Statherian (ca. 1714–1680 Ma) Extension-Related Magmatism and Deformation in the Southwestern Korean Peninsula and Its Geological Significance: Constraints from the Petrological, Structural, Geochemical and Geochronological Studies of Newly Identified Granitoids

Abstract

In this study, petrological, structural, geochemical, and geochronological analyses of the Statherian alkali feldspar granite and porphyritic alkali feldspar granite in the southwestern part of the Korean Peninsula were conducted to examine petrogenesis of the granitoids and their tectonic setting. Zircon U-Pb dating revealed that the two granites formed around 1.71 Ga and 1.70–1.68 Ga, respectively. The results of the geochemical analyses showed that both of the granites have a high content of K₂O, Nb, Ta, and Y, as well as high FeO^t/MgO and Ga/Al ratios. Both granites have alkali-calcic characteristics with a ferroan composition, indicating an A-type affinity. Zircon Lu-Hf isotopic compositions yielded negative ε_Hf^(t) values (−3.5 to −10.6), indicating a derivation from ancient crustal materials. Both granite types underwent ductile deformation and exhibited a dextral sense of shear with a minor extension component. Based on field relationships and zircon U-Pb dating, it was considered that the deformation event postdated the emplacement of the alkali feldspar granite and terminated soon after the emplacement of the porphyritic alkali feldspar granite in an extensional setting. These data indicated that there were extension-related magmatic activities accompanying ductile deformation in the southwestern part of the Korean Peninsula during 1.71–1.68 Ga. The Statherian extension-related events are well correlated with those in the midwestern part of the Korean and eastern parts of the North China Craton.

1. Introduction

The Wilson cycle [1] is closely associated with the formation and destruction of orogenic belts and related cratonic blocks. The North China Craton (NCC), one of the largest cratonic blocks in northeast Asia, is divided into eastern and western blocks, and it is generally accepted that the eastern block has retained the changes that occurred during the Wilson cycle-like evolution during the Paleoproterozoic (2.12–1.67 Ga) [2,3,4,5]. Although there is still a debate on the tectonic setting for the initial stage of the Wilson cycle-like evolution [3], it could be marked by the opening of the ocean together with intraplate magmatism between the Longgang Block in the eastern part of the NCC and the Nangnim Massif in the Korean Peninsula at ca. 2.12 Ga [6]. These events were followed by the subduction, continental collision, as well as post-collisional magmatic, sedimentary, metamorphic, and deformation events relating to the formation and destruction of the Jiao-Ji mobile belt during 1.95–1.67 Ga [3,4,5,7].

The last stage of the Wilson cycle-like evolution in the eastern part of the NCC, including the Korean Peninsula, is characterized by the occurrence of extension-related magmatism, sedimentation, and regional anatexis [4,8,9]. The extension-related magmatism has produced igneous rocks that have mafic to felsic bimodal compositions in the northwestern area of the eastern part of the NCC [10,11,12,13,14], the southern part of the NCC [8,15], and the western part of the Nangnim and Gyeonggi massifs in the Korean Peninsula [9,16] during 1.80–1.60 Ga. Integrated geochemical studies suggest that igneous rocks were formed in post-orogenic and/or anorogenic settings after the continental collision [8,14]. It was recently identified that the southwestern part of the Korean Peninsula also underwent the late Paleoproterozoic (1.71–1.68 Ga) magmatism and deformation [17]. It is well known that the understanding of the nature of granitoids can provide critical information about the tectonic setting. The late Paleoproterozoic (Statherian) magmatism and deformation in the eastern part of the NCC is one of the key factors in interpreting the tectonic evolution of northeast Asia. Similarly, the late Paleoproterozoic magmatism and deformation in the southwestern part of the Korean Peninsula can also provide the crucial information needed to understand the tectonic evolution of northeast Asia.

In this study, whole-rock geochemical, zircon U-Pb, and Lu-Hf analyses were conducted on the newly identified granitoids from the southwestern region of the Korean Peninsula to decipher their emplacement timing and trace their origin and petrogenesis. The structural analysis of the granitoids was also conducted to shed light on the structural geometry and kinematics of the late Paleoproterozoic. Based on the data obtained from the current and previous studies, the extension-related magmatism and deformation in the western part of the Korean Peninsula were correlated with those in the eastern NCC and the Yangtze Block in the South China Craton, and the geological relationships between them were discussed.

2. General Geology and Petrography

The basement of the Korean Peninsula is divided into four Precambrian tectonic provinces (Kwanmo, Nangnim, Gyeonggi, and Yeongnam massifs) and is mainly composed of Paleoproterozoic (Orosirian) para- and orthogneisses with minor Archean remnants [18,19] (Figure 1a). The early Orosirian paragneisses formed after 2.0 Ga and were intruded by orthogneisses during 2.00–1.80 Ga [20,21,22,23]. The para- and orthogneisses underwent upper amphibolite to granulite facies metamorphism during 1.88–1.86 Ga [24,25,26]. These Paleoproterozoic magmatic and metamorphic events are considered to be closely related to the amalgamation and breakup of the Columbia supercontinent [27]. The Paleoproterozoic rocks formed during the Orosirian Period are covered by Statherian sedimentary rocks (Seosan Group) and then intruded by Statherian granitoids [9,16,28]. Recently, it has been suggested that the Statherian granitoids in the midwestern part of the Korean Peninsula (western part of the Gyeonggi Massif) are A₂-type granites formed in a post-collisional setting [9].

The study area (Sangtaedo-Jungtaedo-Hataedo-Ganseodo), located in the southwestern part of the Korean Peninsula, consists of quartz schist, foliated alkali feldspar granite, foliated porphyritic alkali feldspar granite, conglomerate, and dikes (Figure 1) [17]. Based on field relationships, the quartz schist preserved as xenolith in the foliated alkali feldspar granite is considered to be the oldest geological unit in the study area, although its depositional age is not constrained. The foliated alkali feldspar granite (AFG) is exposed in the regions of Hataedo, Jungtaedo, and the southern part of Sangtaedo and is intruded by the foliated porphyritic alkali feldspar granite (PAFG), which is exposed in the region of Sangtaedo, northwestern part of Jungtaedo, and Ganseodo (Figure 1). The AFG is unconformably overlain by the Cretaceous conglomerate. The Cretaceous conglomerate in the western part of Hataedo is a massive, clast-supported conglomerate. Various types of Cretaceous undeformed dikes (mafic, intermediate, and acidic compositions) have intruded the AFG and PAFG.

3. Analytic Methods

3.1. Zircon U-Pb Analyses

The zircon grains were separated from the AFG and PAFG by standard crushing, water-based panning, magnetic separation, and heavy liquid separation techniques, and the separated zircon grains were mounted together with SL13 (U = 238 ppm) and FC-1 standards (²⁰⁶Pb*/²³⁸U = 0.1859; 1099 Ma) to calibrate the U contents and Th/U ratios. The FC-1 standard zircon yielded a weighted-mean age of 1099 ± 9.5 Ma (MSWD = 1.73, n = 55), which was consistent with the recommended value. The internal texture of zircon was documented by cathodoluminescence (CL) using a JEOL JSM-6610LV scanning electron microscope at the Korea Basic Science Institute (KBSI) Ochang, Korea. The U-Th-Pb isotopes in zircon grains were measured using a sensitive high-resolution ion microprobe (SHRIMP IIe/MC instrument) at KBSI. The primary oxygen beam was accelerated at 10 kV and focused to a spot diameter of approximately 25 μm. Each U-Pb analysis involved five scans in the mass range of 196–254 AMU. The U and Th concentrations were determined relative to those of the SL13 standard zircon. The measured ²⁰⁶Pb/²³⁸U ratios were calibrated using an FC-1 standard zircon. A common Pb correction was conducted using the ²⁰⁴Pb correction method [30]. The detailed procedure and review of U-Th-Pb dating of zircon using SHRIMP are given by [31]. The obtained data were processed using SQUID 2.50 and Isoplot 3.75 [32]. The uncertainties for ages and ratios are given at the 1σ level, whereas uncertainties for weighted-mean ages are given at the 2σ level.

3.2. Zircon Lu-Hf Analyses

The zircon Lu-Hf isotope analyses were conducted using laser ablation-multicollector-inductively coupled plasma-mass spectrometry (LA-MC-ICP-MS) employing an ESI NWR193UC LA system attached to a Nu Plasma II MC-ICP-MS instrument at the KBSI, Ochang, Korea. Laser energy of approximately 5 J/cm², a laser spot size of 45 μm, and a repetition rate of 20 Hz were used during the analysis. The interference of ¹⁷⁶Yb and ¹⁷⁶Lu on ¹⁷⁶Hf was corrected by measuring the intensity of the interference-free ¹⁷³Yb and ¹⁷⁵Lu isotopes. The 91,500 and FC-1 standard zircons were analyzed to monitor the accuracy of the ¹⁷⁶Hf/¹⁷⁷Hf ratios. The 91,500 and FC-1 zircons yielded weighted-mean ¹⁷⁶Hf/¹⁷⁷Hf ratios of 0.282298 ± 0.00001 (N = 61; 2σ) and 0.282177 ± 0.000015 (N = 27; 2σ). The analytical procedure and data acquisition are described in detail in [20]. The ¹⁷⁶Lu decay constant (1.867 × 10⁻¹¹ y⁻¹; [33]), depleted mantle (¹⁷⁶Lu/¹⁷⁷Hf = 0.0384 and ¹⁷⁶Hf/¹⁷⁷Hf = 0.28325; [34]) and chondrite (¹⁷⁶Lu/¹⁷⁷Hf = 0.0332 and ¹⁷⁶Hf/¹⁷⁷Hf = 0.282772; [35]) values were used to calculate the ε_Hf^(t) values and model ages (T_DM1). The average continental crustal composition (¹⁷⁶Lu/¹⁷⁷Hf = 0.015; [36]) was used to calculate the two-stage crustal model ages (T_DM2).

3.3. Whole-Rock Geochemistry

The AFG and PAFG samples were crushed into <0.5 cm fragments in a tungsten carbide mortar and powdered in an agate ball mill. The crushed samples were pulverized to pass through a 200-mesh sieve to ensure homogeneity. The concentrations of major and trace elements were measured by inductively coupled plasma atomic emission spectrometry (ICP-AES; ThermoJarrel-Ash ENVRIO II) and inductively coupled plasma-mass spectrometry (ICP-MS; Perkin Elmer Sciex Elan 9000) at Activation Laboratories, Ancaster, ON, Canada. The major elements were measured with international reference materials, including NIST 694, DNC-1, W-2a, SY-4, and BIR-1, and the detection limits of major elements were 0.01%. The trace elements were measured with international reference materials, including SDC-1, TDB-1, SY-4, and ZW-C, and the detection limits of trace elements were 0.002–0.01ppm. More detailed analytical processes and conditions are provided in http://www.actlabs.com/ (accessed on 23 May 2021).

4. Results

4.1. Petrography and Structural Analysis

The AFG is generally medium- to coarse-grained and is characterized by augen-shaped alkali feldspar megacrysts 3–5 cm in size (7 cm maximum) aligned parallel to the regional mylonitic foliation (Figure 2). The AFG consists of alkali feldspar phenocrysts together with alkali feldspar, biotite, quartz, and plagioclase (Figure 3a,b). The PAFG is medium- to coarse-grained and is characterized by pale, reddish-colored alkali feldspar phenocrysts ranging in size from 1 to 3 cm (Figure 4). The PAFG consists of alkali feldspar phenocrysts embedded in a fine-grained matrix composed of alkali feldspar, quartz, biotite, and plagioclase (Figure 3c,d).

The Paleoproterozoic AFG and PAFG were mostly affected by ductile shearing parallel to the regional shear zones. The regional extension of the shear zone was unclear because of its occurrence in isolated island areas. The deformation degree of the AFG was much stronger than that of the PAFG, and abrupt transitions from protomylonite to ultramylonite were frequently observed. The highly strained zones in the AFG occurred as discrete shear zones, which were mainly composed of ultramylonite. The discrete shear zones had various widths ranging from a few centimeters to several meters and locally showing patterns of anastomosing shear zones surrounding lenses of weakly deformed granite (Figure 2a–c). The discrete shear zones showed a low to subvertical dip angle. The mylonitic foliation stroke NE-ENE and dipped to the NW (Figure 5). The stretching lineation mainly plunged gently to the NE (Figure 2d). Kinematic indicators, including S-C fabrics, shear bands, and asymmetric porphyroclast systems of rounded alkali feldspar, consistently showed a dextral sense of shear (Figure 2e,f). These structural features indicate that dextral strike-slip movement with a minor extensional component (southeast side up) was dominant in the shear zone. The PAFG, which intrudes into the AFG, was also pervasively foliated but was less deformed compared to the AFG (Figure 4c,d). The highly strained zone in the PAFG was less frequent and was characterized by a very thin ultramylonite zone, several millimeters wide. The overall attitude of mylonitic foliation in the PAFG was parallel to that in the AFG, and the sense of shear was also dextral, as indicated by the geometry of the minor continuous shear zones (Figure 4d).

4.2. Zircon U-Pb and Lu-Hf Analyses

Zircon grains from the TD12 sample (AFG) were euhedral to subhedral and coarse-grained (>200 μm). In the cathodoluminescence (CL) image, most of the zircon grains showed concentric- or faint-zoned cores partly rimmed by dark unzoned domains (Figure 6a). The zircon cores had low U (19‒95 ppm) and Th (15‒113 ppm) contents with high Th/U ratios, ranging from 0.82 to 1.46 (Table S1). Eleven U-Th-Pb analyses yielded ²⁰⁷Pb/²⁰⁶Pb ages ranging from 1639 to 1742 Ma and are concordant at 1714 ± 12 Ma (MSWD = 1.3; Figure 7a). Eleven analyses of zircon cores gave ε_Hf^(t) values ranging from –3.7 to ‒7.7 with the Neoarchean T_DM2 model ages ranging from 2623 to 2874 Ma (Figure 8a,b; Table S2).

Zircon grains from the TD14 sample (AFG) were euhedral to subhedral and medium- to coarse-grained (100‒200 μm). In the CL image, most of the zircon grains showed concentric, patchy, or banded-zoned cores partly rimmed by dark unzoned domains (Figure 6b). The zircon cores had low U (14–125 ppm) and Th (12–180 ppm) contents with high Th/U ratios, ranging from 0.85 to 1.21 (Table S1). Twenty U-Th-Pb analyses yielded ²⁰⁷Pb/²⁰⁶Pb ages ranging from 1226 to 1682 Ma and a concordance age of 1707 ± 6.1 Ma (MSWD = 1.2; Figure 7b). Seventeen zircon core analyses yielded ε_Hf^(t) values ranging from ‒3.5 to ‒8.1 with the Neoarchean T_DM2 model ages ranging from 2609 to 2894 Ma (Figure 8a,b; Table S2).

Zircon grains from the TD13 sample (PAFG) were euhedral to subhedral and fine- to medium-grained (70‒120 μm). In the CL image, most of the zircon grains showed concentric or patchy-zoned cores (Figure 6c). The zircon cores had low to medium U (41‒702 ppm) and Th (42‒1205 ppm) contents with high Th/U ratios, ranging from 0.65 to 1.77 (Table S1). Thirteen U-Th-Pb analyses yielded ²⁰⁷Pb/²⁰⁶Pb ages ranging from 1534 to 1689 Ma and yielded a concordance age of 1680 ± 4.0 Ma (MSWD = 0.26; Figure 7c). Nine analyses of zircon cores gave ε_Hf^(t) values ranging from −3.6 to −7.9, with the Neoarchean T_DM2 model ages ranging from 2596 to 2861 Ma (Figure 8a,b; Table S2).

Zircon grains from GS1 (PAFG) were euhedral to subhedral and fine- to coarse-grained (70–250 μm). In the CL image, most of the zircon grains showed concentric, patchy, or banded-zoned cores partly rimmed by dark unzoned domains (Figure 6d). The zircon cores had low U (26–254 ppm) and Th (24–251 ppm) contents with high Th/U ratios, ranging from 0.56 to 1.30 (Table S1). The dark unzoned rim had low U (163 ppm) and Th (1 ppm) contents with low Th/U ratios (0.01). Seventeen U-Th-Pb analyses on zircon cores and one U-Th-Pb analysis on zircon rim yielded ²⁰⁷Pb/²⁰⁶Pb ages of 1635 to 1720 Ma and 145 Ma, respectively. The discordia line from zircon core and rim constrained upper and lower intercept ages at 1689.8 ± 9.4 Ma and 150 ± 26 Ma, respectively (MSWD = 1.06), and 16 zircon cores yielded concordance age of 1696 ± 8.1 Ma (MSWD = 1.8; Figure 7d). Analyses of the 16 zircon cores yielded ε_Hf^(t) values ranging from −3.6 to −10.6, with the Neoarchean T_DM2 model ages ranging from 2602 to 3039 Ma (Figure 8a,b; Table S2).

4.3. Whole-Rock Geochemical Analyses

The AFG samples had 67.30–72.33 wt.% of SiO₂, 3.08–7.16 wt.% of Fe₂O₃^(t), 0.32–1.93 wt.% of MgO, 11.96–13.24 wt.% of Al₂O₃, 0.59–1.88 wt.% of CaO, 0.82–2.70 wt.% of Na₂O, 4.92–7.21 wt.% of K₂O, 0.22–0.82 wt.% of TiO₂, and 0.04–0.08 wt.% of MnO (Table S3). In the total alkali (Na₂O + K₂O) vs. SiO₂ diagram (TAS diagram), the AFG was plotted in the granodiorite to granite fields (Figure 9a). The AFG samples were plotted on the high-K calc-alkaline series field, except for one sample (plotted in shoshonitic series) in the K₂O vs. SiO₂ diagram (Figure 9b), and had a metaluminous-to-peraluminous character (Figure 9c) with ferroan-to-magnesian compositions (Figure 9d).

The PAFG samples had 70.58–76.40 wt.% of SiO₂, 1.89–3.16 wt.% of Fe₂O₃^(t), 0.07–0.85 wt.% of MgO, 11.43–12.83 wt.% of Al₂O₃, 0.08–1.49 wt.% of CaO, 1.99–4.04 wt.% of Na₂O, 3.58–6.25 wt.% of K₂O, 0.15–0.50 wt.% of TiO₂, and 0.01–0.05 wt.% of MnO (Table S3). The PAFG plotted in the granite field in the TAS diagram is shown in Figure 9a. All the PAFG samples were plotted on the high-K calc-alkaline series field in the K₂O vs. SiO₂ diagram (Figure 9b) and had a metaluminous-to-peraluminous character (Figure 9c) with ferroan-to-magnesian compositions (Figure 9d).

In the chondrite-normalized rare earth element (REE) diagram, the AFG samples showed enrichment in light REE’s ((La/Yb)_N = 7.8–22.6; Figure 10a). These samples had negative Eu anomalies (Eu/Eu* = Eu_N/$\sqrt{{\mathrm{Sm}}_{\mathrm{N}}{\ast \mathrm{Gd}}_{\mathrm{N}}}$) ranging from 0.2 to 0.7 and also had relatively high concentrations of Rb (100–293 ppm), Ba (591–1874 ppm), and Pb (15–217 ppm; Table S3). In the primitive mantle-normalized spider diagram, the AFG samples showed enrichment in large ion-lithophile elements (e.g., Rb, Ba, and K), Th, U, Pb, La, Ce, and Nd, and negative Nb, Ta, P, and Ti anomalies (Figure 10b) (Table S3).

In the chondrite-normalized REE diagram, the PAFG samples showed enrichment in light REE’s ((La/Yb)_N = 4.9–12.2; Figure 10c) with negative Eu anomalies ranging from 0.2 to 0.8, and relatively high concentrations of Rb (89–282 ppm), Ba (521–1106 ppm), and Pb (28–449 ppm; Table S3). In the primitive mantle-normalized spider diagram, the foliated PAFG samples had high contents of large ion lithophile elements (e.g., Rb, Ba, and K), Th, U, Pb, La, Ce, and Nd, and negative Nb, Ta, P, and Ti anomalies (Figure 10d; Table S3).

5. Discussion

5.1. Timing of Pluton Emplacement and Deformation

Based on zircon U-Pb dating and field relationships, an attempt was made to constrain the timing of magmatism and deformation in the study area. The zircon grains separated from the AFG showed oscillatory or banded zoning with high Th/U ratios (0.8–1.5), which was consistent with the characteristics of magmatic zircons [46]. These zircon grains yield a concordant age of 1.71 Ga (1714 ± 12 Ma and 1707 ± 6.1 Ma; Figure 7a,b), indicating the AFG emplacement at 1.71 Ga. The zircon grains separated from the PAFG had typomorphic and compositional characteristics similar to those of the zircon grains from the AFG (Figure 6 and Table S1). These zircon grains yield a concordant age of 1.70–1.68 Ga (1696 ± 8.1 Ma and 1680 ± 4.0 Ma; Figure 7c,d) that was interpreted as the emplacement age. Although the youngest and oldest emplacement ages of the AFG and PAFG overlapped within the error range, their field relationships, wherein the PAFG intruded the AFG, indicated that the AFG formed before PAFG [17].

The AFG and PAFG underwent regional ductile shearing, which was recorded by the development of the regional mylonitic fabric. The onset of ductile shearing can easily be constrained by the crosscutting relationship between AFG and PAFG. The weakly foliated PAFG crosscut the strong mylonitic foliation of the AFG, indicating that the AFG was strongly deformed before the emplacement of the PAFG. The results of zircon U-Pb dating showed that the main ductile shearing in the AFG could have occurred between 1707 ± 6.1 Ma and 1696 ± 8.1 Ma. Although the timing of the deformation of the PAFG was not constrained, it was assumed that it might have occurred soon after its emplacement. However, further studies are needed to verify the timing of deformation of the PAFG.

5.2. Genetic Type and Source Material of the AFG and PAFG

As mentioned earlier, AFG and PAFG underwent ductile deformation. In addition, zircons in the AFG and PAFG have recrystallized rims that show dim and unzoned textures (Figure 6). Thus, the element mobility of the AFG and PAFG needs to be examined before discussing petrogenesis using whole-rock geochemical compositions. The silicic or carbonatic alteration was not observed in AFG and PAFG. The losses on ignition of the AFG and PAFG were 0.96–1.59 and 0.48–1.82, respectively. The Ce* (Ce* = Ce_N/$\sqrt{{\mathrm{La}}_{\mathrm{N}}{\ast \mathrm{Pr}}_{\mathrm{N}}}$) values of the AFG and PAFG were 1.0–1.1 and 0.9–1.0, respectively. This information indicates that the whole-rock compositions could be used to constrain the petrogenesis and source material of the AFG and PAFG. However, the two PAFG samples (TD13 and GS1) had distinct Ce* values (0.5, 1.3), implying that some mobile elements (e.g., Sr) might have been modified during deformation. Thus, the mobile elements in the TD13 and GS1 samples are not considered in the discussion of petrogenesis.

The whole-rock geochemical analyses showed that the AFG had granodioritic to granitic compositions, while PAFG had granitic compositions (Table S3). Both rock types had high contents of K₂O, K₂O + Na₂O, Nb, Ta, Y, Zr, and light REEs with alkali-calcic and ferroan characteristics contrasting with low contents of Al₂O₃, CaO, and Ba. They also had high Nb + Y (>60) content with high FeO^t/MgO and Ga/Al ratios. These parameters indicated A-type rather than I- or S-type affinities [47,48,49]. In addition, both the AFG and PAFG were plotted in the A-type field in the granite classification diagram and had higher zircon saturation temperatures (T_zr °C = 820–932 °C) than the average zircon saturation temperature of A-type granite (Figure 11d) [50]. Based on the ratios of incompatible elements, A-type granite was subdivided into A₁- and A₂-types and these were considered to have formed in an anorogenic and post-collisional tectonic setting, respectively [51]. In the A-type granite subdivision diagram, the AFG and PAFG were plotted in the A₂-type field, indicating that they formed in the post-collision tectonic setting (Figure 11). The subdivision of A₁- and A₂-type granites should only be used for granitoids that were plotted in the A-type granite field suggested in [47] and the within-plate granite field suggested in [52]. This was the case of the AFG and PAFG granites, thus supporting the A₂-type affinity (Figure 12).

The source material and genetic process of A-type granitoids have long been discussed. In case of the A₂-type granitoids, there are three possible source materials as follows: (1) mantle-derived mafic melt, (2) crust-derived melt, and (3) mixing or assimilation between mantle- and crust-derived melts [51,55,56]. The zircon separated from the AFG and PAFG yielded negative ε_Hf^(t) values ranging from −3.5 to −8.1 for the AFG and from ‒3.6 to −10.6 for the PAFG with the T_DM2 model age (2775 Ma on average) much older than the emplacement age (Table S2). This indicates that the source material for the AFG and PAFG was derived from ancient crustal material, excluding the mantle-derived melt. In summary, the geochemical analysis shows that the granitoids originated from the reworked ancient crustal material in an extension-related, post-collisional setting.

5.3. Implication of the Statherian Events in the Korean Peninsula

Based on the geochemical and geochronological analyses, it was revealed that the granitoids in the southwestern region of the Korean Peninsula formed in an extension-related setting during the Statherian (1.71–1.68 Ga). The extension-related setting was also confirmed by the development of the dextral strike-slip with a minor extensional component (a southeast side up) on the foliated AFG and the emplacement of the foliated PAFG in a syntectonic setting. In terms of geochemical composition, these Statherian granitoids could be well correlated with the granitic gneiss and anatectic granite of the midwestern part of the Korean Peninsula (the western Gyeonggi Massif or the Hongseong-Imjingang Belt) [9]. The rocks in both areas were classified as A-type granitoids based on the high contents of alkalis (K₂O and Na₂O), light REEs, Nb + Y, and high FeO^t/MgO and Ga/Al ratios. Both rock types also had similar zircon Lu-Hf isotopic compositions, with ε_Hf^(t) values ranging from −3.6 to −17.8 (Figure 8a). In addition, the biotite granite in the northwestern part of the Korean Peninsula (Uiju area in the northwestern part of the Nangnim Massif) also had an emplacement age of 1654 ± 79 Ma, similar to granitoids and granitic gneiss in the midwestern to the southwestern part of the Korean Peninsula [16]. Although there were no geochemical data, it was assumed that this biotite granite also formed in an extensional setting because of the similarity in emplacement age and the Orosirian tectonothermal events in the Nangnim and Gyeonggi massifs. The data indicate that there were regional extension-related magmatic events accompanying the ductile deformation along the western part of the Korean Peninsula during 1.71–1.68 Ga. The Statherian granitoids of the western part of the Korean Peninsula had geochemical compositions that were similar to the granite formed in a post-collisional setting (Figure 11 and Figure 12) [9]. Thus, the Statherian extension occurred in a post-collisional setting. Considering that the basement of the Korean Peninsula underwent orogenic magmatism, metamorphism, and deformation during 1.93–1.78 Ga [20,21,24,57,58,59], the Statherian post-collisional magmatism in the western part of the Korean Peninsula might have followed the Orosirian orogenic events.

As mentioned earlier, the Statherian extension occurred in the eastern part of the NCC and the Yangtze Block in the South China Craton during 1.74–1.63 Ga, but their tectonic setting was different. In general, it is considered that the Statherian events in the eastern part of the NCC occurred in a post-collisional setting that followed the collision of the eastern and western blocks of the NCC [8 and references therein]. On the other hand, the extension in the southwestern part of the Yangtze Block occurred in the continental rifting regime [40,60], although a subduction setting has also been suggested [61]. Recently, [62] suggested that continental rifting occurred in the northern margin of the Yangtze Block (in the region of the Tongbai orogeny) at ca. 1.63 Ga, and these events could be correlated well with the continental rifting in the southwestern part of the Yangtze Block, indicating continental rifting as the dominant setting of the Yangtze Block during ca. 1.74–1.63 Ga. The petrogenesis of the Statherian granitoids in the eastern part of the NCC was also different from that of the Statherian granitoids of the Yangtze Block. In general, most of the Statherian granitoids in the eastern part of the NCC are formed by partial melting of the ancient crust [8], but the Statherian granitoids in the Yangtze Block are formed by fractional crystallization of the juvenile mafic magma [40].

As previously mentioned, the Statherian granitoids in the southwestern part of the Korean Peninsula had geochemical compositions that were similar to those of post-collisional granites. The zircon Lu-Hf isotopic compositions showed that the Statherian granitoids originated from ancient crustal material that might have formed during the Neoarchean (Figure 8). These geochemical and isotopic characteristics correlated well with the Statherian granitoids in the eastern part of the NCC. Recently, a comparison of the geochemical compositions of the Statherian granitoids in the midwestern part of the Korean Peninsula, the eastern part of the NCC, and southwestern part of the Yangtze Block was made [9]. It was also concluded that the Statherian granitoids on the Korean Peninsula are better correlated with those of the eastern part of the NCC than with those of the Yangtze Block. For example, the Statherian granitoids in the midwestern part of the Korean Peninsula and eastern NCC have distinctly lower (Nb/La)_N, (Th/Nb)_N, and (Ta/La)_N ratios than the Statherian granitoids of the Yangtze Block. Thus, we propose that the western part of the Korean Peninsula (in present coordinates) might have undergone regional, extension-related magmatism during the Statherian (1.71–1.68 Ga), which is similar to that in the eastern part of the NCC.

6. Conclusions

(1)

The SHRIMP zircon U-Pb dating revealed that the foliated AFG and PAFG were emplaced in the southwestern extreme of the Korean Peninsula at 1.71 Ga and 1.70–1.68 Ga, respectively.

(2)

The zircon Lu-Hf isotope and the whole-rock geochemical analyses suggested that the foliated AFG and PAFG were possibly derived from the reworked ancient crustal material and formed in a post-collisional setting.

(3)

The structural analysis showed that the foliated AFG underwent ductile deformation converting into protomylonite, mylonite, or ultramylonite. The mylonitic foliation stroke NE-ENE and dipped to NW. The foliated PAFG was weakly deformed in a ductile regime and characterized by very thin ultramylonite zones having a width of few millimeters. Asymmetric structures (e.g., S-C fabric) indicated a dextral sense of movement with minor extension.

(4)

Based on field relationship and zircon U-Pb dating, it could be concluded that the ductile deformation might have been initiated after emplacement of the AFG and terminated soon after emplacement of the foliated PAFG.

(5)

The Statherian igneous activities in the region of the southwestern part of the Korean Peninsula could be well correlated with those occurring in the midwestern Gyeonggi Massif and in the eastern NCC.