Genesis of Carboniferous volcanic rocks in northeastern Junggar Basin: New insights into the Junggar Ocean closure

doi:10.13745/j.esf.sf.2021.12.2

Abstract

Abstract:

The Junggar Ocean is an important branch of the northern Paleo-Asian Ocean and part of its stage evolution. However, the subduction and closure time of the Junggar Ocean and the basement property of the Junggar Basin are still unclear. In this study, Carboniferous volcanic rocks including basalts, basaltic andesites, and andesites in the northeastern margin of the Junggar Basin (Wulungu area) were investigated to reveal their magmatic provenance and formation mechanism. Combined with major and trace element and Sr-Nd isotope analysis, the closure time of the Junggar Ocean during the Late Paleozoic was further clarified. Three types of basement volcanic rocks with low TiO₂ (0.60%-0.84%) and relatively high alkaline (1.18%-8.59%) contents were identified. The basalts belong to tholeiitic series while andesites to high calc-alkaline series, indicating a volcanic arc association. The low-medium ⁸⁷Sr/⁸⁶Sr_(i) ratios (0.703250- 0.704559) and relatively depleted ε_Nd(t) (+4.8-+6.8) and t_DM2 (483-625 Ma) values suggested all three types formed from fractional crystallization of depleted mantle magmas, with andesites formed later than the others. Trace element and isotope tracing suggested the volcanic rocks originated from mantle wedge metasomatized by slab-derived fluid, with andesites more impacted by crustal contamination. The volcanic rocks were enriched in LILEs (Ba, Sr), Pb, Zr and Hf, and showed strong negative Nb and Ta anomalies. These characteristics are consistent with the tectonic setting of a subduction zone. The rock series showed enrichments of incompatible elements (Th, U, K) and LREE, high Ba/La ratio (30.14-208.86), low TiO₂ content (0.60%-0.84%), and low Ce/NB (8.71-12.05) and Th/Nb (0.93-1.74) ratios. These characteristics support the continuing Carboniferous Junggar Ocean subduction along the continental block, which led to island arc accretion, followed by Junggar Ocean closure in the Late Carboniferous (ca. 305.5±4.4 Ma) and subduction-related magma superposition onto the continental crust through island arc. The above results provided new basis for the understanding of basement formation in the Junggar Basin.

Key words: Junggar Basin, Wulungu, Carboniferous, volcanic rocks, island arc, petrogenesis

CLC Number:

P588.14

JIAO Xiaoqin, ZHANG Guanlong, NIU Huapeng, WANG Shengzhu, YU Hongzhou, XIONG Zhengrong, ZHOU Jian, GU Wenlong. Genesis of Carboniferous volcanic rocks in northeastern Junggar Basin: New insights into the Junggar Ocean closure[J]. Earth Science Frontiers, 2022, 29(4): 385-402.

Figures/Tables 11

Fig.1 Simplified geological maps of the study area. (a) Geological sketch map of northwestern China, (b) tectonic sketch map of Junggar Basin (modified after [42-43]), and (c) geological sketch map of Wulungu

Fig.2 Compositions and structural characteristics of intermediate-basic volcanic rocks of Wulungu

Table 1 Results of major and trace element analysis of Carboniferous volcanic rocks of Wulungu

Fig.3 Classification diagrams for Carboniferous volcanic rocks of Wulungu. (a) (K2O+Na2O) vs. SiO2 diagram (adapted from [50]). (b) Zr/TiO2 vs. Nb/Y diagram (adapted from [51]). (c) K2O vs. SiO2 diagram (adapted from [52]). (d) AFM diagram (adapted from [53]).

Fig.4 Chondrite-normalized REE patterns (a) and primitive mantle-normalized trace element spidergrams for Carboniferous volcanic rocks of Wulungu (b). Chondrite-normalized and primitive mantle-normalized values from [56].

Table 2 Sr-Nd isotope compositions of Carboniferous volcanic rocks of Wulungu

样品号	岩性	Age/ Ma	w_B/10^-6		⁸⁷Rb/⁸⁶Sr	⁸⁷Sr/⁸⁶Sr	±2σ	(⁸⁷Sr/⁸⁶Sr)_i	w_B/10^-6		¹⁴⁷Sm/¹⁴⁴Nd	¹⁴³Nd/¹⁴⁴Nd	±2σ	(¹⁴³Nd/¹⁴⁴Nd)_t	ε_Nd(t)	t_DM1/ Ma	t_DM2/ Ma
样品号	岩性	Age/ Ma	Rb	Sr	⁸⁷Rb/⁸⁶Sr	⁸⁷Sr/⁸⁶Sr	±2σ	(⁸⁷Sr/⁸⁶Sr)_i	Sm	Nd	¹⁴⁷Sm/¹⁴⁴Nd	¹⁴³Nd/¹⁴⁴Nd	±2σ	(¹⁴³Nd/¹⁴⁴Nd)_t	ε_Nd(t)	t_DM1/ Ma	t_DM2/ Ma
WG-2	玄武岩	305	9.8	306	0.09	0.704 875	0.000 009	0.704 474	1.64	5.70	0.174 0	0.512 939	0.000 009	0.512 939	6.8	810	483
WG-3	玄武岩	305	6.5	235	0.08	0.704 904	0.000 007	0.704 559	1.62	5.52	0.177 4	0.512 932	0.000 003	0.512 932	6.5	916	502
WG-4	玄武质安山岩	332	88.6	480	0.53	0.706 109	0.000 010	0.703 586	4.26	18.80	0.137 0	0.512 830	0.000 003	0.512 830	6.3	637	540
WG-5	玄武质安山岩	332	73.6	506	0.42	0.705 517	0.000 006	0.703 529	4.27	19.50	0.132 4	0.512 842	0.000 007	0.512 842	6.7	578	510
WG-6	安山岩	312	48.8	360	0.39	0.706 081	0.000 009	0.704 340	3.21	16.80	0.115 5	0.512 779	0.000 004	0.512 779	6.0	577	543
WG-7	安山岩	312	66.4	265	0.72	0.707 399	0.000 009	0.704 180	4.55	21.30	0.129 1	0.512 746	0.000 004	0.512 746	4.8	729	625
WG-1	安山岩	312	244.0	244	2.90	0.716 107	0.000 007	0.703 250	6.45	31.00	0.125 8	0.512 831	0.000 005	0.512 831	6.6	554	501

Fig.5 εNd(t) vs. 87Sr/86Sr(i) plot for Carboniferous volcanic rocks of Wulungu (adapted from [58]). LC—lower crust; UC—upper crust; DM—depleted mantle.

Fig.6 Geochemical classification plots for Carboniferous volcanic rocks of Wulungu. (a) 87Sr/86Sr(i) vs. SiO2 (adapted from [60]). (b) 143Nd/144Nd(t) vs. SiO2. (c) Nb/Zr vs. Th/Zr (adapted from [59]);(d) Th/Yb vs. Nb/Yb (adapted from [71]).

Fig.7 Relationships between SiO2 and oxides in Carboniferous volcanic rocks of Wulungu

Fig.8 Tectonic discrimination diagrams for Carboniferous volcanic rocks from Wulungu. (a) TiO2 vs. Zr (adapted from [54], data partly from [10,26]). (b) Ce/Nb vs. Th/Nb (adapted from [85], data partly from [10,26]).(c) Nb-Zr-Y diagram (adapted from [86]). (A1+A2)—WPB-alkaline basalts; (A2+C)—WPB tholeiite; B—E-MORB; (C+D)—volcanic basalts. (d) Hf/3-Th-Ta diagram (adapted from [21]).

Fig.9 A model for the tectonic evolution of Wulungu (modified after [21])

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