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Precambrian to Early Cretaceous Rocks of the Strandja Massif (NW Turkey); Evolution of a Long Lasting Magmatic Arc

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Precambrian to Early Cretaceous Rocks of the Strandja Massif (NW Turkey); Evolution of a Long Lasting Magmatic Arc Canadian Journal of Earth Sciences Precambrian to Early Cretaceous rocks of the Strandja Massif (NW Turkey); evolution of a long lasting magmatic arc Journal: Canadian Journal of Earth Sciences Manuscript ID cjes-2016-0026.R2 Manuscript Type: Article Date Submitted by the Author: 20-Jul-2016 Complete List of Authors: Natal'in, Boris; Đstanbul Technical University, Geology Engineering Sunal, Gürsel;Draft Đstanbul Technical university Gun, Erkan; Đstanbul Technical University Wang, Bo; Department of Earth Sciences, Nanjing University, 210093, Nanjing, People’s Republic of China Zhiqing, Yang; nstitute of Geology, Chinese Academy of Geological Sciences The Strandja Massif, NW Turkey, Zircon U-Pb ages, magmatic setting, Keyword: tectonics https://mc06.manuscriptcentral.com/cjes-pubs Page 1 of 66 Canadian Journal of Earth Sciences 1 Precambrian to Early Cretaceous rocks of the Strandja Massif (NW 2 Turkey); evolution of a long lasting magmatic arc. 3 4 Boris A. Natal’in 1, Gürsel Sunal 1, Erkan Gün 2, Bo Wang 3; Yang Zhiqing 4 5 1) Đstanbul Teknik Üniversitesi, Jeoloji Mühendisliği Bölümü, 34469, Istanbul/Turkey 6 2) Đstanbul Teknik Üniversitesi, Avrasya Yer Bilimleri Enstitüsü, 34469, Istanbul/Turkey 7 3) State Key Laboratory for Mineral Deposits Research, Department of Earth Sciences, 8 Nanjing University, Nanjing 210093, China 9 4) Institute of Geology, Chinese Academy of Geological Sciences No.26, Baiwanzhuang 10 Road, Beijing, 100037 P.R. China 11 *Corresponding author; e-mail: [email protected], Tel: +90 212 2856221 12 13 Abstract Draft 14 The Strandja Massif, NW Turkey, forms a link between the Balkan Zone of Bulgaria, which 15 is correlated with Variscan orogen in Europe, and the Pontides, where Cimmerian structures 16 are prominent. Five fault-bounded tectonic units form the massif structure. 1) The Kırklareli 17 Unit consists of the Paleozoic basement intruded by the Carboniferous to Triassic Kırklareli 18 metagranites. It is unconformably overlain by Permian and Triassic metasediments. 2) The 19 Vize Unite that is made of Neoproterozoic metasediments, which are intruded by Cambrian 20 metagranites, and overlain by the pre-Ordovician molasse. Unconformably laying the 21 Ordovician quartzites pass upward into quartz schists and then to alternating marble and chert 22 of, possibly, latest Devonian age. Rocks of the Vize Unit are intruded by the late 23 Carboniferous metagranites. The Vize Unit may be correlated with the passive continental 24 margin of the Istanbul Zone. 3) The Mahya accretionary complex and 4) the paired Yavuzdere 25 magmatic arc were formed in the Carboniferous. 5) Nappes consisting of the Jurassic https://mc06.manuscriptcentral.com/cjes-pubs 1 Canadian Journal of Earth Sciences Page 2 of 66 26 dolomites and marbles thrust to the north in late Jurassic – early cretaceous time. They occupy 27 the highest structural position on all above-mentioned tectonic units. 28 Tectonic subdivision of the Strandja Massive is supported by new 18 ages of magmatic and 29 detrital zircons. 30 The long duration of subduction-related magmatism in the region and its continuity in the 31 Triassic contradicts with the widely accepted ideas about the dominance of the passive 32 continental margin settings in the tectonic evolution of the Strandja Massif. The massif is 33 interpreted as a fragment of the long-lived, Cambrian to Triassic Silk Road magmatic arc. At 34 least since the late Paleozoic this arc evolved on the northern side of Paleo-Tethys. 35 Key Words: The Strandja Massif, NWDraft Turkey, Zircon U-Pb ages, Magmatic setting 36 37 1. Introduction 38 The Neoproterozoic to Jurassic Strandja Massif belongs to the western Pontides (Şengör and 39 Yılmaz 1981). To the west, it continues to Bulgaria as the Balkan Zone (Haydoutov and 40 Yanev 1997), but the eastern continuation of the massif is unclear because of wide 41 distribution of the Eocene and younger cover deposits (Fig. 1). Okay et al. (1994) suggests 42 that the dextral West Black Sea Fault separates the massif and the easterly-located Istanbul 43 Zone, but Cretaceous magmatic rocks of the Pontide Arc are not displaced (Natal’in and Say 44 2015); thus, the junction between the Strandja Massif and the Istanbul Zone is problematic. 45 Traditionally, the structure of the Turkish part of the massif is interpreted as a Paleozoic 46 basement, which is intruded by Permian granitoids, with overlying Permo-Jurassic 47 metasedimentary cover (Aydın, 1974, 1982; Çağlayan and Yurtsever 1998; Okay et al 2001). 48 All of these units are metamorphosed in greenschist to low-amphibolite facies and strongly https://mc06.manuscriptcentral.com/cjes-pubs 2 Page 3 of 66 Canadian Journal of Earth Sciences 49 deformed in middle Jurassic-early Cretaceous times during the Cimmeride Orogeny (Okay et 50 al. 2001; Sunal et al. 2011; Natal’in et al. 2012b). 51 The Paleozoic basement is more widely exposed in the western part of the massif while the 52 Mesozoic cover mainly constitutes its eastern part. Çağlayan and Yurtsever (1998) subdivide 53 the Paleozoic and Mesozoic metamorphic rocks into more than 30 lithostratigraphic units. 54 However, the age control and convincing structural relations supporting this subdivision is 55 extremely limited. For instance, temporal control on stratigraphic relationships comes from a 56 Jurassic crinoid finding and from the Rb-Sr age of 244 Ma for the Kırklareli metagranite 57 (Çağlayan and Yurtsever 1998). Later, Okay et al. (2001) determined the U-Pb age of the 58 same metagranite as 271 Ma and Hagdorn and Göncüoglu (2007) found Triassic crinoids in 59 the metasedimentary cover. Recently,Draft Bedi et al. (2013) reported additional fossil findings in 60 the Triassic and Jurassic metasedimentary rocks, but we think that they do not principally 61 change the original ideas on the stratigraphy of the massif that has been developed by Aydın 62 (1974, 1982), Şengör et al. (1984), and Çağlayan and Yurtsever (1998). If the stratigraphy is 63 unclear, disagreements on the tectonic nature, correlations with surrounding tectonic units, 64 and understanding of the tectonic structure of the Strandja Massif would be too uncertain. For 65 instance, Şengör and Yılmaz (1981) consider it as a part of the Cimmerian continent (or part 66 of the Gondwana-Land), alternatively, Okay et al. (1996) assign it to the southern passive 67 continental margin of Eurasia. 68 Our work in the western part of the Strandja massif, the Kırklareli region (Fig. 2), has resulted 69 in the discovery of the late Carboniferous magmatic events, the recognition of the regional 70 metamorphism and deformation that happened between ~312 and ~257 Ma, and the 71 identification of strong penetrative fabric (S2 foliation and L 2 lineation), which almost 72 completely reworked the previous structures. These structures were formed in middle Jurassic 73 to early Cretaceous times under greenschist to low-amphibolite facies metamorphism https://mc06.manuscriptcentral.com/cjes-pubs 3 Canadian Journal of Earth Sciences Page 4 of 66 74 (Natal’in et al. 2005a, c; Sunal et al. 2006; Sunal et al. 2008; Natal’in et al. 2009; Natal’in et 75 al. 2012 a-d). The Ar-Ar ages of the S 2 foliation are between 165 and 157 Ma (Natal’in et al. 76 2005a and c) and Rb-Sr (whole rock and mica) ages of 134 −163 Ma (Sunal et al. 2011). 77 Studies in the eastern part of the massif (Kıyıköy region) have resulted in the recognition of 78 two critical rock assemblages. The first consists of clastic rocks (the Mahya Complex) 79 metamorphosed in greenschist facies with inclusions of deep-water (oceanic?) metachert, 80 metavolcanics, and meta-intrusive rocks of mafic and ultramafic compositions. The second 81 assemblage is the Yavuzdere Complex, which is made of metatuff, intermediate to felsic 82 metavolcanics, and metagranites. 83 Metamorphic grade and structural history of these two assemblages are similar to Mesozoic 84 rocks in the Kırklareli region. The sameDraft S 2 foliation appears as penetrative structure 85 throughout the study area. In many places, the L 2 stretching lineation shows the same top-to- 86 north, top-to-northwest, or top-to-northeast sense of shear as it does in the western part of the 87 massif. In the Mahya and Yavuzdere complexes, we could not find unequivocal evidence of 88 the presence of the earlier fabrics. Çağlayan and Yurtsever (1998) assign the Mahya and the 89 Yavuzdere complexes to the Triassic and the Jurassic, respectively and interpret them as the 90 metasedimentary cover of the Strandja Massif. Because of the absence of fossil remnants, this 91 reasoning is understandable. However, we found (Natal’in et al. 2012b and d) that U-Pb 92 zircon ages from the Mahya and Yavuzdere complexes vary from 313 to 303 Ma. 93 According to Çağlayan and Yurtsever (1998), the Mahya and Yavuzdere units occur 94 structurally higher than the Şermat Quartzites, which are interpreted as the lowest Permo- 95 Triassic stratigraphic unit of the Strandja Massif sedimentary cover. In the Kıyıköy region, the 96 Şermat Quartzite unconformably covers K-feldspar metagranites that are petrographically 97 similar to the Kırklareli metagranites (Kırklareli “Group” of Çağlayan and Yurtsever (1998)). https://mc06.manuscriptcentral.com/cjes-pubs 4 Page 5 of 66 Canadian Journal of Earth Sciences 98 They were dated as early Permian in the Kırklareli region (Aydın 1974, 1982; Okay et al. 99 2001; Natal’in et al. 2005a; Sunal et al. 2006). Our new isotopic age determinations show that 100 depositional age of the Şermat Quartzite is Ordovician and the age of metagranite that are 101 lithologically similar to the Kırklareli metagranites are between 546 – 506 Ma. 102 This short overview shows a wide range of interpretations and opinions, often contradictory, 103 on almost all aspects of the geology of the Strandja Massif. Descriptions of the geological 104 structure and analysis of new isotopic age determinations are the goals of this study.
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