| Citation: |
Ya-ying Wang, Ling-sen Zeng, Li-e Gao, Li-long Yan, Ling-hao Zhao, Jia-hao Gao, Ying-long Di, Guang-xu Li, Yi-hong Tian, 2024. The plume-lithosphere interaction in the Comei Large Igneous Province: Evidence from two types of mafic dykes in Gyangze, south Tibet, China, China Geology, 7, 80-90. doi: 10.31035/cg2023023
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The plume-lithosphere interaction in the Comei Large Igneous Province: Evidence from two types of mafic dykes in Gyangze, south Tibet, China
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Abstract
Two suites of mafic dykes, T1193-A and T1194-A, outcrop in Gyangze area, southeast Tibet. They are in the area of Comei LIP and have indistinguishable field occurrences with two other dykes in Gyangze, T0902 dyke with 137.7±1.3 Ma zircon age and T0907 dyke with 142±1.4 Ma zircon age reported by Wang YY et al. (2016), indicating coeval formation time. Taking all the four diabase dykes into consideration, two different types, OIB-type and weak enriched-type, can be summarized. The “OIB-type” samples, including T1193-A and T0907 dykes, show OIB-like geochemical features and have initial Sr-Nd isotopic values similar with most mafic products in Comei Large Igneous Provinces (LIP), suggesting that they represent melts directly generated from the Kerguelen mantle plume. The “weak enriched-type” samples, including T1194-A and T0902 dykes, have REEs and trace element patterns showing within-plate affinity but have obvious Nb-Ta-Ti negative anomalies. They show uniform lower εNd(t) values (−6‒−2) and higher 87Sr/86Sr(t) values (0.706‒0.709) independent of their MgO variation, indicating one enriched mantle source. Considering their closely spatial and temporal relationship with the widespread Comei LIP magmatic products in Tethyan Himalaya, these “weak enriched-type” samples are consistent with mixing of melts from mantle plume and the above ancient Tethyan Himalaya subcontinental lithospheric mantle (SCLM) in different proportions. These weak enriched mafic rocks in Comei LIP form one special rock group and most likely suggest large scale hot mantle plume-continental lithosphere interaction. This process may lead to strong modification of the Tethyan Himalaya lithosphere in the Early Cretaceous.
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References
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Ya-ying Wang, Ling-sen Zeng, Li-e Gao, Li-long Yan, Ling-hao Zhao, Jia-hao Gao, Ying-long Di, Guang-xu Li, Yi-hong Tian, 2024. The plume-lithosphere interaction in the Comei Large Igneous Province: Evidence from two types of mafic dykes in Gyangze, south Tibet, China, China Geology, 7, 80-90. doi: 10.31035/cg2023023
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Figure 1.
a‒Physiographic map of the Indian Ocean and surrounding continents, showing spatial-temporal locations of the Comei LIP and other products created by the Kerguelen plume (after Zhu DC et al., 2008); b‒sketch tectonic map of the east-central Tethyan Himalaya and eastern India showing the present location of the Comei LIP (after Zhu DC et al., 2009); c‒simplified geologic map showing spatial extent and distributions of Comei LIP (after Wang YY et al., 2022) and the location of T1193-A and T1194-A dykes. Other samples, T0902 and T0907, in Gyangze are from Wang YY et al. (2016).
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Figure 2.
Microphotographs of diabase dyke samples in Gyangze (a) T1193-A and (b) T1194-A.
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Figure 3.
Classification of diabase dyke samples in Gyangze. a‒IUGS-recommended TAS diagram of Le Bas MJ and Streckeisen AL (1991); b‒an immobile element-based TAS proxy diagram (after Floyd PA and Winchester JA, 1975). T0907 and T0902 samples are from Wang YY et al., (2016).
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Figure 4.
Variation diagrams of major oxides (%) versus MgO (%) of Gyangze samples in Comei LIP. T0907 and T0902 samples are from Wang YY et al., (2016). All major oxide percentages were recalculated after removing their LOI values.
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Figure 5.
(a and c) Rare earth element distribution diagrams and (b and d) trace element distribution diagrams. The shaded areas are coeval Gyangze samples from Wang YY et al. (2016). Data of chondrite, primitive mantle, OIB, E-MORB and N-MORB are from Sun SS and McDonough WF (1989).
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Figure 9.
a–87Sr/86Sr(t) vs. εNd(t) diagram and b–Nb/La vs. εNd(t) diagram of diabase samples in Gyangze.
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Figure 6.
Tectonic environment discrimination diagram of diabase samples from Gyangze. (a) Zr–Zr/Y diagram (Pearce JA, 1982), WPB: within-plate basalt, MORB: mid-ocean ridge basalt, IAB: island arc basalt and (b) Ti/1000 -V linear plot (Shervais JW, 2022). The shaded areas are “most mafic products in Comei LIP” from OIB-end member samples (Wang YY et al., 2022).
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Figure 7.
a–Nb/Yb-Th/Yb (after Pearce JA, 2008); b–Zr/Y-Nb/Y (after Fitton JG et al., 1997) diagrams of diabase samples in Gyangze. The shaded areas are “most mafic products in Comei LIP” from OIB-end member samples (after Wang YY et al., 2022).
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Figure 8.
Plots of (a) Nd/Pb vs. MgO, (b) Nb/U vs. MgO, (c) εNd(t) vs. MgO, and (d) 87Sr/86Sr(t) vs. MgO of Gyangze samples. The data of OIB, N-MORB, and CC (continental crust) are after Sun SS and McDonough WF (1989) and Rudnick RL and Gao S (2003), respectively. Results show that these diagnostic values sensitive to crustal contamination are nearly uniform within T1194-A samples, independent of MgO variation and do not show AFC trend.
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Figure 10.
a–Nb/U-Nb/La plot; b–Ce/Pb-Nb/La plots of diabase samples in Gyangze. The shaded areas are “most mafic products in Comei LIP” from OIB-end member samples (after Wang YY et al., 2022).
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Figure 11.
A proposed model of formation of OIB-type and weak enriched rocks in Comei LIP.