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Simplified geological map of the Wutai-Hengshan-Fuping area (modified after Wilde et al., 2005; Zhao et al., 2007).
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... area, one of typical representative exposed Precambrian basements in the North China Craton (NCC), is located in the central part of Trans-North China Orogen (TNCO) (Fig. 1). The area is composed of three parts, i.e., the Hengshan, Fuping and Wutai complexes (Fig. 2). The Hengshan and Fuping complexes are characterized by grey tonalite-trondhjemite-granodiorite (TTG) gneisses, mafic granulites and supracrustal rock assemblages at amphibolite to granulite facies metamorphic grade ( Kröner et al., 2005;Tian et al., 1996;Zhao et al., 2001), whereas the Wutai complex is represented by low-grade ...
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... Zanhuang and Wutai complexes. There still exists numerous researches focusing on their tectonic setting (a retro-arc foreland basin or a riftrelated basin setting; Du et al., 2017;Peng et al., 2017), which are helpful for figuring out the tectonic evolution of the TNCO. The Wutai-Hengshan-Fuping area is located in the central part of the TNCO (Fig. 2) and attracts many geologists to carry out extensive studies due to its well-exposed lithologically representative basement ( Wilde et al., 1997). The Hengshan complex is separated from the Wutai by the broad valley of the Hutuo River, while the Wutai-Fuping boundary is a clear tectonic feature-the Longquanguan ductile shear zone ( Fig. ...
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... TNCO (Fig. 2) and attracts many geologists to carry out extensive studies due to its well-exposed lithologically representative basement ( Wilde et al., 1997). The Hengshan complex is separated from the Wutai by the broad valley of the Hutuo River, while the Wutai-Fuping boundary is a clear tectonic feature-the Longquanguan ductile shear zone ( Fig. 2; Li and Qian, 1991;Zhang et al., 2009;Zhao et al., 2007). Both Hengshan and Fuping complexes are the high-grade gneiss terranes, intervening with the low-grade terrane of the Wutai complex ( Wang et al., 1996). The Hengshan complex consists of four basic lithological assemblages, including the Hengshan mafic granulites and ...
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... partial melting of a juvenile source ( Liu et al., 2004). According to lithological assemblages and metamorphic grades, the Wutai Group is divided into Shizui, Taihuai and Gaofan subgroups. The lower Shizui Subgroup, which distributes widely in the northeastern and western part of the complex, has been metamorphosed to lower amphibolite facies ( Fig. 2; Bai, 1986), with arkose and minor limestone at the bottom (Banyukou Formation), tholeiite, BIF, chert and biotite schists interbedded with marbles and amphibolites in the middle (Jingangku Formation), and felsic volcanics, amphibolites and leptynites at the top (Zhuangwang-Wenxi Formation). Wilde et al. (2004a) reported zircon ages ...
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... the WutaiHengshan region, including four types of granodioritic gneiss, tonalitic gneiss, rhyolite and quartz diorite, of which one tonalitic gneiss and quartz diorite were taken from the Hengshan complex and the rest were collected in the Wutai complex. The sampling locations, field photographs and representative photomicrographs are shown in Figs. 2-4. Detailed petrographic feature descriptions of each sample analyzed in this study are given ...
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... granodioritic gneiss 12EK01 was collected from the Ekou orthogneisses ( Fig. 3a), exposed in the south of An'tou village (N 39°06′24″, E 113°14′43″) (Fig. 2). It is coarse-to medium-grained, evidently oriented and comprises of plagioclase (45%), alkali-feldspar (15%), quartz (30%) and biotite (10%) (Fig. 4a). Plagioclases occur as euhedral laths with mild sericitization and alkali-feldspars are mainly made up of microclines, displaying typical cross hatched twin. Biotites show as ...
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... (Fig. 3b), Guangmingshi ( Fig. 3c) and Dongshandi orthogneisses (Fig. 3d), exposed in the northeast of Zhangxiangou village (N 39°05′34″, E 113°38′21″), southwest of Lingdi village (N 39°03′43″, E113°35′55″), western part of Baizhiyan village (N 39°01′46″, E 113°39′40″) and Dongshandi village (N 39°12′54″, E 113°35′42″) respectively (Fig. 2). The Dongshandi tonalitic gneiss is intruded by tens of meters pegmatite dyke, which has dominant dark minerals of stumpy tourmaline (Fig. 3d). The samples show medium-to coarse-grained texture and prominent gneissic structure ( Fig. 4b-e), with the major mineral assemblage of plagioclase (50%-60%), quartz (30%-40%) and biotite ...
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... rhyolite HMY-1 was taken from the roadcut from Shahe to Taihuai town (N 39°03′21″, E 113°39′16″) (Fig. 2), about three kilometres from the basaltic andesite to rhyodacite of Hongmenyan sampled by Wilde et al. (2004a). It has evidently vesicular structure (Fig. 3e), blasto-porphyritic texture and contains 30 vol. % phenocrysts of quartz (50%), plagioclase (25%), K-feldspar (20%), biotite (5%) (Fig. 4f). Quartzs are the most dominant ...
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... investigated samples represent a tonalitic gneiss (sample 12YXZ07) and a quartz diorite enclave (12YXZ01) from the Yixingzhai Pluton, which are situated about 1 km west from Yixingzhai village (N 39°22′26″, E 113°35′59″) in Hengshan complex (Fig. 2). The Yixingzhai Pluton shows monolithic grey in color and displays a typical gneissic structure. It is intruded by younger mafic dykes dated at ∼2060 Ma ( Peng et al., 2012) and has dark enclaves which have similar component with the hosted rock (Fig. 3f). The tonalitic gneiss sample mainly consists of plagioclase (60%), quartz (20%), ...
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... tonalitic gneiss sample from the Chechang-Beitai Pluton is representative of the most voluminous igneous unit found within the Wutai complex (Fig. 2). The majority of zircons from sample 12WT02 are euhedral with lengths and length/width ratios ranging from 80-140 μm and 1:1-1.5:1 respectively (Fig. 5c). CL images of most zircon grains show oscillatory zoning patterns, and some of them have thin overgrowths which are too small to be analyzed (#04, #09, #15). In addition, a few ...
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... area, one of typical representative exposed Precambrian basements in the North China Craton (NCC), is located in the central part of Trans-North China Orogen (TNCO) (Fig. 1). The area is composed of three parts, i.e., the Hengshan, Fuping and Wutai complexes (Fig. 2). The Hengshan and Fuping complexes are characterized by grey tonalite-trondhjemite-granodiorite (TTG) gneisses, mafic granulites and supracrustal rock assemblages at amphibolite to granulite facies metamorphic grade ( Kröner et al., 2005;Tian et al., 1996;Zhao et al., 2001), whereas the Wutai complex is represented by low-grade ...
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... Wutai-Hengshan-Fuping area is located in the central part of the TNCO (Fig. 2) and attracts many geologists to carry out extensive studies due to its well-exposed lithologically representative basement ( Wilde et al., 1997). The Hengshan complex is separated from the Wutai by the broad valley of the Hutuo River, while the Wutai-Fuping boundary is a clear tectonic feature-the Longquanguan ductile shear zone ( Fig. ...
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... TNCO (Fig. 2) and attracts many geologists to carry out extensive studies due to its well-exposed lithologically representative basement ( Wilde et al., 1997). The Hengshan complex is separated from the Wutai by the broad valley of the Hutuo River, while the Wutai-Fuping boundary is a clear tectonic feature-the Longquanguan ductile shear zone ( Fig. 2; Li and Qian, 1991;Zhang et al., 2009;Zhao et al., 2007). Both Hengshan and Fuping complexes are the high-grade gneiss terranes, intervening with the low-grade terrane of the Wutai complex ( Wang et al., 1996). The Hengshan complex consists of four basic lithological assemblages, including the Hengshan mafic granulites and ...
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... to lithological assemblages and metamorphic grades, the Wutai Group is divided into Shizui, Taihuai and Gaofan subgroups. The lower Shizui Subgroup, which distributes widely in the northeastern and western part of the complex, has been metamorphosed to lower amphibolite facies ( Fig. 2; Bai, 1986), with arkose and minor limestone at the bottom (Banyukou Formation), tholeiite, BIF, chert and biotite schists interbedded with marbles and amphibolites in the middle (Jingangku Formation), and felsic volcanics, amphibolites and leptynites at the top (Zhuangwang-Wenxi Formation). Wilde et al. (2004a) reported zircon ages ...
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... the WutaiHengshan region, including four types of granodioritic gneiss, tonalitic gneiss, rhyolite and quartz diorite, of which one tonalitic gneiss and quartz diorite were taken from the Hengshan complex and the rest were collected in the Wutai complex. The sampling locations, field photographs and representative photomicrographs are shown in Figs. 2-4. Detailed petrographic feature descriptions of each sample analyzed in this study are given ...
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... granodioritic gneiss 12EK01 was collected from the Ekou orthogneisses ( Fig. 3a), exposed in the south of An'tou village (N 39°06′24″, E 113°14′43″) (Fig. 2). It is coarse-to medium-grained, evidently oriented and comprises of plagioclase (45%), alkali-feldspar (15%), quartz (30%) and biotite (10%) (Fig. 4a). Plagioclases occur as euhedral laths with mild sericitization and alkali-feldspars are mainly made up of microclines, displaying typical cross hatched twin. Biotites show as ...
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... (Fig. 3b), Guangmingshi ( Fig. 3c) and Dongshandi orthogneisses (Fig. 3d), exposed in the northeast of Zhangxiangou village (N 39°05′34″, E 113°38′21″), southwest of Lingdi village (N 39°03′43″, E113°35′55″), western part of Baizhiyan village (N 39°01′46″, E 113°39′40″) and Dongshandi village (N 39°12′54″, E 113°35′42″) respectively (Fig. 2). The Dongshandi tonalitic gneiss is intruded by tens of meters pegmatite dyke, which has dominant dark minerals of stumpy tourmaline (Fig. 3d). The samples show medium-to coarse-grained texture and prominent gneissic structure ( Fig. 4b-e), with the major mineral assemblage of plagioclase (50%-60%), quartz (30%-40%) and biotite ...
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... rhyolite HMY-1 was taken from the roadcut from Shahe to Taihuai town (N 39°03′21″, E 113°39′16″) (Fig. 2), about three kilometres from the basaltic andesite to rhyodacite of Hongmenyan sampled by Wilde et al. (2004a). It has evidently vesicular structure (Fig. 3e), blasto-porphyritic texture and contains 30 vol. % phenocrysts of quartz (50%), plagioclase (25%), K-feldspar (20%), biotite (5%) (Fig. 4f). Quartzs are the most dominant ...
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... investigated samples represent a tonalitic gneiss (sample 12YXZ07) and a quartz diorite enclave (12YXZ01) from the Yixingzhai Pluton, which are situated about 1 km west from Yixingzhai village (N 39°22′26″, E 113°35′59″) in Hengshan complex (Fig. 2). The Yixingzhai Pluton shows monolithic grey in color and displays a typical gneissic structure. It is intruded by younger mafic dykes dated at ∼2060 Ma ( Peng et al., 2012) and has dark enclaves which have similar component with the hosted rock (Fig. 3f). The tonalitic gneiss sample mainly consists of plagioclase (60%), quartz (20%), ...
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... tonalitic gneiss sample from the Chechang-Beitai Pluton is representative of the most voluminous igneous unit found within the Wutai complex (Fig. 2). The majority of zircons from sample 12WT02 are euhedral with lengths and length/width ratios ranging from 80-140 μm and 1:1-1.5:1 respectively (Fig. 5c). CL images of most zircon grains show oscillatory zoning patterns, and some of them have thin overgrowths which are too small to be analyzed (#04, #09, #15). In addition, a few ...
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... Previous studies have revealed that the calc-alkaline granitoid and volcanic rocks in the Wutai greenstone belt represent the earliest evidence of arc-related magmatism in the TNCO at 2560-2520 Ma [18,19]. Similarly aged 2560-2438 Ma granitoids have been recognized in other Terranes of the TNCO, including Xuanhua, Huai'an, Hengshan, Wutai, Fuping, Yunzhongshan, and Zhongtiao Complexes [2,[20][21][22][23][24][25][26][27][28][29][30][31]. Located in the westernmost margin of the TNCO (Figure 2), the Lüliang Complex represents the most viable area for constraining the above debates. ...
... Of the I-type group, Loiselle and Wones [74] introduced the A-type subgroup, which was further studied by Collins et al. [75]. The granitoids in this study can [26,27,29,38,63,109,110,112,113,118,119,[128][129][130][131][132][133][134][135][136][137]. The depleted mantle evolution trend (DM) was constructed using the modern-day values of mid-ocean ridge basalts [138]. ...
... Additionally, multiple terranes in the TNCO have recorded magmatic events during the Neoarchean period. For instance, the Datong-Huai'an Complex contains the TTGs emplaced at 2538-2497 Ma [25]; the Hengshan Complex contains the diorites, TTGs and volcanics with the age range of 2538-2483 Ma [26]; the Wutai Complex has granitoids with emplacement ages of 2560-2519 Ma [27]; the Fuping Complex has the TTG rocks emplaced at 2513 ± 13 Ma [28]. The Yunzhongshan area contains granitoid gneisses and metamorphosed volcanosedimentary sequences formed at 2535-2486 Ma [29]; and the Zhongtiao Complex contains the Zhaizi and Xiyao TTGs formed at 2560-2536 Ma [30,31]. ...
There has been a long debate regarding the timing of the final amalgamation of the North China Craton, which is considered to have occurred either during the Neoarchean or Paleoproterozoic era. One major point of contention is whether there existed a long-lived subduction lasting through the Neoarchean to Paleoproterozoic. The Lüliang Complex contains multiphases of magmatism and thus represents the most viable region to address this controversy. In this study, we carried geochronological and geochemical analysis on the representative granitoids. Secondary ion mass spectrometry U–Pb dating revealed four distinct granitoid groups emplaced at 2531 ± 4, 2189–2173, 2027 ± 25, and 1852 ± 41 Ma, respectively. Notably, the 2531 Ma granitic gneiss was identified for the first time in this region. Based on the geochemical characteristics, the granitoids can be divided into two types. The 2531 and 2027 Ma groups display I-type features, while the 2189–2173 and 1852 Ma groups exhibit A-type geochemical affinities. Both I-type groups exhibit enrichment in Rb, depletion in Nb, Ta, and Ti, moderate fractionated REE patterns, substantial negative Eu anomalies, low Sr/Y ratios, and positive εHf(t) (+3.51 to +5.53 and +5.59 to +7.32, respectively), indicating that they were generated from partial melting of the juvenile mafic crust. In contrast, the 2189–2173 Ma granitoids belong to A2-type and were most likely generated by the partial melting of felsic rocks in the back-arc region, while the 1852 Ma granitoids belong to A1-type and were most possibly the result of partial melting of mafic-intermediate rocks during the post-collisional stage. Based on the records of A-type granitic magmatism and the ~1950 Ma peak metamorphism throughout the Trans-North China Orogen, we propose that a long-lived subduction process (2531–1950 Ma) can mostly explain the existing geological phenomena. It is likely that the subduction between the Eastern and Western Blocks should have commenced at ~2531 Ma, followed by a long-lived subduction. The two blocks ultimately collided with each other to form the North China Craton at ~1950 Ma, which triggered post-collisional exhumation and partial melting at ~1852 Ma.
