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Tectonic History of the Kolyvan-Tomsk Folded Zone (KTFZ), Russia: Insight from Zircon U/Pb Geochronology and Nd Isotopes

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Tectonic History of the Kolyvan-Tomsk Folded Zone (KTFZ), Russia: Insight from Zircon U/Pb Geochronology and Nd Isotopes Tectonic history of the Kolyvan-Tomsk folded zone (KTFZ), Russia: Insight from zircon U/Pb geochronology and Nd isotopes Item Type Article Authors Zhimulev, Fedor I.; Gillespie, Jack; Glorie, Stijn; Jepson, Gilby; Vetrov, Evgeny V.; De Grave, Johan Citation Zhimulev, FI, Gillespie, J, Glorie, S, Jepson, G, Vetrov, EV, De Grave, J. Tectonic history of the Kolyvan–Tomsk folded zone (KTFZ), Russia: Insight from zircon U/Pb geochronology and Nd isotopes. Geological Journal. 2020; 55: 1913– 1930. https:// doi.org/10.1002/gj.3679 DOI 10.1002/gj.3679 Publisher WILEY Journal GEOLOGICAL JOURNAL Rights © 2019 John Wiley & Sons, Ltd. Download date 27/09/2021 15:01:23 Item License http://rightsstatements.org/vocab/InC/1.0/ Version Final accepted manuscript Link to Item http://hdl.handle.net/10150/641031 1 Tectonic history of the Kolyvan-Tomsk folded zone (KTFZ), Russia: insight from zircon 2 U/Pb geochronology and Nd isotopes 3 Fedor I. Zhimuleva*, Jack Gillespieb, Stijn Glorieb, Gilby Jepsonb, c, Evgeny V. Vetrova, d, 4 Johan De Gravee 5 a Sobolev Institute of Geology and Mineralogy Siberian Вrаnch Russian Academy of 6 Sciences, Novosibirsk 630090 Koptuga ave. 3, Russia 7 b Tectonics, Resources and Exploration (TraX), Department of Earth Sciences, University of 8 Adelaide, Adelaide, Australia 9 c Department of Geosciences, University of Arizona, Tucson, AZ, USA 10 11 d Siberian Research Institute of Geology, Geophysics and Mineral Resources, Novosibirsk, 12 630099 Krasniy ave. 35, Russia. 13 e Department of Geology, Ghent University, Krijgslaan 281.S8, WE13, 9000 Gent, Belgium 14 15 * Corresponding author: 16 Sobolev Institute of Geology and Mineralogy Siberian Вrаnch Russian Academy of Sciences, 17 Novosibirsk, Russia 18 [email protected], [email protected] 19 20 21 Abstract 22 The Kolyvan-Tomsk folded zone (KTFZ) represents part of the Central Asian Orogenic Belt 23 (CAOB). The KTFZ is mainly composed of detrital late Paleozoic sedimentary deposits, with 24 minor intrusions. Detrital zircon geochronology on the Upper Devonian to lower Permian 25 sedimentary sequences of the KTFZ and the associated Gorlovo foreland basin yield four age 26 peaks, reflecting the magmatic events in the source terranes. These events consist of (1) a 27 minor Neoproterozoic peak (0.9-0.7 Ga), (2) a significant early Paleozoic peak (550-460 Ma) 28 with a maximum at 500 Ma, and two well defined late Paleozoic peaks during (3) the Middle- 29 Late Devonian (385-360 Ma) and (4) the Carboniferous- early Permian (360-280 Ma), with a 30 maximum at 320 Ma. Older zircons (>1 Ga) are quite rare in the sampled sedimentary 31 sequences. Slightly negative εNd values and associated relatively young Nd model ages were 32 obtained (εNd(T)= -0.78, T(DM) ~1.1 Ga for Upper Devonian sandstones, εNd(T)= -1.1, 33 T(DM) ~1.1 Ga for lower Permian sandstones), suggesting only minor contribution of ancient 34 continental crust to the main sedimentary units of the KTFZ. All intrusive and volcaniclastic 35 rocks on the contrary are characterized by high positive εNd(T) values in the range of 3.78– 36 6.86 and a late Precambrian model age (T(DM)=581–916 Ma), which corroborates its 37 juvenile nature and an important depleted mantle component in their source. The oldest unit 38 of the KTFZ, the Bugotak volcanic complex formed at the Givetian – early Frasnian 39 transition, at about 380 Ma. Upper Devonian detrital deposits of the KTFZ were formed in 40 the early Paleozoic accretion belt of the Siberian continent, and specifically in a passive 41 continental margin environment. Deposits of the Gorlovo foreland basin, adjoining the KTFZ, 42 were accumulated as a result of erosion of the Carboniferous – early Permian volcanic rocks, 43 that are now buried under the Meso-Cenozoic sedimentary cover of the West Siberian Basin. 44 The magmatic events, recorded in the KTFZ zircon data, correspond to the most significant 45 magmatic stages that affected the western part of the CAOB as a whole. 46 Highlights 47 Volcanism in the Kolyvan-Tomsk folded zone occurred during the Middle to Late Devonian. 48 Source province for the Kolyvan-Tomsk folded zone sediments was the Salair terrane. 49 Source rocks for the Gorlovo basin deposits were Carboniferous magmatic complexes. 50 There are no early Precambrian crustal blocks in the Kolyvan-Tomsk folded zone. 51 52 Keywords: Atai-Sayan, Central Asian Orogenic Belt, detrital zircon geochronology, 53 Devonian, magmatism, Nd isotope composition, West Siberia, 54 55 56 1. INTRODUCTION 57 The Kolyvan-Tomsk folded zone (KTFZ) is located at the junction of the Altai-Sayan fold 58 belt (ASFA) (e.g. Buslov et al. 2013; Glorie et al. 2011), and the Ob`-Zaisan folded belt 59 (Matveevskaya, 1969) in the northern Central Asian Orogenic Belt (CAOB) (Wilhem, 60 Windley, & Stampfli, 2012; Windley, Alexeiev, Xiao, Kröner, & Badarch 2007, Xiao et al., 61 2009; Xiao, Huang, Han, Sun, & Li, 2010) (Figure1). The CAOB is the largest Phanerozoic 62 accretionary orogen in the world, located between the East-European, Siberian, Tarim and 63 North China cratons (Figure 1) and consists of a collage of different terranes: fragments of 64 microcontinents, volcanic arcs, and accretionary complexes (Wilhem et al., 2012, Windley at 65 al., 2007, Xiao et al., 2009, 2010). In recent decades, the tectonic structure and evolution of 66 the CAOB has been an important topic for various geological and geochronological studies, 67 due to its importance in terms of metallogeny, geohazards and fundamental geoscientific 68 issues such as the growth of the continental crust (e. g. Goldfarb, Taylor, Collins, Goryachev, 69 & Orlandini, 2014, Jahn, Wu, & Chen, 2000, Kröner et al., 2014, Safonova 2017, Sengör, 70 Natal’in, & Burtman, 1993, Wang et al., 2009, 2014, Windley et al., 2007, Xiao et al., 2010). 71 The presumed presence of ancient continental crustal blocks in the basement of the 72 overprinted sedimentary basins, such as Junggar, Ili, Minusa, Kuznetsk and others is a hotly 73 debated topic (Zhao, Chen, Deng, Shao & Ma, 2019). The Ob`-Zaisan folded system runs 74 through eastern Kazakhstan and northwestern China, east of the Altai-Sayan (Figure 1). The 75 Ob`-Zaisan system includes the KTFZ with a characteristic NE strike, and the NW-striking 76 Rudny Altai folded zone. This difference in orientation can be explained as a result of 77 oroclinal bending (Choulet et al., 2011; Li et al., 2017, 2018; Sengör et al., 1993; Vladimirov 78 et al., 2005; Zonenshain, Kuzmin & Natapov, 1990). Berzin et al., (1994) suggested that the 79 propagation of the KTFZ to the south is represented by the Rudny Altai folded zone, although 80 this is difficult to ascertain as the junction between the Rudny Altai and KTFZ is covered by 81 the thick Meso-Cenozoic sediments of the West Siberian Basin (WSB). Despite numerous 82 studies by Russian geologists, which focused on geological mapping (Babin et al., 2015, 83 Belyaev & Nechaev 2015, Kotel’nikov Maksimov, Kotel’nikova, Makarenko & Subbotin 84 2008), paleontology and biostratigraphy (Izokh & Yazikov, 2015, Yazikov, Izokh, Shirokikh 85 & Kutolin, 2015), ore resources (Kalinin, Naumov, Borisenko, Kovalev, & Antropova, 2015), 86 petrology (Kungurtsev et al., 1998; Sotnikov, Fedoseev, Ponomarchuk, Borisenko & Berzina 87 2000), and some associated overview monographs published in Russian (Roslyakov et al., 88 2001, Sotnikov et al., 1999, Sviridov et al., 1999; Vrublevskii Nagorniy, Rubtsov, & Erv’ye 89 1987), the KTFZ remains very poorly constrained in terms of geochronology. Whereas the 90 geochronology of the Chinese and to a lesser extent the Russian Altai has been intensively 91 studied (e.g. Cai et al., 2016, Chen et al., 2015, 2016, Dong et al., 2018, Glorie et al., 2011, Li 92 et al., 2017, Long et al., 2007, Kruk, Kuibida, Shokalskiy, Kiselev & Gusev, 2018), the 93 northern extension of these structures in the Kolyvan-Tomsk and Salair regions remains very 94 poorly characterized concerning its geochronologic frame work. Currently, there are no zircon 95 U-Pb ages and for magmatic intrusions or sedimentary sequences in the KTFZ published 96 within the international literature. The tectonic environment of sedimentation and magmatism 97 in this zone thus remains poorly understood, making it difficult to accurately correlate the 98 KTFZ with the late Paleozoic folded zones of Eastern Kazakhstan (e.g. Glorie et al., 2012, 99 Vladimirov et al., 2005,) and north-western China in the context of CAOB evolution (e.g. 100 Choulet et al., 2011; 2012; Hong et al., 2017; Li et al., 2017; 2018; Liu, Han, Gong, & Chen, 101 2019; Long et al., 2007; Zhou et al., 2017). 102 The KTFZ along its entire length is composed of fairly homogeneous along-strike late 103 Devonian-Carboniferous carbonate-detrital deposits. Volcanic and intrusive rocks are 104 relatively scarce. The tectonic setting in which this sedimentary unit was deposited is not 105 completely defined. Dating of the detrital zircons from these deposits will provide valuable 106 information about the source provenance, basin evolution, sedimentation rates, and the 107 general character of the tectonic events in the region. Volcanic rocks, lying at the base of the 108 sedimentary unit, have been dated in this work, to provide a geochronological constraint on 109 the onset of this particular regional tectonic cycle. Nd isotope composition of the intrusive, 110 volcanic and sedimentary rocks of the KTFZ was measured to estimate the age of the 111 continental crust and to evaluate a possible contribution of the recycled ancient crustal 112 material. The geochronological results on the KTFZ rocks presented here, are an important 113 contribution to our understanding of the tectonic evolution of the less studied north-western 114 part of CAOB during the late Paleozoic. 115 116 2. GEOLOGICAL SETTING 117 The KTFZ is located at the north-western edge of the Altai-Sayan folded area (ASFA) (Figure 118 1), extending to the north-east for a distance of about 450 km, with a width of 60-100 km 119 (Figure 2).
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