which developed between the Jiamusi Block and Songliao Block from the Late Paleozoic to Mesozoic, records the processes of rifting and accretion between these two continents [4,5]. The ocean was later influenced by the westward subduction of the ancient Pacific Plate, eventually leading to collision and closure [6,7]. Therefore, understanding the evolutionary process of the Mudanjiang Ocean is essential for reconstructing the tectonic history of the amalgamation of the Jiamusi Block with the Songliao Block.
The Heilongjiang Complex, located at the western edge of the Jiamusi Block, has undergone metamorphism from greenschist to lower-amphibolite facies. It is considered to preserve crucial geological records of the subduction and closure of the Mudanjiang Ocean [9,10]. Chronological reveals that the protoliths of the complex were formed during the Late Paleozoic to Early Mesozoic. Among them, the rocks representing residual oceanic crust, such as blueschist, metamorphic basalt, and metamorphic gabbro, provide the crystallization age between 288 and 250 Ma [4,11,12]. These results confirm that the rifting of the Mudanjiang Ocean had already occurred by the Permian. U-Pb dating of detrital zircons from mica quartz schist (230–170 Ma) indicates that the ocean basin persisted into the Late Triassic to Early Jurassic [13,14]. Geochronology of metamorphic rocks further constrains the final closure of the Mudanjiang Ocean to the Early–Middle Jurassic (190–145 Ma) [15,16,17]. Geophysical data reveal a westward subduction direction [18], and the north–south trending arc-related igneous rocks along the western edge of the Jiamusi Block and the eastern edge of the Songliao Block provide further support for a bidirectional subduction model [19,20]. Given the Heilongjiang Complex’s importance in understanding the amalgamation history of the Jiamusi Block and Songliao Block, for the purposes of this study, samples were collected from the Heilongjiang Complex in the Huanan area of Jiamusi. Zircon U-Pb and 40Ar/39Ar isotopic dating were applied to mica quartz schist and amphibolite to investigate the protolith ages and tectonic thermal events, offering new insights into the tectonic evolution of the Mudanjiang Ocean.

2. Geological Background and Sample Descriptions

The Jiamusi Block, located in the eastern part of Heilongjiang Province, is bordered to the west by the Mudanjiang Fault, which separates it from the Songliao Block; to the east by the Yujinshan Fault, connecting it with the Nadanhada terrane; and to the south by the Dunmi Fault, which separates it from the Khanka Block. The block extends northward into Russia (Figure 2a). It is characterized by a typical double-layered structure of microcontinent, with exposed geological units including the Mashan Complex, Heilongjiang Complex, Paleo-Mesozoic granitic rocks, and sedimentary rock sequences [2,6]. The Mashan Complex, which serves as the metamorphic basement of the Jiamusi Block, is distinguished by the presence of graphite, serpentine, and garnet, suggesting its protoliths belong to the Khondalite Series. The sedimentation period of Mashan Complex ranges from 1900 to 900 Ma, with metamorphism occurring around 500 Ma during the late Pan-African orogeny [21,22,23]. Granitic rocks are widely distributed across the Jiamusi Block, with Early Paleozoic granites (541–484 Ma) originating from Pan-African magmatism, forming a metamorphic crystalline basement alongside the Mashan Complex. Permian granites (270–254 Ma) typically display arc-related characteristics, while Mesozoic igneous rocks are products of the westward subduction of the ancient Pacific Ocean [24,25,26].
The Heilongjiang Complex, forming in an N-S trending zone along the Mudanjiang Fault, is exposed mainly in the Luobei–Jiayin, Yilan–Huanan, and Mudanjiang–Muling areas (Figure 2a). The main rock units of the Heilongjiang Complex include blueschist, amphibolite, greenschist, meta-sedimentary rocks, serpentinite, metasilicalite, and marble [6,9]. Blueschist occurs in the Yilan and Mudanjiang areas, often preserving pillow structures. The protolith age of the Yilan blueschist is mainly Permian, while that of the Mudanjiang blueschist may be Triassic, with geochemical characteristics of OIB and E-MORB [9,11,16]. The protolith of the amphibolite primarily formed in the Permian, with reports of Triassic and Jurassic ages as well, reflecting various interpretations such as arc-related, MORB, and continental rift characteristics [5,16,27,28]. The protolith of the greenschist formed in the Middle Jurassic (162 ± 3.9 Ma) and is characterized by oceanic island attributes [27]. Meta-sedimentary rocks are the most significant rock units of the Heilongjiang Complex, primarily consisting of mica schist and quartz schist, with some local preservation of sedimentary layering indicative of sedimentary origin [28], forming in the forearc basin environment [14]. Current research on serpentinite, metasilicalite, and marble remains limited to their petrographic characteristics. Zhang identified siliceous rocks containing radiolarians in the Yilan Heilongjiang Complex, suggesting that they should belong to the oceanic crustal components [29]. Therefore, the Heilongjiang Complex is composed of various rocks with different origins and tectonic backgrounds, structurally mixed together, accompanied by intense metamorphic deformation [6,9,30].
The Heilongjiang Complex exposed in the Huanan area is in fault contact with the Late Permian granite and the Neoproterozoic Dapandao Complex, and is unconformably covered by sandstone of the Upper Cretaceous Houshigou Formation (Figure 2b). According to the deformation characteristics and material composition of the complex, it can be divided into matrix and rock blocks; the matrix is mainly composed of mica quartz schist (Figure 3a), which has undergone mylonitization. Rock blocks are mainly composed of amphibolite, greenschist, metasilicalite, marble, and serpentinite mixed in the matrix. The amphibolite is mainly blocky (Figure 3b), with locally developed folds. Marble is interbedded with amphibolite or greenschist (Figure 3c,d), exhibiting characteristics of oceanic island rock assemblages. Metasilicalites are generally observed as rock blocks (Figure 3e), and serpentinite is in fault contact with rocks on both sides (Figure 3f). These units have experienced multiple phases of intense metamorphic deformation due to thrusting and shearing. This study collected five samples of mica quartz schist and two samples of amphibolite in the Huanan area; details of the samples are listed in Table S1. The mica quartz schist shows a lepidoblastic texture and schistose structure, with quartz (50%), muscovite (20%), biotite (15%), albite (10%), and garnet (5%). Quartz is a banded aggregate alternating with muscovite and biotite (Figure 3g). The amphibolite has a crystalloblastic texture and schistose structure, and contains hornblende (75%), plagioclase (20%), and quartz (5%). Plagioclase appears granular or lenticular (Figure 3h).

3. Analytical Methods

3.1. LA-ICP-MS Zircon Dating

Zircon separation was conducted at the Hebei Regional Geological Survey and Research Institute. Under the microscope, larger and well-formed zircon grains were selected. Zircon LA-ICP-MS U-Pb dating was performed at the Tianjin Geological Survey Center, utilizing the 19 nm ArF excimer laser ablation system (RESOLUTION LR, produced by Australian Scientific Instrument Pte Ltd. in Singapore) and the Inductively Coupled Plasma Mass Spectrometer (ICP-MS, Agilent 7900, produced by Thermo Fisher Scientific in Waltham, MA, USA). Helium gas was used as the carrier gas for the ablated material. The laser beam diameter for the U-Pb age determination was set at 35 μm, with an ablation time of 30 s. Zircon standard 91500 and glass standard SRM 610 from the National Institute of Standards and Technology were selected as external standards for isotope and trace element fractionation correction. The test data were completed using ICPMSDataCal 10.9 software. The U-Pb age concordia diagrams and age-weighted average calculations for zircon samples were performed using Isoplot software (Ver 2.49).

3.2. 40Ar/39Ar Dating

Mineral composition analyses in the thin section (HN23005) were performed using an electron probe microanalyzer (EPMA; JEOL JXA-8230, produced by JEOL Ltd. in Tokyo, Japan) at the Key Laboratory of Mineral Resources Evaluation in Northeast Asia, Ministry of Natural Resources, Jilin University, Changchun, China. The EPMA was operated with an accelerating voltage of 15 kV, a beam current of 10 nA, and a beam diameter of 1–5 μm. Calibration utilized 53 certified reference materials from SPI Supplies® in West Chester, PA, USA, ensuring analytical precision with relative standard deviations (RSDs) below 2% for major elements. Mineral end-member calculations were processed using the AX program.
A sample (Ar2301) of mica quartz schist, characterized by intense deformation and well-developed foliation, was collected. The selection of single-mineral muscovite was carried out at the Yuheng Mining and Rock Technology Service Co., Ltd. in Langfang, China. The purified muscovite was then sent to the Chinese Academy of Geological Sciences for 40Ar/39Ar testing. Every cleaned sample and neutron fluence monitor were wrapped in aluminum foil and then arranged in one aluminum foil tube. Several aluminum foil tubes were sealed into a quartz bottle to be irradiated by fast neutrons for 1681 min in the nuclear reactor. The monitor irradiated together with the samples is an internal standard named Fangshan biotite (ZBH-25), with a reference age of 132.7 ± 1.2 Ma, and its potassium content is 7.6%. After irradiation, the samples needed to be left in the nuclear reactor for about three months to reduce the radiation. After being taken to the lab, the samples and standards were loaded into the sample holder and connected to the vacuum system. Then, the vacuum system was pumped, with the pipe and furnace heated to obtain an ultrahigh vacuum. When the blank met the requirement, the analysis could be carried out. The samples were heated by a graphite furnace. The heating–extraction duration for each temperature was 10 min, and then the released gases were purified by Zr/Al getter pumps for 10–15 min. After the purification, the gases were analyzed by the noble gas Mass Spectrometer GV Helix MC. The correction factors of interfering isotopes produced during irradiation were determined by analysis of irradiated pure K2SO4 and CaF4. The calculations of 40Ar/39Ar data were performed by the software ArArCALC (v2.5.2).

3.3. Major and Trace Elements

The analysis of major and trace elements in whole rocks was conducted by the laboratory of the Harbin Center of Natural Resources Integrated Survey. The major elements were analyzed using X-ray fluorescence spectrometry (XRF), and the instrument was PANalytical from the Almelo, The Netherlands, with the testing standard DZ/T 0279.1-2016. Trace element analysis was performed using Inductively Coupled Plasma–Mass Spectrometry (ICP-Ms), and the instrument was Thermo Fisher Scientific from USA, with the testing standard DB/T 14506.30-2010. Detailed descriptions of the methods can be found in [31].

4. Analytical Results

4.1. Zircon U-Pb Dating

Zircon U-Pb dating was conducted on four samples of mica quartz schist and two samples of amphibolite from the Huanan region. The analytical results are shown in Supplementary Table S2.
(1) Mica quartz schist (Sample HN23005, Figure 4a): The zircon grains are predominantly euhedral to subhedral, with some exhibiting rounded shapes, and their sizes range from 200 to 300 μm. The oscillatory zoning is well developed, and the Th/U is between 0.06 and 1.62. Some zircon grains display core–rim structures, indicating that the majority of the zircons are of magmatic origin, and some have been affected by subsequent metamorphic processes [32]. A total of 60 spots were measured, with 7 spots excluded for being discordant. The zircon ages of remaining spots range from 237 to 1317 Ma, revealing three main age groups: Permian–Triassic (237–296 Ma, age peak at ~258 Ma, accounting for 35%); Cambrian (493–556 Ma, age peak at 527.7 ± 7.5 Ma, 28.33%); Neoproterozoic (656–999 Ma, age peak at ~930 Ma, 25%). Additionally, a single concordant age of 1317 Ma is obtained. Notably, the Late Triassic–Early Jurassic zircon ages (214–175 Ma) of the four spots deviating from the concordia may relate to later tectonic thermal events (Figure 4a).
(2) Mica quartz schist (Sample HN23012, Figure 4b): The zircon grains exhibit irregular to rounded shapes, with sizes predominantly ranging from 100 to 150 μm, although some can reach up to 300 μm. Most zircon grains are poorly developed or lack oscillatory zoning. The Th/U is between 0.01 and 1.75. A total of 60 spots were measured, with 4 spots excluded for being discordant. The remaining spots are divided into two groups of concordant ages: The first group consists of 11 spots with ages ranging from 255 ± 2 to 264 ± 4 Ma, yielding a weighted mean age of 259.8 ± 2.1 Ma (MSWD = 1.3). The zircons in this group are relatively large and exhibit some development of magmatic oscillatory zoning, with the Th/U between 0.21 and 0.65, indicative of typical magmatic hydrothermal zircon. The second group includes 45 spots with ages ranging from 485 ± 4 to 502 ± 4 Ma, yielding a weighted mean age of 491.6 ± 1.4 Ma (MSWD = 0.74). The zircon grains in this group are generally smaller, with poorly developed magmatic oscillatory zoning and well-defined core–rim structures, and the Th/U is mostly < 0.1, suggesting a metamorphic origin.
(3) Mica quartz schist (Sample HN23017, Figure 4c): The zircon grains exhibit irregular to rounded shapes, with sizes ranging from 100 to 150 μm. The oscillatory zoning is relatively well developed, and the Th/U is between 0.03 and 1.68, with some zircon grains displaying core–rim structures and wider metamorphic rims. A total of 70 spots were measured, excluding one erroneous data spot. The zircon ages of remaining spots range from 155 to 2238 Ma, revealing four main age groups: Mesozoic (155–249 Ma, accounting for 71.43%), Paleozoic (275–480 Ma, 8.57%), Cambrian (496–529 Ma, 2.85%), and Neoproterozoic (634–2238 Ma, 15.71%). The Mesozoic ages can be further divided into two groups: the first group consists of six spots with ages ranging from 236 ± 3 to 249 ± 6 Ma, yielding a weighted mean age of 237.8 ± 6.7 Ma (MSWD = 1.4). The zircons in this group exhibit developed magmatic oscillatory zoning, with the Th/U between 0.16 and 1.34, characteristic of typical magmatic zircon, representing the youngest sedimentary age. The second group includes 43 spots with ages ranging from 155 ± 1 to 229 ± 3 Ma, showing poorer concordance. Most spots fall outside the concordial curve, and the intersecting discordant line with the concordial curve yields an interception age of 207.9 ± 3.5 Ma, representing the metamorphic age.
(4) Mica quartz schist (Sample HN23035, Figure 4d): The zircon grains are predominantly subhedral to rounded, with sizes ranging from 100 to 200 μm. The oscillatory zoning is well developed, and the Th/U is between 0.1 and 1.25, indicating a magmatic origin for the zircon. Most zircon grains exhibit core–rim structures, with narrow metamorphic rims that preclude the determination of metamorphic ages. A total of 60 spots were measured, all of which are distributed along and near the concordial line. The zircon ages range from 254 to 1812 Ma, revealing three main age groups: Permian (254–263 Ma, age peak at of 259.5 ± 4.7 Ma, accounting for 8.33%); Cambrian (492–501 Ma, age peak at 498.4 ± 1.4 Ma, 71.66%); Neoproterozoic (585–977 Ma, 16.66%). Additionally, single concordant ages of 430 Ma and 1812 Ma are obtained.
(5) Amphibole (Sample HN23050, Figure 5a): The zircon grains exhibit subhedral to tabular shapes, with sizes ranging from 50 to 120 μm. The oscillatory zone is well developed, and the Th/U is between 0.04 and 0.7 (mostly > 0.1), indicating a magmatic origin for the zircon. Some grains also display narrow metamorphic rims. A total of 40 spots were measured, with 7 spots excluded for being discordant. Twenty-nine spots yielded relatively consistent concordant ages ranging from 241 ± 3 to 252 ± 5 Ma, with a weighted mean age of 245.5 ± 1.2 Ma (MSWD = 0.47), representing the crystallization age of the amphibole. Additionally, single concordant ages of 368, 497, 519, and 1609 Ma are obtained, reflecting the ages of the captured zircon grains.
(6) Amphibole (Sample HN23039, Figure 5b): The zircon grains exhibit irregular to rounded shapes, with sizes ranging from 50 to 100 μm. Some grains display core–rim structures, while oscillatory zoning is not developed. The Th/U is between 0.01 and 0.60 (mostly < 0.1), indicating that the zircon has undergone subsequent metamorphic alteration. A total of 40 spots were measured, excluding 4 spots that fell outside the concordial curve (spots 4, 7, 19, and 22) and 1 spot representing a captured zircon age (365 Ma). The remaining spots yielded ages ranging from 200 ± 2 to 233 ± 3 Ma, which can be further divided into two groups: The first group consists of 25 spots with ages ranging from 227 ± 5 to 233 ± 3 Ma, yielding a weighted mean age of 229.9 ± 1.3 Ma (MSWD = 0.32), with Th/U between 0.01 and 0.60. The second group includes 10 spots with ages ranging from 200 ± 2 to 205 ± 15 Ma, with a weighted mean age of 202.2 ± 1.7 Ma (MSWD = 0.3), and the Th/U is between 0.01 and 0.07.

4.2. 40Ar/39Ar Dating Results

Electron probe microanalysis of the mica quartz schist samples revealed the following results (Supplementary Table S3): The SiO2 content of muscovite ranges from 46.13% to 48.97%. After normalizing to 11 oxygen atoms, the number of silicon atoms per formula unit (p.f.u) in muscovite is distributed between 3.18 and 3.27 pfu, indicating that it is phengite (Si > 3.1 apfu, [33]). We conducted 40Ar/39Ar step-heating age analysis on the phengite in the mica quartz schist (Sample Ar2301), with the relevant experimental data presented in Supplementary Table S4. The results from 11 step-heating 40Ar/39Ar measurements produced a well-defined age spectrum. Ten temperature steps between 770 and 1400 °C formed a plateau, with the width of age plateau exceeding 90% of the entire plateau. The initial argon isotopic ratio (40Ar/36Ar)0 was determined to be 290.5 ± 13.2, which falls within the range of the modern atmospheric argon abundance (40Ar/36Ar)a = 295.5 ± 0.5, indicating that the muscovite in the sample did not capture excess argon during crystallization. The weighted plateau age is calculated as 183.40 ± 1.83 Ma (MSWD = 5.57), corresponding to a high 39Ar release fraction of 88.21%. The normal isochron age is 183.76 ± 1.91 Ma (MSWD = 6.71), which is consistent with the plateau age (Figure 6).

4.3. Geochemical Characteristics

4.3.1. Mica Quartz Schist

The analytical results of the major and trace elements for the mica quartz schist samples are shown in Supplementary Table S5. The loss on ignition (LOI) of the samples ranges from 0.94 to 2.68 wt.%. After removing the loss on ignition, the recalculated major elements are as follows: SiO2 = 66.56–74.23 wt.%, TiO2 = 0.43–0.74 wt.%, Al2O3 = 12.65–16.28 wt.%, Fe2O3 = 0.04–2.67 wt.%, FeO = 3.48–8.55 wt.%, MnO = 0.04–0.44 wt.%, MgO = 0.31–2.83 wt.%, CaO = 0.4–2.09 wt.%, Na2O = 1.86–2.91 wt.%, K2O = 1.96–3.83 wt.%, and P2O5 = 0.08–0.16 wt.%, These values are close to the average composition of North American Shale (NASC) [34], indicating characteristics of sedimentary rocks. The projection points of the samples in the Ni–(Zr/TiO2) diagram (Figure 7a) are all located in the sedimentary rock area, and in the (al+fm)–(c+alk)-Si diagram (Figure 7b), the projections fall within the sandy sedimentary rock area. In the log(SiO2/Al2O3)–log(Na2O/K2O) diagram (Figure 7c), most samples fall in the greywacke region. In the ΣREE–La/Yb diagram (Figure 7d), the samples primarily fall into the sandstone region. Therefore, the protolith of the mica quartz schist is a set of sedimentary rocks composed of sandstone and subarkose.
The total rare-earth element content (ΣREE) of the samples ranges from 113.52 to 221.16 (ppm). The light rare-earth elements (LREEs) are enriched relative to the heavy rare-earth elements (HREEs), with LaN/YbN = 3.19–11.63. In the chondrite-normalized REE distribution pattern (Figure 8a), the profiles are all right-leaning, with the light rare-earth curve being steeper and the heavy rare-earth curve being relatively flat, exhibiting a moderate degree of Eu negative anomaly (δEu = 0.48–0.69). This pattern is consistent with the rare-earth distribution curve of upper crustal rocks, representing a typical rare-earth distribution model for clastic rocks in active continental margin arcs. In the primitive mantle-normalized trace element pattern (Figure 8b), there is a relative enrichment of large-ion lithophile elements (LILEs) such as Rb and K, along with a depletion of high-field-strength elements (HFSEs) such as Nb, Ta, and Ti, which is consistent with the trace element composition patterns of upper crustal rocks.

4.3.2. Amphibolite

The analytical results of the major and trace elements for the amphibolite samples are shown in Supplementary Table S6. The loss on ignition (LOI) of the diorite amphibolite ranges from 0.51 to 2.77 wt.%. After removing the loss on ignition, the recalculated major elements are as follows: SiO2 = 45.03–50.92 wt.%, TiO2 = 1.13–2.40 wt.%, Al2O3 = 12.67–17.63wt.%, TFe2O3 = 12.20–20.77 wt.%, CaO = 8.79–12.35wt.%, and MgO = 4.41–7.70 wt.%, with the Mg# value ranging from 40 to 54. In the (Ca+Mg)–(Al+Fe+Ti) diagram (Figure 9a), the amphibolite samples fall within the basic volcanic rock area. In the Nb/Y–Zr/TiO2 × 10−4 diagram (Figure 9b), the samples are located in the subalkaline basalt/andesite area. In the SiO2–TFe2O3/MgO diagram (Figure 9c), the samples fall within the tholeiitic series. Therefore, the protolith of the amphibolite is subalkaline tholeiitic basalt.
The total rare-earth element content (ΣREE) of the samples ranges from 56.91 to 98.96 (ppm). There is no obvious differentiation between light and heavy rare-earth elements (LaN/YbN = 0.91–3.10). In the chondrite-normalized REE distribution pattern (Figure 10a), the distribution curve is relatively flat and exhibits a weak Eu negative anomaly (δEu = 0.74–0.92). In the primitive mantle-normalized trace element pattern (Figure 10b), there is a relative enrichment of large-ion lithophile elements (LILEs) such as Rb and K, along with a depletion of high-field-strength elements (HFSEs) such as Nb and Ta, and a slight depletion of Ti, resembling the E-MORB curve.

5. Discussion

5.1. Protolith Ages of the Heilongjiang Complex in the Huanan Area

5.1.1. Deposition Time of the Mica Quartz Schist

The minimum detrital zircon age from meta-sedimentary rocks in the Heilongjiang Complex can provide a lower limit for their deposition, while the overlying strata can determine an upper limit. In this study, the minimum detrital zircon age obtained from Sample HN23005 is 237 ± 2 Ma, and Sample HN23017 yields a weighted mean age of 237.8 ± 6.7 Ma, representing the youngest sedimentary age. This establishes the lower limit for the deposition of the mica quartz schist as Late Triassic, consistent with the lower limit age of 240 Ma for the felsic schist in the Yilan and Mudanjiang areas [42]. Regarding the upper limit age for the mica quartz schist, the metamorphic age of Sample HN23017 is 207.9 ± 3.5 Ma. Additionally, the Heilongjiang Complex in the Luobei area is covered by unmetamorphosed Middle Jurassic strata, which constrains the formation age of the Heilongjiang Complex to prior to the Middle Jurassic [43]. Therefore, we conclude that the deposition time of the mica quartz schist is Late Triassic (237–207 Ma).

5.1.2. Protolith Age of the Amphibole

The zircon grains from amphibole (Sample HN23050) indicate a magmatic origin, with a concordant age of 245.5 ± 1.2 Ma, representing the protolith age of the amphibole formed during the Middle Triassic. Similar ages for amphibole have been reported in the Mudanjiang area (248 ± 4 Ma, [16]). In the regional context of the Heilongjiang Complex, the protolith ages of amphibole are primarily concentrated in the Middle to Late Permian. In the Yilan area, the protolith ages of amphibole are recorded as 256 ± 2.1 Ma, 261.3 ± 3.0 Ma, 261.8 ± 3.3 Ma, and 274 ± 2 Ma [17,27,44]. In the Luobei area, the protolith ages are reported as 256 ± 1 Ma, 261 ± 2 Ma, and 267 ± 2 Ma [14,36]. Additionally, amphibole from the Mudanjiang area has protolith ages of 257 ± 4 Ma and 257 ± 5 Ma [45]. This study presents the first report of Middle Triassic (~245 Ma) amphibole of the Heilongjiang Complex in the Huanan area.

5.2. Deposition Provenances of the Mica Quartz Schist

The provenances of the meta-sedimentary rocks in the Heilongjiang Complex provide important information for understanding the history of the amalgamation between the Jiamusi Block and Songliao Block. The U-Pb dating results of 250 detrital zircon grains from the mica quartz schist reveal four age groups: 155–229 Ma, 237–296 Ma, 485–556 Ma, and 585–2238 Ma (Figure 11). The composition of the detrital zircons is closely related to the regional tectonic and magmatic evolution.
The zircon age range of 155–229 Ma primarily consists of discordant and hydrothermal ages, with an age peak of ~210 Ma that is close to the metamorphic age of the mica quartz schist (207.9 ± 3.5 Ma), reflecting the tectonic thermal events during the collision between the Jiamusi Block and Songliao Block.
For the age range of 237–296 Ma, the age peak is ~260 Ma, and the zircons exhibit a magmatic origin. This magmatic event is widely distributed regionally, such as the development of 278–253 Ma granitic rocks on the western edge of the Jiamusi block [2,30,46,47]. Similarly, there is also granitic magmatism at 264–252 Ma along the eastern margin of the Songliao Block [48,49]. These Permian magmatic rocks have similar geochemical characteristics and are formed in an island arc environment related to subduction processes [19].
The zircon age range of 485–556 Ma includes three concordant ages: 527.7 ± 7.5 Ma, 498.4 ± 1.4 Ma, and 491.6 ± 1.4 Ma. The first two ages are magmatic ages, with 491.6 ± 1.4 Ma representing the metamorphic age. The Jiamusi Block developed a large amount of Early Paleozoic magmatism [23,50], with granulite facies metamorphism occurring around 500 Ma, representing a late Pan-African magmatic–metamorphic event [51]. Additionally, Early Paleozoic magmatic activity has been reported along the eastern margin of the Songliao Block (508–424 Ma, [52]), indicating derivation from partial melting of thickened ancient crustal materials that formed during the amalgamation of the northern Songliao Block and the northern Jiamusi Block [53].
Furthermore, the mica quartz schist contains scattered detrital zircons of Proterozoic age (585–2238 Ma). Both the western margin of the Jiamusi Block and the eastern margin of the Songliao Block exhibit Neoproterozoic magmatic activity, with the ages of 930–703 Ma or 950–573 Ma [54,55,56]. Yang et al. reported the presence of Neoproterozoic magmatism in the Jiamusi Block (891–898 Ma and 757–751 Ma) [57], while granites exposed in the Yichun area date to 1821 Ma [58]. Moreover, multiple Proterozoic peak ages have been identified in detrital zircons from the Dongfengshan Group in the eastern Songliao Block [59]. The sporadic distribution of Precambrian ages suggests the potential existence of an ancient crystalline basement within the sedimentary source area.
Previous studies indicate that the Jiamusi Block mainly experienced two periods of granitic magmatism around 530–515 Ma and 270–254 Ma [24,46], which are consistent with the main peak ages found in mica quartz schist. There are also reports of contemporaneous magmatic activity along the eastern margin of the Songliao Block. The Heilongjiang Complex is located between the Jiamusi Block and the Songliao Block, suggesting that the provenances of the detrital zircons are related to the magmatic and metamorphic activities in both blocks.

5.3. Thermal Events of the Heilongjiang Complex

The zircon characteristics of the amphibole (Sample HN23039) indicate that it underwent late-stage metamorphism. Two groups of concordant ages were identified: the first group, with an age of 229.9 ± 1.3 Ma, represents metamorphosed or recrystallized ages from tectonic thermal events. The second group, with an age of 202.2 ± 1.7 Ma, consists of zircon with Th/U between 0.01 and 0.07, all representing metamorphic ages, suggesting that the amphibole experienced two distinct metamorphic events. In this study, detrital zircons from the mica quartz schist yielded discordant ages ranging from 229 to 155 Ma, indicating that tectonic thermal events began as early as ~229 Ma, and there is a metamorphic age of 207.9 ± 3.5 Ma, which is close to the metamorphic age of the amphibole. Regionally, similar metamorphic ages and collision events have been reported. Han noted that the metamorphic age of biotite-bearing gneiss in the Luobei area was 197 ± 2 Ma, constraining the collision time between the Jiamusi Block and Songliao Block to be 210–197 Ma [43]. The Mesozoic collisional granitic magmatic activity in the Lesser Xing’an Range occurred between 216 and 184 Ma [6,60], while collisional volcanic rocks in the Yanji area developed between 217 and 201 Ma [61]. Therefore, the ages of 207 to 202 Ma represent the collision time between the Jiamusi Block and Songliao Block.
The 40Ar/39Ar age of phengite from the mica quartz schist is 183.40 ± 1.83 Ma, which represents the geological significance directly related to its closure temperature. When mineral grains are above the closure temperature, radiogenic isotopes are entirely lost. Conversely, below this temperature, the isotopic system does not experience effective diffusion [62]. Therefore, the 40Ar/39Ar isotopic dating reflects the time elapsed since the mineral fell below the closure temperature of the argon isotopic system. Previous studies have investigated the metamorphic temperature of the Heilongjiang Complex. The metamorphic temperature of schistose blueschists ranges from 350 to 550 °C [63,64], while the temperature for amphibolite facies is reported to be between 400 and 640 °C [16,65]. The metamorphic temperature for mica schists is noted to be 536–598 °C [66] or 510–610 °C [67]. The closure temperature for Ar isotopes in muscovite is approximately 350 ± 50 °C [68], which is lower than the metamorphic temperatures recorded in the Heilongjiang Complex. In addition, the electron probe results showed that the muscovite sample is phengite. Consequently, the 40Ar/39Ar age represents the cooling time after peak metamorphism, specifically the closure of the Mudanjiang Ocean.

5.4. The Evolutionary History of the Mudanjiang Ocean

The term “Mudanjiang Ocean” was first introduced by [24] to represent the ancient ocean that existed between the Jiamusi Block and Songliao Block during the Late Paleozoic to Early Mesozoic. We have not found any petrological records related to the opening of the Mudanjiang Ocean in the Huanan area. The oldest protolith age of blueschists reported in the Yilan area is 288 Ma, with oceanic island properties [16], suggesting that the Mudanjiang Ocean existed in the Early Permian. The Permian amphibolites (274 ± 2 Ma) in the Yilan and Luobei regions exhibit active continental margin properties [5], indicating that subduction has occurred. Both the western edge of the Jiamusi Block and the eastern edge of the Songliao Block developed an N-S trending volcanic arc during the Middle to Late Permian [3,14,30,44,45,46], suggesting that the Mudanjiang Ocean underwent bidirectional subduction during the Middle Permian.
The protolith of the amphibolite in the Huanan area is subalkaline tholeiitic basalt, which is characterized by the depletion of high-field-strength elements (HFSEs) such as Nb, Ta, and Ti, and exhibits E-MORB features. The amphibolite shows arc attributes in tectonic discrimination diagrams. In the TiO2/10–MnO–P2O5 diagram (Figure 12a), the samples fall within the island arc tholeiitic basalt and MORB regions. In the 2×Nb–Zr/4–Y diagram (Figure 12b), the samples are located in the volcanic arc basalt region. In the Hf/3-Th–Nb/16 diagram (Figure 12c), the samples fall into the island arc tholeiitic basalt and calc-alkaline basalt regions. Combining geochemical characteristics suggests that the amphibolite formed in an active continental margin environment. The protolith age of the amphibolite is 245.5 ± 1.2 Ma, indicating that the Mudanjiang Ocean was still in a subduction phase during the Middle Triassic.
The protolith of the mica quartz schist is a set of sedimentary rocks primarily composed of sandstone and subarkose. Appropriate tectonic setting discrimination diagrams for sedimentary rocks were used. In the SiO2–K2O/Na2O diagram (Figure 13a), all samples fall within the active continental margin zone. In the (TFe2O3+MgO)–TiO2 diagram (Figure 13b), most samples are located in the continental margin arc region. In the Th–La diagram and La–Th–Sc diagram (Figure 13c,d), the samples fall into either the continental island arc or active continental margin regions. Therefore, the mica quartz schist formed in an island arc environment within the context of an active continental margin and were deposited in a forearc basin environment [69]. Comparing the Late Paleozoic to Early Mesozoic magmatic rocks at the junction of the Jiamusi Block and Songliao Block (Figure 14), the magmatic activity was relatively weak, between 240 and 220 Ma. The deposition time of the mica quartz schist is 237–207 Ma, suggesting that the subduction of the Mudanjiang Ocean was relatively weak in the Late Triassic, with the deposition of mica quartz schist in the forearc basin.
The closure of the Mudanjiang Ocean is mainly limited by the metamorphic ages of the Heilongjiang Complex. Previous studies on 40Ar/39Ar geochronology of phengite in blueschist and meta-sedimentary rocks, as well as SIMS U-Pb ages of pyrite in amphibolite, suggest that the peak metamorphic time of the Heilongjiang complex is the Early–Middle Jurassic (190–145 Ma, [6,7,15,16,17]). In the Huanan area, we have discovered a large number of ductile shear zones and thrust structures in the Heilongjiang complex, which may have occurred during the collision process. The 40Ar/39Ar age of phengite in the Huanan area is 183.40 ± 1.83 Ma, representing the closure of the Mudanjiang Ocean. In the Luobei area, the Heilongjiang Complex is found to be unconformably covered by unmetamorphosed Middle Jurassic strata [43]. Therefore, the closure of the Mudanjiang Ocean occurred during the Early to Middle Jurassic.
In summary, this study reconstructs the evolutionary history of the Mudanjiang Ocean between the Jiamusi Block and Songliao Block (Figure 15): (1) During the Early Permian (>288 Ma), the Mudanjiang Ocean had already been opened, characterized by the development of oceanic island basalt. (2) Between the Middle Permian and Middle Triassic (274–245 Ma), bidirectional subduction occurred, with arc magmatism developing along the western edge of the Jiamusi Block and the eastern edge of the Songliao Block. (3) In the Late Triassic (237–207 Ma), the subduction of Mudanjiang Ocean was relatively weak, with the deposition of mica quartz schist in the forearc basin. (4) By the Early to Middle Jurassic (190–145 Ma), the Mudanjiang Ocean closed due to continental collision, leading to the final positioning of the Heilongjiang Complex.

6. Conclusions

(1)
The LA-ICP-MS U-Pb dating results of six samples from the Heilongjiang Complex in the Huanan area show that the deposition time of the mica quartz schist is Late Triassic (237–207 Ma), with provenances related to magmatic and metamorphic activities at the junction of the Jiamusi Block and Songliao Block, while the protolith age of the amphibolite is Middle Triassic (245.5 ± 1.2 Ma).
(2)
40Ar/39Ar isotopic dating yielded a plateau age of 183.40 ± 1.83 Ma for phengite in the mica quartz schist, with the metamorphic ages obtained from zircon U-Pb dating. We identify three significant metamorphic events in the Heilongjiang Complex: (1) ~229 Ma, marking the earliest tectonic thermal disturbance in the complex; (2) 207–202 Ma, corresponding to the metamorphic event related to the collision between the Jiamusi Block and Songliao Block; and (3) ~183 Ma, indicating the closure of the Mudanjiang Ocean.
(3)
The tectonic evolution history of the Mudanjiang Ocean is reconstructed: During the Early Permian, the Mudanjiang Ocean had already opened. Between the Middle Permian and Middle Triassic, bidirectional subduction occurred. In the Late Triassic, the Mudanjiang Ocean entered a subduction dormancy period. By the Early to Middle Jurassic, the Mudanjiang Ocean closed due to continental collision, leading to the final positioning of the Heilongjiang Complex.

Supplementary Materials

The following supporting information can be downloaded at: https://www.mdpi.com/article/10.3390/min15050517/s1, Table S1. Sample information of the Heilongjiang Complex in the Huanan area. Table S2. Zircon LA-ICP-MS U-Pb dating results of samples from the Heilongjiang complex in the Huanan area. Table S3. Electron microprobe analysis results of muscovite in mica quartz schist in the Huanan area (wb/%). Table S4. 40Ar/39Ar dating results for muscovite from mica quartz schist in the Huanan area. Table S5. Major (wt.%) and trace (×10−6) elements data of the mica quartz schist samples. Table S6. Major (wt.%) and trace (×10−6) elements data of the amphibole samples.

Author Contributions

J.X.: Methodology, Formal Analysis, Writing—Original Draft, and Writing—Review and Editing; P.H. (Corresponding Author): Supervision, Conceptualization, and Writing—Review and Editing; W.W.: Conceptualization; H.G.: Data Curation; X.Z.: Investigation. All authors have read and agreed to the published version of the manuscript.

Funding

This research was supported by China Geological Survey Project (NO. DD202501026, NO. DD20230250), the funding project of Northeast Geological S&T Innovation Center of China Geological Survey (NO. QCJJ2023-23), the National Science Foundation of China (Grant No. 42072268), Chinese Academy of Geological Sciences (Grant No. JKYZD202305), and Institute of Geology, Chinese Academy of Geological Sciences (Grant No. J2323).

Data Availability Statement

The authors confirm that the data generated or analyzed during this study are provided in full within the published article.

Acknowledgments

We are grateful to Wei Zhao and Chao Li from Harbin Center for Integrated Natural Resources Survey for their assistance in sample collection. We appreciate the excellent suggestions and comments from the editor and other anonymous reviewers.

Conflicts of Interest

The authors declare no conflicts of interest.

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Figure 1. Tectonic map showing the main subdivisions of central and eastern Asia and location of the study area (Modified after [8,9]).
Figure 1. Tectonic map showing the main subdivisions of central and eastern Asia and location of the study area (Modified after [8,9]).
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Figure 2. (a) Geological sketch map of the Jiamusi Block and adjacent areas in NE China (modified after [1,7,11]). (b) Detailed geological map of the Huanan area showing sample locations.
Figure 2. (a) Geological sketch map of the Jiamusi Block and adjacent areas in NE China (modified after [1,7,11]). (b) Detailed geological map of the Huanan area showing sample locations.
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Figure 3. Field photographs and photomicrographs of the Heilongjiang Complex in Huanan. (a) Field photograph of mica quartz schist, with location of samples HN23005 and Ar2301. (b) Field photograph of amphibolite, with location of sample HN23050. (c): Interlayering of marble and amphibolite. (d) Interlayering of marble and actinolite–chlorite schist. (e) Metasilicalites appear as lenses. (f) Field photograph of serpentinite. (g) Photomicrographs of mica quartz schist sample (HN23005). (h) Photomicrographs of amphibolite sample (HN23050). Abbreviations: Qz = quartz, Ms = muscovite, Bt = biotite, Ab = albite, Grt = garnet, Hbl = hornblende, Pl = plagioclase.
Figure 3. Field photographs and photomicrographs of the Heilongjiang Complex in Huanan. (a) Field photograph of mica quartz schist, with location of samples HN23005 and Ar2301. (b) Field photograph of amphibolite, with location of sample HN23050. (c): Interlayering of marble and amphibolite. (d) Interlayering of marble and actinolite–chlorite schist. (e) Metasilicalites appear as lenses. (f) Field photograph of serpentinite. (g) Photomicrographs of mica quartz schist sample (HN23005). (h) Photomicrographs of amphibolite sample (HN23050). Abbreviations: Qz = quartz, Ms = muscovite, Bt = biotite, Ab = albite, Grt = garnet, Hbl = hornblende, Pl = plagioclase.
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Figure 4. Representative CL images and zircon U-Pb ages of mica quartz schist from (a) Sample HN23005, (b) Sample HN23012, (c) Sample HN23017, and (d) Sample HN23035.
Figure 4. Representative CL images and zircon U-Pb ages of mica quartz schist from (a) Sample HN23005, (b) Sample HN23012, (c) Sample HN23017, and (d) Sample HN23035.
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Figure 5. Representative CL images and U-Pb concordia diagram of amphibole from (a) Sample HN23050 and (b) Sample HN23039.
Figure 5. Representative CL images and U-Pb concordia diagram of amphibole from (a) Sample HN23050 and (b) Sample HN23039.
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Figure 6. 40Ar/39Ar age spectrum (a) and normal isochron age diagram (b) of phengite from the mica quartz schist.
Figure 6. 40Ar/39Ar age spectrum (a) and normal isochron age diagram (b) of phengite from the mica quartz schist.
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Figure 7. The protolith restoration discrimination diagrams of the mica quartz schist. (a): the Ni–(Zr/TiO2) diagram (after [35]), (b): the (al+fm)–(c+alk)-Si diagram (after [36]), (c): the log(SiO2/Al2O3) −log(Na2O/K2O) diagram (after [37]), and (d): the ΣREE–La/Yb diagram (after [34]).
Figure 7. The protolith restoration discrimination diagrams of the mica quartz schist. (a): the Ni–(Zr/TiO2) diagram (after [35]), (b): the (al+fm)–(c+alk)-Si diagram (after [36]), (c): the log(SiO2/Al2O3) −log(Na2O/K2O) diagram (after [37]), and (d): the ΣREE–La/Yb diagram (after [34]).
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Figure 8. Chondrite-normalized REE distribution pattern (a) and primitive mantle-normalized trace element pattern (b) of the mica quartz schist. Chondrite and primitive mantle values are from [38].
Figure 8. Chondrite-normalized REE distribution pattern (a) and primitive mantle-normalized trace element pattern (b) of the mica quartz schist. Chondrite and primitive mantle values are from [38].
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Figure 9. Geochemical classification of the amphibolite. (a): the (Ca+Mg)–(Al+Fe+Ti) diagram (after [39]), (b): the Nb/Y–Zr/TiO2 × 10−4 diagram (after [40]), and (c): the SiO2–TFe2O3/MgO diagram (after [41]).
Figure 9. Geochemical classification of the amphibolite. (a): the (Ca+Mg)–(Al+Fe+Ti) diagram (after [39]), (b): the Nb/Y–Zr/TiO2 × 10−4 diagram (after [40]), and (c): the SiO2–TFe2O3/MgO diagram (after [41]).
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Figure 10. Chondrite-normalized REE distribution pattern (a) and primitive mantle-normalized trace element pattern (b) of the amphibolite. Chondrite and primitive mantle values are from [38].
Figure 10. Chondrite-normalized REE distribution pattern (a) and primitive mantle-normalized trace element pattern (b) of the amphibolite. Chondrite and primitive mantle values are from [38].
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Figure 11. Relative probability plot of detrital zircons from the mica quartz schist in the Heilongjiang complex.
Figure 11. Relative probability plot of detrital zircons from the mica quartz schist in the Heilongjiang complex.
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Figure 12. The tectonic setting discrimination diagrams of the amphibolite. (a): the TiO2/10–MnO–P2O5 diagram, OIT = oceanic island basalt, MORB = mid-ocean ridge basalt, IAT = island arc tholeiites, CAB = calc-alkaline basalt, OIA = oceanic island alkaline. (b): the 2×Nb–Zr/4–Y diagram, A1 + A2 = Intraplate alkaline basalt, A2 + C = intraplate rift basalt, B = E-type mid-ocean ridge basalt, D = normal mid-ocean ridge basalt, C + D = volcanic arc basalt. (c): the Hf/3–Th–Nb/16 diagram, IAT = island arc tholeiites, CAB = calc-alkaline basalt, N-MORB = normal mid-ocean ridge basalt, E-MORB = enrichment mid-ocean ridge basalt, WPAB = within-plate alkaline basalt, WPT = within-plate transitional.
Figure 12. The tectonic setting discrimination diagrams of the amphibolite. (a): the TiO2/10–MnO–P2O5 diagram, OIT = oceanic island basalt, MORB = mid-ocean ridge basalt, IAT = island arc tholeiites, CAB = calc-alkaline basalt, OIA = oceanic island alkaline. (b): the 2×Nb–Zr/4–Y diagram, A1 + A2 = Intraplate alkaline basalt, A2 + C = intraplate rift basalt, B = E-type mid-ocean ridge basalt, D = normal mid-ocean ridge basalt, C + D = volcanic arc basalt. (c): the Hf/3–Th–Nb/16 diagram, IAT = island arc tholeiites, CAB = calc-alkaline basalt, N-MORB = normal mid-ocean ridge basalt, E-MORB = enrichment mid-ocean ridge basalt, WPAB = within-plate alkaline basalt, WPT = within-plate transitional.
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Figure 13. The tectonic setting discrimination diagrams of the mica quartz schist. (a): the SiO2–K2O/Na2O diagram, (b): the (TFe2O3+MgO)–TiO2 diagram, (c): the Th–La diagram, and (d): the La–Th–Sc diagram.
Figure 13. The tectonic setting discrimination diagrams of the mica quartz schist. (a): the SiO2–K2O/Na2O diagram, (b): the (TFe2O3+MgO)–TiO2 diagram, (c): the Th–La diagram, and (d): the La–Th–Sc diagram.
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Figure 14. Age spectrum of Late Paleozoic–Early Mesozoic magmatic rocks at the junction of the Jiamusi Block and Songliao Block (modified after [61]). X axis—magmatic rock age (Ma); Y axis—number of reported magmatic rocks.
Figure 14. Age spectrum of Late Paleozoic–Early Mesozoic magmatic rocks at the junction of the Jiamusi Block and Songliao Block (modified after [61]). X axis—magmatic rock age (Ma); Y axis—number of reported magmatic rocks.
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Figure 15. Schematic diagrams showing the tectonic evolution of the Mudanjiang Ocean during the Late Paleozoic–Mesozoic.
Figure 15. Schematic diagrams showing the tectonic evolution of the Mudanjiang Ocean during the Late Paleozoic–Mesozoic.
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Xu, J.; Hu, P.; Wang, W.; Guo, H.; Zhang, X. Late Paleozoic–Mesozoic Tectonic Evolution of the Mudanjiang Ocean: Constraints from the Zircon U-Pb and Ar-Ar Chronology of the Heilongjiang Complex, NE China. Minerals 2025, 15, 517. https://doi.org/10.3390/min15050517

AMA Style

Xu J, Hu P, Wang W, Guo H, Zhang X. Late Paleozoic–Mesozoic Tectonic Evolution of the Mudanjiang Ocean: Constraints from the Zircon U-Pb and Ar-Ar Chronology of the Heilongjiang Complex, NE China. Minerals. 2025; 15(5):517. https://doi.org/10.3390/min15050517

Chicago/Turabian Style

Xu, Jianxin, Peiyuan Hu, Wendong Wang, Hongyu Guo, and Xin Zhang. 2025. "Late Paleozoic–Mesozoic Tectonic Evolution of the Mudanjiang Ocean: Constraints from the Zircon U-Pb and Ar-Ar Chronology of the Heilongjiang Complex, NE China" Minerals 15, no. 5: 517. https://doi.org/10.3390/min15050517

APA Style

Xu, J., Hu, P., Wang, W., Guo, H., & Zhang, X. (2025). Late Paleozoic–Mesozoic Tectonic Evolution of the Mudanjiang Ocean: Constraints from the Zircon U-Pb and Ar-Ar Chronology of the Heilongjiang Complex, NE China. Minerals, 15(5), 517. https://doi.org/10.3390/min15050517

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