| Citation: |
Si-hong Jiang, Leon Bagas, Yi-fei Liu, Li-li Zhang, 2021. Archean (about 2500 Ma) anatexis in eastern North China Block, China Geology, 4, 215-229. doi: 10.31035/cg2021014
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Archean (about 2500 Ma) anatexis in eastern North China Block
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Abstract
Two Neoarchean alkaline feldspar-rich granites sourced from partially melted granulite-facies granodioritic orthogneiss have been here recognised in the eastern part of the North China Block (NCB). These poorly foliated granites have previously been assumed to be Mesozoic in age and never dated, and so their significance has not been recognised until now. The first granite (AG1) is a porphyritic syenogranite with megacrystic K-feldspar, and the second (AG2) is a quartz syenite with perthitic megacryst. Zircons from the granites yield LA-ICP-MS U-Pb ages of 2499 ± 10 Ma (AG1), and 2492 ± 28 Ma (AG2), which are slightly younger than the granodioritic orthogneiss that they intrude with a crystallisation U-Pb age of 2537 ± 34 Ma. The younger granites have higher assays for SiO2 (71.91% for AG1 and 73.22% for AG2) and K2O (7.52% for AG1 and 8.37% for AG2), and much lower assays for their other major element than the granodioritic orthogneiss. All of the granodioritic orthogneiss and granite samples have similar trace element patterns, with depletion in Th, U, Nb, and Ti and enrichment in Rb, Ba, K, La, Ce, and P. This indicates that the granites are derived from the orthogneiss as partial melts. Although they exhibit a similar REE pattern, the granites have much lower total REE contents (30.97×10−6 for AG1, and 25.93×10−6 for AG2), but pronounced positive Eu anomalies (Eu/Eu* = 8.57 for AG1 and 27.04 for AG2). The granodioritic orthogneiss has an initial 87Sr/86Sr ratio of 0.70144, εNd(t) value of 3.5, and εHf(t) values ranging from −3.2 to +2.9. The orthogneiss is a product of fractional crystallisation from a dioritic magma, which was derived from a mantle source contaminated by melts derived from a felsic slab. By contrast, the AG1 sample has an initial 87Sr/86Sr ratio of 0.6926 that is considered too low in value, εNd(t) value of 0.3, and εHf(t) values between +0.57 and +3.82; whereas the AG2 sample has an initial 87Sr/86Sr ratio of 0.70152, εNd(t) value of 1.3, and εHf(t) values between +0.5 and +14.08. These assays indicate that a Sr-Nd-Hf isotopic disequilibrium exists between the granite and granodioritic orthogneiss. The elevated εHf(t) values of the granites can be explained by the involvement of Hf-bearing minerals, such as orthopyroxene, amphibole, and biotite, in anatectic reactions in the granodioritic orthogneiss. Based on the transitional relationship between the granites and granodioritic orthogneiss and the geochemical characteristics mentioned above, it is concluded that the granites are the product of rapid partial-melting of the granodioritic orthogneiss after granulite-facies metamorphism, and their crystallisation age of about 2500 Ma provides the minimum age of the metamorphism. This about 2500 Ma tectonic-metamorphic event in NCB is similar to the other cratons in India, Antarctica, northern and southern Australia, indicating a possible connection between these cratons during the Neoarchean.
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Si-hong Jiang, Leon Bagas, Yi-fei Liu, Li-li Zhang, 2021. Archean (about 2500 Ma) anatexis in eastern North China Block, China Geology, 4, 215-229. doi: 10.31035/cg2021014
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Figure 1.
Geological map showing: a‒tectonic units of the NCB and location of the study area (modified from Zhao GC et al., 2005); b‒geological sketch map of the Malanyu Antiform in Eastern Hebei Province showing the locations of the samples for which U-Pb and Lu-Hf zircon analyses were completed (modified from Bai X et al., 2016 and Geological Survey of Hebei Province, 1970).
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Figure 2.
Photographs and photomicrographs of granodioritic orthogneiss, syenogranite, and quartz syenite from the Archean Malanyu Inlier. a‒granodioritic orthogneiss with moderate foliation and intruded lensoidal syenogranite dykes; b‒light red anatectic granite (AG1) showing transitional relationships with granodioritic orthogneiss; c‒anatectic granite (AG2) with dark perthitic megacryst; d‒medium-grained granodioritic orthogneiss sample JD16-049 consisting of aligned orthopyroxene, hornblende, biotite, plagioclase, and quartz; e‒syenogranite (AG1) sample JD16-050 with K-feldspar megacryst and veinlet-like quartz; f‒xenolith of the host granodioritic orthogneiss within syenogranite (AG1); g‒quartz syenite (AG2) sample JD16-052 with K-feldspar megacryst and fine-grained quartz and plagioclase. The polysynthetic twinning can still be seen in plagioclase; h‒quartz syenite (AG2) sample JD16-052 with small albite crystals in perthitic feldspar. Ab-albite; Hb‒hornblende; Bi‒biotite; Opx‒orthopyroxene; Kfs‒K-feldspar, Pl‒plagioclase; Q‒quartz; Xen-xenolith. All the photomicrographs are taken under cross-polarized light. The hammer and marker pen in the photographs are 410 mm and 140 mm long, respectively.
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Figure 3.
CL images of representative zircon grains from samples JD16-049, JD16-050, and JD16-052 showing the inner structures and analysed locations.
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Figure 4.
Zircon U-Pb concordia diagram for granodioritic orthogneiss, syenogranite, and quartz syenite samples from the Malanyu Antiform. a‒granodioritic orthogneiss; b‒syenogranite (AG1); c‒quartz syenite (AG2). The weighted mean age or upper intercept ages and MSWD are shown in each graph.
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Figure 5.
Normalisation plots. a‒chondrite-normalised REE plot; b‒primitive mantle normalised element spider plot for the granodioritic orthogneiss, syenogranite, and quartz syenite in the Malanyu Antiform. Chondrite normalising values from Taylor SR and McLennan SM (1985), and primitive mantle normalised values from Sun SS and McDonough WF (1989).
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Figure 6.
Plot of zircon U-Pb ages vs. εHf(t) values for zircons from the granodioritic orthogneiss, syenogranite, and quartz syenite in the Malanyu Antiform. The error bar for individual εHf(t) value was not shown, as most of them have error range less than 1.0 unit, and thus within the symbol if plotted. All εHf(t) values were calculated at the age of the rock.
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Figure 7.
Petrogenetic discrimination diagrams for granodioritic orthogneiss. a‒MgO vs SiO2 plot (after Martin H et al., 2005); b‒(La/Yb)N vs YbN plot discriminating between adakitic and classical arc calc-alkaline compositions (after Martin H, 1986). The data of dioritic and trondhjemitic gneisses were cited from Bai X et al. (2014). PMB‒experimental partial melts from basalts or amphibolites; LSA‒low-silica adakite; HSA‒high-silica adakite.
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Figure 8.
Chondrite-normalised REE patterns of analysed zircons from samples. a‒JD16-049; b‒JD16-050; c‒JD16-052. Chondrite normalising values from Taylor SR and McLennan SM (1985).
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Figure 9.
Th vs U diagram for the zircons from the granodioritic orthogneiss, syenogranite, and quartz syenite in the Malanyu Antiform.