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
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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
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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 ( engör 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
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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), engör 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, engör 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
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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 ermat Quartzites, which are interpreted as the lowest Permo
95 Triassic stratigraphic unit of the Strandja Massif sedimentary cover. In the Kıyıköy region, the
96 ermat Quartzite unconformably covers K feldspar metagranites that are petrographically
97 similar to the Kırklareli metagranites (Kırklareli “Group” of Çağlayan and Yurtsever (1998)).
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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 ermat 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.
105 2. Tectonic units of the St randja Massif
106 The Turkish part of the Strandja Massif consists of five tectonic units:
107 (1) The Kırklareli Unit has two fold subdivisionDraft of metamorphic rocks into the basement and
108 metasedimentary cover. Unconformable relations between early medial Paleozoic Tekedere
109 Group and Permian and Triassic Metasedimentary/Kuruköy complexes are the characteristic
110 features of this unit (Fig. 3). In the heterogeneous Paleozoic basement (Fig. 4) we established
111 late Carboniferous metagranites, preserving the earliest foliation(s), and obtain additional age
112 constraints on the emplacement of the Kırklareli metagranites (Natal’in et al. 2005a; Sunal et
113 al. 2006). The Permian – Triassic Koruköy gneisses and Triassic metasedimentary complex
114 form the massif’s cover and preserve only one S 2 foliation. The most remarkable feature of
115 these units is a thrust contact between the Permo Triassic siliciclastic rocks and Jurassic
116 carbonate rocks (Fig. 4 a and b).
117 (2) The Vize Complex is exposed in the eastern part of the Strandja Massif where it unites the
118 Neoproterozoic metasedimentary rocks, the newly recognized Cambrian metagranites, the
119 unconformably lying ermat Quartzite, and overlying schist and rare marble layers that are all
120 cut by the late Carboniferous foliated (S 2 foliation!) intrusions and dykes (Natal’in et al.
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121 2012b and d). The Cambrian metagranites had been previously and incorrectly correlated with
122 the Permian Kırklareli metagranites (Çağlayan and Yurtsever 1998; Aydın 1974, 1982; Okay
123 et al. 2001). Detrital zircon ages indicate an Ordovician depositional age of the ermat
124 Quartzite, in contrast to the previously considered Pemo Triassic age (Çağlayan and
125 Yurtsever 1998; Aydın 1974, 1982).
126 (3) and (4) The Yavuzdere and Mahya units (complexes): Following Chatalov (Chatalov
127 1988, 1991), in the Turkish segment of the Strandja Massif, Okay et al. (2001) reconstruct a
128 allochtonous Triassic metasedimentary and metavolcanic rocks. Later on, lower Paleozoic and
129 lower Mesozoic fossils were found in this complex in Bulgaria (Gerdjikov 2005). Bedi et al.
130 (2013) have accepted the idea of the allochtonous position of this tectonic unit and have 131 named it the Mahyadag Nappe. SimilarDraft to Gerdjikov (2005) they include into this unit 132 Paleozoic and Triassic rocks separated by an unconformity, but we cannot support this
133 conclusion. In our study area, this tectonic unit more or less fits the Mahya and Yavuzdere
134 complexes (Fig. 5) that were mapped by Çağlayan and Yurtsever (1998) as the Triassic
135 Mahya schist and Jurassic Yavuzdere gneiss. However, only Carboniferous U Pb zircon ages
136 can be detected in both units (Natal’in et al. 2012b and d).
137 (5) In the Kırklareli region, Natal’in et al. (2005a; 2012a) reconstructed a nappe structure
138 including dolomite, marble and limestone covering the metamorphic rocks (Fig. 4 a and b). In
139 the following, we call this unit the “Kapakli unit”. Carbonate mylonites at the base of this unit
140 quickly change into the unmetamorphosed and low strained rocks. Çağlayan and Yurtsever
141 (1998) assign dolomites and limestones to the Jurassic, while Okay et al. (2001) and Hagdorn
142 and Göncüoglu (Hagdorn and Göncüoglu 2007) consider these rocks as Triassic.
143 Unmetamorphosed low strained carbonates are also exposed in the eastern part of the Strandja
144 Massif (Çağlayan and Yurtsever 1998). If in the western part of the massif these rocks
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145 compose the highest structural levels, unmetamorphosed carbonate may tectonically underlie
146 the Mahya Complex in its eastern part.
147 2.1 The Kırklareli Unit
148 This unit consists of five lithostratigraphic complexes (Fig. 3 and 4): (1) the Paleozoic
149 metasedimentary complex, which is intruded by the late Carboniferous granite gneisses and
150 the late Paleozoic Kırklareli metagranites; (2) the late Paleozoic −Triassic Koruköy
151 metasedimentary complex; (3) the Kuzulu Complex of unknown age, and (4) the Triassic
152 metasedimentary complex (Natal'in et al. 2012; Natal’in et al. 2005a; Natal’in et al. 2012a;
153 Natal’in et al. 2012b; Natal’in et al. 2005b; Natal’in et al. 2009; Sunal et al. 2006; Sunal et al.
154 2008; Sunal et al. 2011). Draft 155 2.1.1. Basement
156 Çağlayan and Yurtsever (1998) mapped the Paleozoic metamorphic rocks as the Tekedere
157 Group while Türkecan and Yurtsever (2002) inferred a Precambrian age for them. This group
158 contains rocks of various origins including biotite gneisses, muscovite quartz schists, biotite
159 quartz epidote schists, garnet biotite schists, amphibolites, biotite hornblende gneisses and
160 orthogneisses, biotite quartz plagioclase para and orthogneisses. A few detrital zircons,
161 extracted from the metasedimentary rocks, reveal a wide variation of depositional ages
162 between late Ordovician (446 Ma), early Silurian (433 Ma), and the late Carboniferous (328
163 to 305 Ma cluster) (Natal’in et al. 2005b, 2012a; Sunal et al. 2008).
164 The late Carboniferous biotite hornblende granite gneisses, biotite muscovite granite
165 gneisses, and leucocratic granite gneisses and metagranites intrude the Tekedere Group. The
166 biotite hornblende granite gneisses contain mafic dykes, schlieren of amphibolites indicating
167 magma mingling, and xenoliths of biotite schists. The biotite hornblende and biotite
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168 muscovite granite gneisses and metagranites are cut by metamorphosed leucogranites. The
169 modal compositions of the late Carboniferous magmatic rocks correspond to tonalite, quartz
170 monzodiorite, trondhjemite, and granodiorite (Sunal et al. 2006). The 207 Pb/ 206 Pb ages (single
171 zircon stepwise evaporation method) of the late Paleozoic metaigneous rocks yielded ages
172 between 315 312 Ma (Sunal et al. 2006, Natal’in et al. 2012a).
173 2.1.2. Kırklareli metagranite
174 The Paleozoic metasedimentary complex and late Carboniferous granite gneisses and
175 metagranites are cut by the late Paleozoic porphyric K feldspar metagranites (Kırklareli
176 Complex) consisting of four plutons: the Kırklareli, Üsküp, Kula, and Ömeroba plutons (Fig.
177 3). Contrary the Tekedere Group and late Carboniferous granite gneisses these intrusions
178 reveal only one (S 2) foliation. Using theDraft Rb Sr whole rock method, Aydın (1974, 1982) dated
179 the Kırklareli pluton as 244±11 Ma. According to Okay et al. (2001), the same pluton yields a
180 single zircon stepwise evaporation age of 271±2 Ma that is similar to the zircon evaporation
181 age of the Kula (271±6) and slightly older (309±24 Ma) Üsküp pluton. Sunal et al. (2006)
182 used the same method and dated the age of augen gneisses of the Kırklareli pluton as 257±6.2
183 Ma. We applied the LA ICPMS U–Pb zircon method for dating the Üsküp and Ömeroba
184 plutons as well as a dyke cutting the Kırklareli pluton. The total duration of the Kırklareli
185 magmatism approaches 30 Ma.
186 2.1.3. Koruköy Complex
187 The Koruköy Complex is exposed to the north of the Kırklareli pluton (Fig. 3). It consists of
188 several lithostratigraphic units, showing more or less consistent and compatible lithological
189 content and structural style. In ascending order, they are metaconglomerates, quartzites,
190 schists, metasandstones, and mylonitic gneisses (Natal’in at al. 2012b). A late Triassic aplitic
191 dyke (see below) and pegmatite veins cut this complex.
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192 The Kuzulu Complex is a tectonic slice 1 km long and 0.3 km wide that is exposed in the
193 central part of the Koruköy Complex (Fig. 3 and 4). Thinly laminated microquartzites and
194 gray to reddish pelitic schists have been interpreted as metacherts and metamorphosed
195 siliceous shale (Natal’in at al. 2012a). In places, these rocks show relicts of mélange structure
196 subjected to the strong middle Jurassic early Cretaceous deformation and metamorphism. The
197 Kuzulu rock assemblage may represent the upper parts of an ophiolitic mélange (Natal’in at
198 al. 2005b, 2012a).
199 2.1.4. Triassic metasedimentary complex
200 The Triassic Metasedimentary Complex with basal metaconglomerate unconformably covers
201 the Paleozoic metasedimentary rocks and most likely also the Kırklareli metagranites
202 although in studied outcrops these rockDraft units are separated by ductile shear zones. S2 foliation
203 usually cuts lithological boundaries (Fig. 4b) and the Triassic rocks constitute a large (more
204 than 10 km) synform tectonically squeezed between the underlying Koruköy Complex and the
205 structurally overlying Jurassic Nappe (Kapaklı Unit) (Fig. 3, 4a).
206 The Triassic Metasedimentary Complex reveals a fining up succession: white quartz
207 metasandstone, metaconglomerates, metadiamictites (non genetic term used for poorly sorted
208 conglomerate with abundant matrix), lithic green metasandstones, chlorite sericite schists,
209 calc schists and calcareous metasandstones (total structural thickness is about 8 km). Calc
210 schists and calcareous metasandstones are exposed along the northern limb of the Kapaklı
211 syncline (Çağlayan & Yurtsever 1998). They do not appear along its southern limb (Natal’in
212 et al. 2005b, 2012a) where lithic green metasandstone and chlorite schists directly abate the
213 Jurassic dolomite of the Kapakli Unit across a zone of carbonate mylonites (Fig. 4a). Unlike
214 the structurally overlying Jurassic carbonates, the calc schists and calcareous metasandstone
215 reveal the same structural style as the underlying rocks. Hagdorn and Göncüoglu (2007)
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216 describe early to middle Triassic crinoids from the calcareous rock, whereas Bedi et al. (2013)
217 found early Triassic foraminifers in the same rocks.
218 2.2. The Vize Unit
219 The Vize Unit is exposed in the eastern part of the Strandja Massif (Fig 3 and 5). Similar to
220 the Kırklareli Unit it can be subdivided into the basement intruded by metagranites and
221 metasedimentary cover. However, stratigraphic ages of these two units are very different.
222 2.2.1. Basement
223 Çağlayan and Yurtsever (1998) mapped the basement of this unit as the Tekedere Group.
224 However, in the Vize Unit, composition the Tekedere Group is different from that in the 225 Kırklareli region. Rocks consist of greenishDraft grey and green quartz chlorite muscovite and 226 quartz chlorite biotite muscovite schist, metasandstones, and rare paragneisses.
227 Metasandstones contain 60 70% of sorted quartz and feldspar grains. Alternation of schists
228 and metasandstones indicate a thinly to medium bedded protolith with parallel lithological
229 boundaries that are characteristic for marine rocks. Thick bodies of quartz feldspathic
230 gneisses, amphibolite, granite gneisses and migmatite, which are common to the Tekedere
231 Group in the Kırklareli region, are absent in the Vize Unit. In places, along with penetrative
232 S2 foliation these schists preserve relicts of an older foliation that indicates a deformation
233 event missing in younger rocks of the unit.
234 2.2.2. Neoproterozoic – early Cambrian metagranites
235 The basement of the Vize Unit is cut by metagranites that are petrographically similar to the
236 late Paleozoic Kırklareli Complex. Çağlayan and Yurtsever (1998) mapped them as the
237 Kazandere, Vize, Ayvacık, Bahçeköy, Lala, and Aksicim plutons (Fig. 5). Together with later
238 researches (Okay et al. 2001; Gerdjikov 2005; Natal'in et al. 2005a, 2012a; Okay et al. 2006;
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239 Hagdorn and Göncüoglu 2007; Sunal et al. 2008; Elmas et al. 2011) they consider these
240 granites as a part of a single Permian plutonic belt. Nevertheless, our studies reveal latest
241 Neoproterozoic to early Cambrian zircon ages of the intrusions located in the Vize Unit. We
242 define them as the Kazandere Complex.
243 Similar to the Kırklareli Complex, the Kazandere metagranites are typical porphyritic
244 granites, containing large (up to 5 cm) phenocryst of pink K feldspar embodied into quartz,
245 albite oligoclase, biotite, and muscovite matrix. Original dark minerals are represented by
246 brown biotite that is replaced by green biotite, white mica, and chlorite. Similar to the late
247 Paleozoic Kırklareli metagranite, the granitoids of the Kazandere Complex is metamorphosed
248 in greenschist to low amphibolite facies. K feldspars show dynamic recrystallization and 249 sometimes form perfect augens. TogetherDraft with microcline twinning and perthitic lamellae, 250 they suggest rock recrystallization at a temperature around 500° (Passchier and Trouw 2005;
251 Vernon, 2004). The contacts between the metagranite and country rocks show the absence of
252 contact metamorphism though. They usually coincide with thin ductile shear zones
253 emphasized by grain size reduction in metagranites.
254 2.2.3. “Koruköy” and Evciler gneisses
255 To the east of Sergen (Fig. 5), along the southern margin of the Mahya Complex, a belt of
256 muscovite biotite paragneisses with a blastomylonitic fabric is exposed to the north of the
257 Neoproterozoic early Cambrian metagranites. Çağlayan and Yurtsever (1998) mapped these
258 rocks as the Paleozoic Koruköy Gneiss. There is another lithostratigraphic unit, which has the
259 same name in the Kırklareli Unit. Indeed, a certain lithological similarity between rocks of
260 these two units exists. However, structural and stratigraphic relations with surrounding rocks
261 are different. In the Vize Unit, the “Koruköy” gneisses spatially associate with the Evciler
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262 Gneiss (Çağlayan and Yurtsever, 1998), which reveal transitions to the “Koruköy” gneisses.
263 Contrary to the Kırklareli region, both units contain no relicts of igneous texture.
264 The Evciler metaclastic rocks form a lens (2.3×0.4 km) mainly made of clasts (up to 40 cm)
265 of the Kazandere metagranites, yielding U Pb zircon ages of 508 and 533 Ma (see below). In
266 addition to metagranites, metaconglomerates contain clasts of quartzite, well foliated
267 gneisses, quartz schists, and milky quartz. Pebbles and boulders preserve their own foliations
268 that have different orientation comparing with S 2 foliation in the matrix.
269 In the Triassic metasedimentary complex of the Kırklareli Unit, clasts of the Permian
270 Kırklareli metagranite are absent and, therefore, clasts of the Evciler gneisses should come
271 from very different source areas. This aspect implies a former separation of the Kırklareli and
272 Vize units until Mesozoic times. OrientationDraft of the main S2foliation in the “Koruköy” and
273 Evciler units and its kinematic history is similar to the whole of the Strandja Massif.
274 Therefore, variously orientated foliations in the Evciler pebbles must have been formed before
275 the Ordovician (see below). We claim that it is related to a Cambrian orogeny.
276 2.2.4. Ordovician to Upper Carboniferous metasediments
277 The ermat Quartzite is the most characteristic lithostratigraphic unit in the eastern part of the
278 Strandja Massif. Its thickness (150 250 m), competence, and composition of rocks allow to
279 use them as a marker horizon. Çağlayan and Yurtsever (1998) have assigned these rocks to
280 the Permo Triassic, and have interpreted them as a lower part of the metasedimentary cover of
281 the Strandja Massif. They have divided this part of the section into three lithostratigraphic
282 units (in ascending order): 1) the Kocabayır metasandstone, shale, and metaconglomerate, 2)
283 the ermat Quartzite, and 3) Rampana Quartz Schist.
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284 Because of numerous ductile faults, the Kocabayır metasandstone (Çağlayan and Yurtsever,
285 1998) reveal an uncertain stratigraphic position occurring structurally lower and higher the
286 ermat Quartzite. Therefore, we are not certain about the validity of this unit. The best
287 stratigraphic relationships between the Neoproterozoic – Cambrian metagranites and the
288 ermat Quartzite are observed 1.5 km south of Kızılağaç (Fig. 5) where the Kocabayır unit is
289 missing. Despite the S 2 foliation, the fine to medium grained quartzites preserve their
290 bedding and, in places, cross stratification showing a source location in SSW (Yazıcı and
291 Natal’in, 2015). Parallelism of thin to medium bedding planes suggests marine but not fluvial
292 origin of rocks. Matrix supported quartz clasts (thee is no granitic pebbles!) in the basal
293 conglomerate are well rounded, but they are poorly sorted (Fig. 6b). Their shape suggests a 294 long distance transportation by high energyDraft flow. 295 South of Kızılağaç, the quartz and quartz muscovite chlorite Rampana schists overlie the
296 ermat Quartzites. The contact is transitional. The same schists with quartzite interbeds are
297 exposed in other regions, and in many places, they are structurally higher than the ermat
298 Quartzite as it is clearly seen in outcrops to the SE of Kıyıköy (Fig. 5). Quartz schists may
299 also occur structurally below the ermat Quartzites because of tectonic repetitions along
300 ductile shear zones. In the Rampana schists, we observed relicts of graded bedding and
301 convolute folds. These structures suggest a turbiditic nature of the rocks and in this case, the
302 lens shape quartzite bodies can be interpreted as distributary channels. Thus, we infer that the
303 Rampana basin became deeper comparing with the ermat basin.
304 Thin alternation of calcite marble and metacherts is exposed 3.5 km southwest of Kıyıköy
305 (Fig. 6c). These rocks form a tectonic lens of 100 m thickness and more than 700 m length,
306 which is embodied in quartz muscovite chlorite Rampana schist (Fig. 7). A smaller marble
307 and metachert lenses are exposed in the nearby regions. Alternation of marbles and
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308 metacherts indicates pelagic origin of primary rocks, which allow us to infer the further
309 deepening of the Rampana basin.
310 Detrital zircons extracted from the ermat Quartzite yield the youngest concordant ICP MS
311 ages of 478±6 and 484±6. Both quartz muscovite chlorite schists and marbles are cut by
312 metagranite, yielding 311.3 ± 3.1 Ma. Quartz feldspathic dykes cutting Rampana quartz
313 schists and quartzites yield a similar ~313 Ma ICP MS zircon age (Natal’in et al. 2012b).
314 2.3. Mahya Complex
315 This unit (Fig. 5) is defined as the Triassic Mahya Schist by Çağlayan and Yurtsever (1998)
316 or as Mahya Group by Okay and Yurtsever (2006), who consider them as a part of the 317 Triassic metasedimentary cover of theDraft Strandja Massif. This complex is structurally higher 318 than the Vize Unit as it is evident in the Kızılağac region (Fig. 8). Further to the east, the Vise
319 Unit’s structural position with respect to the Mahya Complex may vary because of thrusting.
320 The Mahya Complex consists of mainly greenschists. Mineral assemblages are made of
321 quartz, albite oligoclase, muscovite, chlorite, and epidote. Rare, tectonic lenses of thinly
322 bedded microquartzites are present (Fig. 6d). Contrary to the ermat Quartzite, these rocks are
323 fine grained and laminated. The color is gray, light gray or reddish. In thin sections, quartz
324 reveals strong dynamic recrystallization and original fabric cannot be recognized. We
325 interpret microquartzites as metachert. Lenses of calcite marbles are also present in the Mahya
326 Complex. Sometimes, microquartzite and marble resemble mélange inclusion.
327 Green to olive green, massive mafic metavolcanics with relicts of doleritic texture represent
328 another key lithology of the Mahya Complex. They consist of actinolite, chlorite, and epidote,
329 quartz, and albite oligoclase. In places, greenschist, metavolcanics, microquartzites, and
330 marbles form alternation, in which packages of individual lithologies are rather thin (10 20 m)
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331 but the strong S 2 foliation implies strong flattening and obliteration of original structural
332 relationships. Nevertheless, the juxtaposition of rocks of different depositional setting
333 suggests a tectonic mixing that is typical for accretionary prisms. The abundance of quartz
334 veins supports this conclusion. The most interesting veins are folded veins that reveal the S2
335 foliation. These veins were formed before the middle Jurassic early Cretaceous deformation
336 and we infer that they were formed during the late Paleozoic deformation. High fluid activity
337 is characteristic for deformation of poorly lithified sediment and thus fits the reconstruction
338 subduction accretion settings (Kusky and Bradley 1999; Moore 1989).
339 To the north of Kı lacık (Fig. 5), we found metapyroxenite and metagabbro. Metagabbro
340 consists of brown euhedral hornblende (~ 70%), which is replaced by light green to bluish 341 actinolite. Relicts of pyroxene are alsoDraft present and they are replaced by hornblende and 342 actinolite. Metapyroxenites are made of similar mafic minerals but contain less amount of
343 altered plagioclase. Metapyroxenite reveals a weak compositional layering that is oblique to
344 S2 foliation. Mafic and ultramafic rocks are associated with greenschists. Euhedral hornblende
345 replacing pyroxene is characteristic for ocean floor metamorphism (cf., Miyashiro, 1972).
346 2.4. Yavuzdere Complex
347 Çağlayan and Yurtsever (1998) mapped this unit as the Yavuzdere hornblende biotite gneiss
348 (Jsy), hornblende porphyry or diorite porphyry (Jsh), and quartz porphyry (Jsp) and,
349 considering structural relation with the Mahya Complex (e.g. Fig. 5), infer a Jurassic age of
350 these rock. Despite of our disagreement on the age determination (see bellow) we believe that
351 the discovery of these magmatic rocks is the very important step in understanding geology of
352 the Strandja Massif.
353 The Yavuzdere Complex consists of mainly magmatic rocks with minor amount of marbles,
354 quartzites (microquartzite/metachert), and chlorite schists (Fig. 9). Gray to light gray medium
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355 grained granite gneisses and metagranites form large elongated bodies and have structural
356 thicknesses between 100 and 1000 m. They consist of quartz, plagioclase, K feldspar,
357 muscovite, brown and green biotite, chlorite, and epidote. Biotites are replaced by muscovites
358 and chlorites. Relicts of the phaneritic texture together with the uniform composition of rocks
359 indicate the magmatic origin. Relations between granite gneisses, country rocks, and the S 2
360 foliation support this conclusion (Fig. 10a). Quartz feldspathic gneisses often associate with
361 the granite gneisses. They are interpreted as metamorphosed leucogranite.
362 Metavolcanic and sedimentary rocks constitute the main volume of the Yavuzdere Complex.
363 Their relationships can be illustrated by a section made along the Yavuz Dere River (Fig. 9).
364 Mafic volcanic rocks, metagabbros, and amphibolites are exposed structurally higher than the 365 granite gneisses. They are dark greenDraft medium grained, massive metamorphic rocks, 366 containing euhedral relicts of altered mafic plagioclase, quartz, hornblende and actinolite,
367 chlorite, epidote, and ore minerals. These rocks are structurally overlain by alternation of
368 green quartz chlorite schist and thin (2 5 cm) laminated fine grained microquartzites, which
369 are interpreted as metacherts.
370 Metatuffs appear at the highest structural position. These rocks are similar to metavolcanics in
371 mineral composition but have darker, greenish gray or olive green color because of higher
372 content of chlorite and epidote. Texture of these rocks is porphyritic, because of the presence
373 of porphyroclasts of plagioclase, amphibole, and volcanic rocks (Fig. 10b). Compositional
374 layering indicates the volcano sedimentary origin of protolith.
375 Biotite schists in the Yavuz Dere section are dark gray, medium grained rocks containing
376 interbeds (2 7 cm) of metasandstones. In places, the alternation of these lithologies is
377 rhythmic, suggesting the turbiditic nature of protolith. This inference is supported by findings
378 of quartzite blocks (debris flow deposits) with their internal deformations of bedding.
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379 In this study, we obtained late Carboniferous age (Kasimovian Gzhelian stages of the Late
380 Carboniferous) for metatuff and metagranites and associated granite gneisses of the Yavuz
381 Dere section.
382 2.5. Jurassic Nappe or the Kapaklı Unit
383 A thick pile of dolomite and limestone/marble (Dolapdere Formation) constitute the core of a
384 large and well developed Kapaklı syncline (Fig. 4). Based on a single crinoid fossil finding
385 Çağlayan and Yurtsever (1998) assigned the Dolapdere Formation to the Jurassic, while Okay
386 et al. (2001) preferred its Triassic age, accounting for a poor preservation of crinoids and
387 long distance correlation with lithologically similar rocks in Bulgaria. Natal’in at al. (2005b,
388 2012b) have inferred that the Dolapdere Formation of the syncline constitute a nappe,
389 covering the Koruköy and Triassic metasedimentaryDraft complexes (Fig. 4). This nappe is
390 marked by carbonate mylonites, which can also be found in the same structural position in
391 other places of the Kırklareli region. Besides the mylonite presence, Fig. 4a shows a structural
392 misfit below and above the nappe. Where the mylonites are absent, the contacts between
393 carbonate rocks and metaclastics are defined by later high angle brittle faults.
394 Recently, Bedi et al. (2013) have reported a number of Triassic and Jurassic fossil findings
395 near the problematic contact. Unfortunately, structures and strain of rocks were not fully
396 accounted for in their study. Because of that and contrary to the previous researches (Aydın,
397 1974, 1982; Çağlayan and Yurtsever 1998; Okay et al. 2001; Okay and Yurtsever 2006;
398 Natal’in et al. 2005b, 2012a), they have assigned stratigraphic units of the same lithological
399 composition both to the Triassic and the Jurassic as if these rocks belonged to different
400 lithostratigraphic units. Moreover, Bedi et al. (2013) claim that the Lower Jurassic
401 unmetamorphosed rocks, including the Bathonian – Kimmeridgian Balaban Formation of
402 black slate, schists and phyllites (Çağlayan and Yurtsever 1998), unconformably cover the
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403 Triassic units and older metamorphosed stratigraphic units. This conclusion may not be
404 correct because in the Kırklareli region Ar Ar ages of the S 2 foliation vary from 165 to 157
405 Ma (Natal’in et al . 2005a) and Rb Sr whole rock and mica ages vary from 162 to 141 Ma
406 (Sunal et al. 2011). In the eastern part of the massif, this foliation yields biotite and muscovite
407 Ar Ar ages between 156.5 and 143.2 Ma (Elmas et al. 2011).
408 In the Kapallı syncline (Fig. 4), carbonate mylonite of various thickness (Fig. 10c) are
409 developed between underlying siliciclastic metamorphic rocks and the overlying non foliated
410 fractured dolomite (Fig. 10d). Near the western closure of the Kapallı syncline and
411 structurally below the Dolapdere carbonates, calc schists (Ta tepe Member, Çağlayan and
412 Yurtsever 1998) contain early middle Triassic crinoids (Hagdorn and Göncüoğlu 2007) and 413 foraminifers (Bedi et al. 2012). SinemurianDraft – Pliensbachian foraminifers were found above 414 the mylonites in dolomitic limestones (Bedi et al. 2013), which we previously mapped it as
415 the Kapakli Member of the Jurassic Dolaprere Formation (Çağlayan and Yurtsever 1998).
416 Resent fossil findings Bedi et al. (2013) and our personal observations show that non foliated
417 dolomite of the Lower Jurassic Dolapdere Formation are tectonically mixed with the foliated
418 metamorphic rocks of the Middle Upper Jurassic Balaban Formation. This mixing occurs in
419 the northern limb of the Kapaklı syncline, where we expect to see the uppermost nappe in the
420 Strandja Massif. There, the tectonic lenses of the Balaban Formations are squeezed between
421 apparently unmetamorphosed rocks of the Dolapdere Formation (Fig. 4) and 4.6 km
422 southwest of Kula, the Triassic chlorite sericite schists thrust onto the carbonate mylonite
423 underlying by non metamorphosed fractured dolomite of the Kapaklı Member of the
424 Dolapdere Formation (Fig. 4A). Near the Kula village, these dolomites are tectonically
425 overlain by the carbonate mylonite showing upward increase of the S2 foliating intensity (Fig.
426 11). The Balaban Formation, which is wide spread in this region, occupies the highest
427 structural position and reveals the well developed S2 foliation. Bedi et al. (2012) report from
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428 this region several findings of the medial to late Jurassic radiolarians. Higher dolomite
429 competence (e.g. Passchier and Trouw 2005) may explain the preservations of the non foliated
430 Dolapdere dolomites structurally lower the Balaban schists and phyllites .
431 Only a few isolated bodies of the Dolapdere Formation were mapped in the Kıyıköy region
432 (Çağlayan and Yurtsever 1998), where the dolomites are exposed structurally below the
433 Mahya Complex (Fig. 5). Within the thrust sheets, non foliated fractured dolomites tend to be
434 at lowest structural levels being overlain by marbles and marble/schists alternations, which
435 show the well developed to mylonitic S 2 foliation (Fig. 12).
436 3. Sampling and analytical technique
437 Zircons were extracted from 5 to 10 kgDraft of rock samples by using standard mineral separation 438 techniques, mainly grinding, sieving, Frantz isodynamic separator and heavy liquids.
439 Separated zircons were handpicked under a binocular microscope, and then a fraction with
440 grain sizes of 63–200 m was selected and sorted according to their crystal properties (i.e.
441 euhedral morphology, lack of overgrowth and visible inclusions). Zircons were mounted in
442 epoxy resin and polished down to expose grain interiors for cathodoluminescence (CL) image
443 technique prior to U–Pb isotopic analyses.
444 3.1. ICP MS dating
445 Some of the zircons (unless indicated) were dated at the State Key Laboratory for Mineral
446 Deposits Research, NJU (Nanjing University, China), using an Agilent 7500a ICP MS
447 attached to a New Wave 213 nm laser ablation system with an in house sample cell. Detailed
448 analytical procedures are similar to those described by Griffin et al. (2004) and Wang et al.
449 (2007). The U–Pb fractionation was corrected using zircon standard GEMOC GJ 1
450 (207 Pb/ 206 Pb age of 608.5 ± 1.5 Ma) (Jackson et al. 2004) and accuracy was controlled using
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451 zircon standards Mud Tank (intercept age of 732 ± 5 Ma) (Black and Gulson 1978). Most
452 analyses were carried out using a beam with a 20 m diameter and a repetition rate of 5 Hz.
453 U–Pb ages were calculated from the raw signal data using the online software package
454 GLITTER (ver. 4.4) (http://www.mq. edu.au/GEMOC). Because 204 Pb could not be measured
455 due to low signal and interference from 204 Hg in the gas supply, common lead correction was
456 carried out using the EXCEL program ComPb Corr#3_15G (Andersen 2002). The spots of
457 the age concordance lower than 85% are deleted due to inadequate precision. All of the U–
458 Th–Pb age calculations and plotting of concordia diagrams were made using the
459 ISOPLOT/Ex program (ver. 2.49) (Ludwig 2001). The concordance values were calculated
460 from 100×( 206 Pb/ 238 U age)/( 207 Pb/ 235 U age))
461 3.2. SHRIMP dating Draft
462 Some zircons (where indicated) were dated on the SHRIMP II ion microprobe at the Beijing
463 SHRIMP Centre, Institute of Geology, Chinese Academy of Geological Sciences. The
464 analytical procedures were similar to those described by Williams (1998). Mass resolution
465 during the analytical sessions was ~5000 (1% definition), and the intensity of the primary ion
466 beam was 5–8 nA. Primary beam size was 25–30 m, and each site was rastered for 120–200
467 s prior to analysis. Five scans through the mass stations were made for each age
468 determination. U abundance was calibrated using the standard SL13 (U=238 ppm, Williams
469 1998) and 206 Pb/ 238 U was calibrated using the standard TEMORA ( 206 Pb/ 238 U age=417 Ma;
470 Black et al. 2003). The decay constants used for age calculation are those recommended by
471 the Subcommission on Geochronology of IUGS (Steiger and Jäger 1977). Measured 204 Pb
472 was applied for the common lead correction, and data processing was carried out using the
473 Squid and Isoplot programs (Ludwig 2001). The uncertainties for individual analyses are
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474 quoted at the 1 sigma confidence level, whereas errors for weighted mean ages are quoted at
475 95% confidence.
476 4. Results
477 A summary of the dating study is given in Table 1. The results will be given according
478 to the age intervals obtained. If there is no indication next to the ages, it means that it is LA
479 ICPMS U Pb zircon age, otherwise it is SHRIMP (supplementary data Tables S1 and S2,
480 respectively). The program Isoplot 3.0 (Ludvig 2001) was used for all age calculations and
481 Concordia diagram productions.
482 4.1. Neoproterozoic – early Cambrian metagranites 483 Neoproterozoic – early CambrianDraft granitoids (the Kazandere Complex) of the Vise Unit 484 are represented by the Vize, Kazander and Lala plutons (see Fig. 5). Accounting for the
485 composition of country rocks, we tentatively assign the Ayvacık, Bahçeköy, Aksicim and
486 Evciler intrusions to the same magmatic event (Fig. 5).
487 4.1.1. The Kazandere Pluton
488 Two samples were collected from the Kazandere pluton, which is located in the Kıyıköy
489 region to the north of the Vize town (Fig. 5). Sample KI 252 (Table 1) was collected from
490 biotite bearing coarse grained K feldspar metagranites. Zircons are euhedral and prismatic.
491 CL images are not perfect, because some zircons are very dark but others show oscillatory
492 zoning supplementary data Fig. S3 ). Metamorphic overgrowth is not visible; inherited cores
493 can be recognized in some grains. Intercept age yielded 542.6 ± 3.5 Ma (Fig. 13a). The
494 second sample (sample KI 227) has also been collected from K feldspar metagranites in a
495 nearby location (Fig. 5). Zircons are idiomorphic and transparent. CL images of the zircons
496 show generally moderate intensity (tones of gray) with oscillatory zoning. Sector zoning is
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497 also present in some grains. Mineral inclusions are represented by dark spots in CL images
498 (supplementary data Fig. S4). Dating study performed on outer rims of the zircons and 535.8
499 ± 4.2 Ma SHRIMP age was obtained from this sample (Fig. 13b).
500 4.1.2. The Lala Pluton
501 We have only one sample from the Lala pluton (KI 225) (Table 1, Fig. 5), which intrude
502 metasedimentary rocks. However, the nature of the exposed northern contact remains unclear
503 because of the superimposed S 2 foliation. Collected sample represents coarse grained
504 muscovite biotite metagranite, where the muscovite is the secondary mineral. Zircons of the
505 sample are idiomorphic and transparent (supplementary data Fig. S5 ). CL images of the
506 zircons show generally dark inner parts that are most probably because of high U amount.
507 Rims of the zircons have high CL intensity.Draft Contrary to the Kazandere pluton inherited cores
508 are visible in some of the zircons. We dated outer rims of the zircons and a 546.4 ± 4.7 Ma
509 SHRIMP U Pb age obtained from this sample (Fig. 13c).
510 4.1.3. The Vize Pluton
511 The sample KI 247 (Table 1) has been collected from the Vize pluton (Fig. 5), from
512 biotite bearing coarse grained K feldspar metagranites that make a transition to augen
513 gneisses. Zircons are euhedral and prismatic. CL images show clear oscillatory zoning and the
514 absence of the metamorphic overgrowth (supplementary data Fig. S6 ). Concordant ages of
515 zircon rims cluster around 506.1 ± 4.5 Ma (Fig. 13d).
516 4.1.4. Pebbles from the Evciler metaconglomerate
517 Two samples were collected from pebbles of porphyritic K feldspar metagranite
518 occurring in the Evciler metaconglomerate (Fig. 5). Extracted zircons from the sample KI
519 255.1 (Table 1) are euhedral and prismatic. CL images reveal clear oscillatory zoning and the
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520 absence of the metamorphic overgrowth (supplementary data Fig. S7 ). Grains have different
521 CL intensity. Some of them are dark in CL image, whereas some have bright color. Only
522 eleven spots were analyzed for this sample. All of them (except spot 1) are concordant and
523 yields an age of 507.9 ± 5.8 Ma (Fig. 13e). Similar to the KI 255.1, the sample KI 252.2
524 (Table 1) is coarse grained muscovite biotite metagranite. Muscovite is the secondary
525 mineral. It has euhedral and prismatic zircons (supplementary data Fig. S8 ). Data of 13 spots
526 gave 533.1 ± 6.1 Ma interception age for this K feldspar rich granite gneiss pebble (Fig.13f).
527 4.2. Detrital zircons of the ermat Quartzites 528 In the Vize Unit, unconformity laying on the granitic basement the thick ermat
529 Quartzite and the overlying Rampana schists was assigned to the Permo Triassic (e.g. 530 Çağlayan and Yurtsever 1998; Okay andDraft Yurtsever 2006). However, we obtained late 531 Carboniferous U Pb zircon ages (sample 263 and 265, see below) from intrusions cutting the
532 Rampana schists. Thus, the determination of the depositional age of the ermat Quartzite
533 becomes crucial for understating of the Strandja Massif geology. Sample KI 246 (Table 1)
534 have been collected from the ermat Quartzites exposed 2.5 km south of Kızılağaç (Fig. 5).
535 We dated 57 zircons of totally 73 extracted grains. CL images of zircons reveal a variety
536 of internal structures, indicating multiple episodes of formation (supplementary data Fig. S9 ).
537 Some grains are euhedral and prismatic, others are slightly rounded or rounded. Many grains
538 show thin oscillatory zoning and internal rounded cores. All dated zircon grains have high
539 Th/U ratio (>0.4) and thus they are magmatic in origin. Almost all age determinations are
540 concordant (Fig.14). The main age cluster occurs between 479 660 Ma. Older zircons are
541 rare. One of them yields an 206 Pb/ 238 U age of 1349±16 Ma. Two others are about 1770 Ma old
542 and four grains fill the interval between 1970 and 2049 Ma. The lower limit of the
543 depositional age of the ermat Quartzite can be constrained by a grain yielding 478 Ma
544 206 Pb/ 238 U age (early Ordovician).
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545 4.3. Carboniferous metagranite, granite gneisses and metatuffs 546 Eight ages were obtained from the Carboniferous metagranites and granite gneisses
547 (Table 1). Two of them belong to the Üsküp pluton (Fig. 3) and were designed to date
548 Kırklareli metagranites of the Kırklareli tectonic unit. In the same tectonic unit, we collected a
549 sample of rocks with relicts of magmatic fabric from the Koruköy gneisses (Fig. 3). Three
550 samples were dated in order determine the age of the Yavuzdere Complex (Fig. 5 and 9). One
551 granite gneiss transitional to metagranite and foliated dyke from the Vize Unite (Fig. 5) were
552 dated to constrain the age of the Rampana schists stratigraphically overlying the Ordovician
553 the ermat Quartzites.
554 Samples KI 239.1 and KI 242 (Table 1) were collected from the Üsküp pluton (Fig. 3).
555 Sample KI 239.1 is represented by light gray to white medium to coarse grained augen
556 gneisses consisting of quartz, orthoclase,Draft altered plagioclase, white mica, and chlorite. Zircons
557 are euhedral and prismatic. CL images show perfect oscillatory zoning and do not reveal
558 metamorphic overgrowth (supplementary data Fig. S10). Some zircons contain inherited
559 cores. All of them have high (> 0.4) Th/U ratios indicating magmatic origin. 35 spots have
560 been used for the age determination. Three concordant ages of inherited cores yielded ages
561 around 530, 540, and 620 Ma (supplementary data Table S1). Concordant ages of rims cluster
562 around 299.1 ± 2.7 Ma, which is interpreted as the magmatic age of the intrusion (Fig. 15a).
563 Sample KI 242 was taken from similar rocks as KI 239.1, but in this sample, relicts of
564 brown biotites are preserved. Zircons are euhedral and prismatic. CL images show perfect
565 oscillatory zoning and do not reveal metamorphic overgrowth (supplementary data Fig. S11).
566 Contrary to the sample KI 239.1, many zircons contain inherited cores. Twenty one spots
567 were dated and 300.6 ± 2.8 Ma obtained from the lower intercept (Fig. 15b). All selected
568 zircon grains have high (>0.4) Th/U ratios and thus are magmatic in origin. Ages of the
569 inherited core are highly discordant (supplementary data Table S1), but two of them, yielding
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570 the ages of approximately 1800 Ma, can be used for further considerations. In the U Pb
571 isotopic system of zircon, 235 U is of minor abundance and therefore less 207 Pb is produced in
572 young zircon (Hiess et al. 2012). Because of that, the 207 Pb/ 235 U and 207 Pb/ 206 Pb ages have
573 lower precision than 206 Pb/ 238 U ages. Therefore, 206 Pb/ 238 U ages are better, especially for
574 young (>1000 Ma) zircon. However, for discordant zircons, the 206 Pb/ 238 U age commonly
575 underestimates the actual age due to Pb loss, while 207 Pb/ 206 Pb age is closer to the primary
576 crystallization age (Ma et al., 2012). 207 Pb/ 206Pb ages of old zircon in Sample KI 242 are
577 1987±26 Ma and 2060±20 Ma (supplementary data Table S1).
578 Shear zones bound the sample KI 235 (Table 1) collected from the Koruköy Gneisses of
579 the Kırklareli Unit (Fig. 3). This sample represents a rather mafic rock with relicts of 580 magmatic fabric containing biotite, amphiboleDraft and minor plagioclase. Zircons of the sample 581 are idiomorphic and have an aspect ratio between 1:2 and 1:3. Twenty spots have significant
582 differences in ages (supplementary data Fig. S15). Inherited ages are enclosed in three groups;
583 (a) ages around 600 Ma, (b) ages between 500 and 550 Ma, and (c) a ~344 Ma age
584 (supplementary data Table S1). The younger age group of ~304 Ma is defined as the age of
585 the intrusion. The intercept age calculated is 304.9 ±7.9 Ma (Fig. 16).
586 The samples 255, 260, and 257 (Table 1) were collected from the Yavuzdere Complex
587 (Fig. 5 and 9). The sample 255 is medium grained muscovite biotite metagranite, which have
588 transitional contacts with surrounding granite genies (Fig. 8). All zircons are idiomorphic.
589 Aspect ratio of the grains is between 1:1.5 and 1:2. CL images reveal mainly oscillatory
590 magmatic zoning, but sometimes sector zoning (supplementary data Fig. S12). Inheritance is
591 rarely observed. Twenty one spots have been dated from this sample (supplementary data
592 Table S2). The highly discordant four ages were excluded from the calculation. The mean age
593 calculated from the rest of the 17 spots is 303.6 ±2.5 Ma (SHRIMP, Fig. 17a).
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594 The sample 260 is a metagranodiorite containing hornblende, biotite, plagioclase and
595 minor quartz, apatite and opaque minerals (Fig. 5). Zircons of the sample are idiomorphic but
596 partly rounded. Aspect ratio of them ranges from 1:1.5 to 1:1. Oscillatory and sector zoning
597 represents internal structures of zircons grains, which have by very thin and bright outer rims
598 formed because of metamorphic resorption (supplementary data Fig. S13). We used 21 spots
599 for zircon dating (supplementary data Table S2). Twelve age determinations have different
600 degrees of discordance and anomalously high content of Th and Pb; so, these spots are
601 rejected (supplementary data Table S2). Nine coherent age determinations were used for the
602 mean age calculation, which is 302.7 ±3.3 Ma (SHRIMP, Fig. 17b).
603 The sample 257 is a metatuff sample (Fig. 9). All of the extracted zircons are 604 idiomorphic (supplementary data TableSDraft 1). They reveal the oscillatory zoning and do not 605 contain inherited cores (supplementary data Fig. S14 ). They have aspect ratio between 1:2
606 and 1:3. Nineteen spots have been dated (supplementary data Table S2). We used all
607 238 U/ 206 Pb ages for the mean age calculation and obtained 305.9 ±2.5 Ma is obtained
608 (SHRIMP, Fig. 16c).
609 The sample 263 (Kaletepe pluton, Table 1) represents a biotite bearing granite gneiss of
610 the Kaletepe intrusion cutting the Rampana schists of the Vize Unit (Fig. 5). Zircons of the
611 sample are idiomorphic and have oscillatory zoning (supplementary data Fig. S16). The
612 aspect ratio of zircon crystals changes between 1:2 and 1:2.5. In this sample, 19 zircons (19
613 spots) have been dated (supplementary data Table S2). Five ages were excluded from the
614 calculation because of inconsistencies of isotope ratios. The rest allows a mean age
615 calculation that is 311.3 ±3.1 Ma (Fig. 18a). The sample 265 (Table 1) was collected from a
616 dyke like muscovite chlorite granite gneiss cutting the Rampana schists (Fig. 5). Zircons of
617 this sample are idiomorphic. Their internal structure reveals oscillatory zoning typical for
618 magmatic rocks. Their aspect ratio ranges from 1:2 to 1:3 (supplementary data Fig. S17).
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619 Nineteen spots were dated but two of them were rejected from the calculations. The main age
620 calculated from 17 spots is 311.3 ±3.1 Ma (SHRIMP, Fig. 18b).
621 4.4. Permo Triassic metagranite and dykes 622 In this study, we obtain three latest Permian – Triassic ages of rocks constituting the
623 Kırklareli Unit, for which a passive continental margin development was suggested in early
624 Mesozoic times (Hagdorn and Göncüoglu 2007; Okay et al. 1996, 2001, 2006). One sample
625 (KI 233.3) was collected from the Ömeroba pluton (Fig. 3; Table 1 ). It is a weakly foliated
626 porphyritic metagranite containing quartz, K feldspar, plagioclase, minor biotite and
627 secondary muscovite. CL images show oscillatory zoning and do not reveal metamorphic
628 overgrowth (supplementary data Fig. S18). Some zircons contain inherited cores, but ages of 629 the core in spot 5 are similar to the agesDraft determined from the rims of other zircons. Similar to 630 the previous samples, all selected zircon grains have high (>0.4) Th/U ratios and thus they are
631 magmatic in origin (supplementary data Table S1). We used 13 spots for dating and age of the
632 Ömeroba pluton was determined to be 251.8 ± 3.4 Ma (Fig. 19a).
633 The sample KI 231 (Table 1) was collected from a leucogranitic dyke cutting the
634 Kırklareli metagranite. The dyke consists of quartz, K feldspar, plagioclase, small amount
635 (<5%) of brown biotite and ore minerals. CL images of the selected zircons (supplementary
636 data Fig. S19) show oscillatory zoning and inherited cores. Similar to the previous samples,
637 all selected zircon grains have high (>0.4) Th/U ratios and thus they are magmatic in origin
638 (supplementary data Table S1). We used 18 spots for dating, from which we determine the
639 magmatic age of the dyke as 243.8 ±5.8 Ma (Fig. 19b).
640 Sample KI 237 represents an aplitic dyke cutting the metaconglomerate of the Koruköy
641 Complex (Table 1; Fig. 3). Similar to the metaconglomerate, the dyke is affected by the
642 middle Jurassic early Cretaceous deformation and metamorphism. Zircons of the sample KI
643 237 are euhedral and prismatic. CL images are very dark and therefore oscillatory zoning
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644 cannot be recognized (supplementary data Fig. S20). The low CL intensity is generally
645 attributed to the high U content of the zircons (Poller et al. 2001). Ages belonging to 18 out of
646 25 spots are concordant (supplementary data Table S1). Two groups of zircon ages were
647 observed (Fig. 19c and d). The first one was around 283 Ma which is a close to the age of the
648 Kırklareli Complex and the second was Triassic. Eleven magmatic grains have intercept age
649 of 213.1 ± 4.1 Ma.
650 5. Discussion
651 Structural studies and new ICP MS and SHRIMP U Pb zircon age determinations
652 allowed us significantly revise available ideas on geology of the Strandja Massif.
653 As we found out, the oldest rocks in the region are Neoproterozoic and Cambrian but in 654 the past, they had been assigned to theDraft Paleozoic or even to the Permian (Çağlayan and 655 Yurtsever 1998; Okay et al. 2001). Widespread K feldspar metagranites are all considered to
656 be a product of a single magmatic event that happened during the early Permian and formed a
657 plutonic belt along the southwestern boundary of the Strandja Massif (e.g. Okay et al. 2001).
658 In this study, we obtained four U Pb zircon ages from the Kazander (SRIMP age of 535.8±4.2
659 Ma and less precise LA ICPMS age of 542.6±3.5 Ma), Lala (546.4±4.7 Ma) and Vize pluton
660 (both are LA ICPMS ages; (Fig. 5). Similar U Pb zircon ages – 535 and 546 Ma – have been
661 reported from the Çatalca metagranite exposed at the eastern termination of the Strandja
662 Massif (Yılmaz ahin et al., 2014). New data imply widespread magmatism in the Vize
663 tectonic unit, confirming the existence of Neoproterozoic bedrock within it, and emphasizing
664 the tectonic independence of the fault bounded Kırklareli and Vize units.
665 Regarding the Neoproterozoic – early Paleozoic evolution of the Strandja Massif, the
666 metaconglomerates of the Vize Unit (“Koruköy” and Evciler gneisses) yielding pebble ages
667 of 507 and 533 Ma suggest a Cambrian orogeny before the deposition of the Ordovician
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668 ermat Quartzite. These ages are younger than the Pan African orogeny in Arabia (Stern and
669 Johnson 2010); thus, the available models of relationships between Balkan – Strandja tectonic
670 units and the Gondwana Land need to be redefined (e. g Natal’in et al. 2012a versus Yanev et
671 al. 2006). In Europe, splitting of the Avalonia blocks from the Gondwana Land and opening
672 of the Rheic ocean is usually considered as the early Ordovician (e.g. Murphy et al. 2009). In
673 Strandja, it was the time of the prolong Neoproterozoic – Cambrian magmatism in the
674 subduction related setting (Natal’in et al., 2012b, c; Yılmaz ahin et al., 2014).
675 The initial inference on the Permian age of the Kırklareli metagranites in the Strandja
676 including the Vize Unit (Aydın 1974, 1982) has led previous geologists to the assumption that
677 the age of the ermat Quartzite unconformably lying on the metagranites is Triassic 678 (Çağlayan and Yurtsever 1998). Our Draftnew age data show that the youngest detrital zircon age 679 in this rock is ~ 475 Ma. Considering the very well developed Carboniferous magmatism in
680 the region and a high possibility of the Carboniferous zircon reworking in Permo Triassic
681 times both in the Kırklareli and Vize tectonic units, we suggest that the obtained date is close
682 to the depositional age of the ermat Quartzite. This inference is partly supported by data
683 collected in the Kırklareli Unit, where metasedimentary rocks of the Tekedere Group are
684 intruded by the Carboniferous metagranite (Sunal et al. 2006; Natal’in et al. 2012a) and a
685 minima of the early Paleozoic – Neoproterozoic detrital and inherited zircon ages is around
686 450 Ma (Sunal et al. 2008). It means that we have some evidence of magmatic processes in
687 the Kırklareli Unit between 484 and 450 Ma and younger times (Sunal et al. 2008), but they
688 are absent in the Vize Unit. At the same time, it is possible that the Kırklareli and Vize Units
689 were significantly separated in space.
690 Newly obtained Cambrian ages of the metagranites, detrital zircon ages of the ermat
691 Quartzite, and the lithological features of the Vize Unit suggest a possibility for their
692 correlation with the Istanbul Zone. Similar to the Vize Unit, the Istanbul Zone consists of the
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693 Neoproterozoic basement and the Ordovician Lower Carboniferous sedimentary cover
694 ( engör and Yılmaz 1981;Görür et al. 1997; Ustaömer 1999; Yiğitba et al. 2004; Yılmaz et
695 al. 1997). Facies changes may explain the presence of Silurian and Devonian carbonates in
696 the Istanbul Zone and their absence in the Vize Unit. Pelagic limestones alternating with
697 metacherts of the latter fit the composition of the latest Devonian – earliest Carboniferous
698 stratigraphic levels of the Istanbul Zone. At the same time, we should note that ages of
699 subduction related Carboniferous metagranites in the Strandja Massif (Natal’in et al. 2005a;
700 Sunal et al. 2006; Natal’in et al. 2012a, b and d) are 20 30 Ma younger than the age of the
701 orogeny in the Istanbul Zone that terminated the evolution of a passive continental margin
702 ( engör and Yılmaz 1981). Nevertheless, except the occurrences of the late Carboniferous
703 magmatism in the Vize Unit, its stratigraphic record resembles the Istanbul Zone. In addition,
704 the main age cluster of the ermat QuartziteDraft is identical to the main age cluster determined in
705 the Ordovician quartzites of the Istanbul Zone (Ustaömer et al. 2011). The unique
706 stratigraphic succession of the Istanbul Zone has never been reported from anywhere else in
707 the Pontides so far. However, in Asia one may find a number of regions with a great
708 stratigraphic similarity, for instance (Natal’in et al. 2012a), the Peredovoi Range in Caucasus
709 (Andruschuk et al. 1968; Khain 2001), the Alay microcontinent (Natal'in and engör 2005),
710 and the southern zone of the Chinese Tienshan (Wang et al. 2010).
711 The late Carboniferous magmatic event in the Kırklareli Unit (315 312 Ma) was
712 followed by deformation and emplacement of the Kırklareli metagranites (Sunal et al. 2006,
713 Natal’in et al. 2012a). The late Paleozoic magmatic rocks are also reported in the Balkan and
714 the Rhodope zones (Carrigan et al. 2005; Machev et al. 2015) (Fig. 1). Their ages vary
715 between 290 and 314 Ma but the deformation event is poorly documented. The Central and
716 the Eastern Pontides were magmatically active. The ages of magmatic rocks in the Central
717 Pontides are similar to the Strandja Massif (303 275 Ma, Nzegge et al. 2006), but in the
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718 Sakarya Zone (the Eski ehir region), they are slightly older (319–327 M, Ustaömer et al.
719 2012a). Topuz et al. (2010) and Dokuz (2011) have discovered even older – 318 329 Ma –
720 granitoids in the eastern Sakarya Zone (Eastern Pontides). Ustaömer et al. (2012b) has also
721 reported 356 325 Ma old magmatic rocks in the Yusufeli area (the eastern Sakarya zone).
722 Previously reported Jurassic magmatic rocks (Çağlayan and Yurtsever 1998) of the
723 Kıyıköy region have turned out to be the late Carboniferous (Natal’in et al. 2012a), which
724 required significant reconsideration of the tectonic structure of the Strandja Massif. The U Pb
725 age of metatuffs in the Yavuzdere Complex is 305.9 ±2.5 and intrusive rocks are 302.7±3.3
726 Ma and 303.6±2.5 Ma old. Ductile shear zones separate the Yavuzdere and Mahya complexes
727 which are interpreted here as the paired magmatic arc – accretionary prism units. The 728 Yavuzdere arc occupies the higher structuralDraft position. 729 The Mahya Complex represents an accretionary prism as originally suggested by
730 engör and Özgül (2010). Thin alternation of siliceous shales and cherts (schists and
731 microquartzite now), blocky (mélange!) structures of some horizons, as well as lenses of
732 greenstones, rare metagabbro, and metapyroxenites are a characteristic lithology of some
733 stratigraphic levels. Together with dominance of chlorite and epidote bearing metaclastics
734 and schists, it fits the descriptions of the Jurassic subduction accretion complexes in the
735 Nipponides (Mizutani 1990; Natal'in 1993; Natal'in and Borukayev 1991) as well as many
736 regions in Central Asia ( engör and Natal'in 1996; engör et al. 2014). In the previous
737 studies, this complex has been considered as Triassic in age (Çağlayan and Yurtsever 1998;
738 Okay et al. 2001) but most likely it also includes the Carboniferous rocks as mentioned in the
739 previous paragraph.
740 In this study, we obtained the additional constraints on the age of the late Paleozoic
741 Kırklareli Complex of metagranite, which was previously estimated to be 309 – 257 Ma old
742 (Okay et al. 2001; Sunal et al. 2006; Natal’in et al. 2012a). The Üsküp metagranite that are
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743 exposed directly to the east of the Neoproterozoic – Cambrian Kazandere metagranites (Fig. 3
744 and 5) yields the U Pb age of 299.1 ± 2.7 and 300.6 ± 2.8 Ma. The age of the Ömeroba pluton
745 that also belongs to the Kırklareli metagranite is 251.8 ± 3.4 Ma old and the age of a dyke
746 cutting the Kırklareli pluton is 243.8 ± 5.8 Ma (Table 1). The duration of the calc alkaline late
747 Paleozoic magmatism is an important criterion for the determination of the geodynamic
748 setting of the Strandja Massif in the late Paleozoic. engör et al. (1984) states that during this
749 time, the Strandja Massif (the Kirklareli Nappe and the Strandja Allochthon) evolved as an
750 active continental margin located at the southern margin of the Paleo Tethys Ocean. This type
751 of evolution continued into the Triassic. To the contrary, Okay et al. (2001) has interpreted
752 the Permian magmatism as collision related and they have considered the Triassic succession
753 as accumulations in an epicontinental basin. Natal’in et al. (2005 a and b, 2012a; also see
754 Sunal et. al. 2006, 2008) has interpretedDraft the Permian magmatism as subduction related, but
755 contrary to engör et al. (1984) they state that the Strandja magmatic arc had the southern
756 polarity. It was a segment of the late Paleozoic – early Mesozoic Silk Road arc stretching
757 along the northern margin of the Paleo Tethyan Ocean (Natal'in and engör 2005).
758 Green color of clastic rocks and presence of chlorite and epidote in metasediments
759 unconformably overlying the Paleozoic rocks in the Kırklareli Unit suggest erosion of regions
760 with synchronous magmatic activity. This conclusion is supported by the discovery of a
761 pillowed plagioclase porphyry in the Kırklareli Unit (Natal’in et al. 2005a and b; 2012a).
762 Triassic magmatic activity is described in the neighboring regions of Bulgaria (Chatalov
763 1990; Chatalov 1991; Gerdjikov 2005). Okay and his co authors as well as other researchers
764 have interpreted the Triassic tectonic setting of the Strandja Massif as completely amagmatic
765 and similar to those of the Buntsandstein Muschelkalk succession in Germany (Okay et al.
766 1996; Okay and Tüysüz 1999; Okay et al. 2006; Okay et al. 2001; Hagdorn and Göncüogl,
767 2007; Okay 2008). However, the early Triassic (Indian) age of the Ömeroba metagranite, the
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768 middle Triassic (Anisian) age of the dyke in the Kırklareli pluton (243.8 ± 5.8 Ma), and the
769 late Triassic (Norian) age of the dyke in the Koruköy Complex (213.1 ± 4.1 Ma; Fig.3, Table
770 1) make this conclusion at least questionable. The late Paleozoic magmatic rocks of the
771 Strandja Massif reveal magmatic arc geochemical signature (Natal’in et al. 2012; Natal’in et
772 al. 2005; Sunal et al. 2006) and preliminary data show that Triassic magmatic rocks follow
773 this trend (Natal’in et al. 2012c). We also infer that the late Paleozoic deformation event in
774 the Kırklareli Unit may be a result of intra arc deformation.
775 The Silk Road Arc (Natal'in and engör 2005) had southern polarity and it evolved
776 mainly in the late Paleozoic – Triassic though in places, its evolution can be traced to the
777 Ordovician. The arc is superimposed on the Tarim and Alay microcontinents as well as on 778 smaller continental blocks in the ScythianDraft domain. In the late Paleozoic – Triassic, this arc 779 experienced tremendous internal deformations because of a longitudinal shortening
780 synchronous and genetically related to strike slip tectonics in the Altaids (Natal’in and
781 engör, 2005; engör and Natal’in, 1996; Van der Voo et al., 2006; Metelkin et al., 2010;
782 engör et al. 2014). In the west (Caucasus, Crimea, Pontides), deformations of the Silk Road
783 Arc continued to the Jurassic. Many regions along the arc including the Strandja Massif
784 present evidence of dextral strike slip motions parallel with the strike of the active subduction
785 zone. These motions may cause mixing tectonic units (e. g. the great contrast between the
786 Kırklareli and Vize unit) while subduction was ongoing. Under these kinematic conditions,
787 the slab may not reach a magma generation zone or may reach it only periodically. The
788 oblique subduction may explain a long duration of the Strandja magmatism together with
789 significant variations of its intensity.
790 The following Jurassic history of the Strandja Massif has started with strong
791 penetrative deformations and low amphibolite to greenschist facies metamorphism. Ar Ar age
792 determinations constrain this event to be between165 and 143 Ma (Natal’in et al. 2005b;
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793 Elmas et al. 2011) and Rb Sr whole rock and mica ages vary from 162 to 141−Ma (Sunal et
794 al. 2011). The deformations occurred in a transpressional tectonic setting that is characterized
795 by northward thrusting combined with the significant dextral motions (Natal’in et al. 2005a;
796 Natal’in et al. 2012a,b; Natal’in et al. 2009; Sunal et al. 2011). Almost all above mentioned
797 tectonic units are allochtonous (e.g. see engör and Yılmaz 1981). The volume of effected
798 rocks, the large magnitudes of thrusting and regional metamorphism indicate a significant
799 continental collision at the end of these defamations, which has been underestimated in
800 regional current studies. Most likely, the location of the root zone of the thrusts is in the
801 vicinity of the Intra Pontide suture.
802 This study has changed very significantly our older views of the Strandja Massif. Where it 803 belongs in the larger tectonic environmentDraft of the western Tethysides is not easy to answer, 804 because its rocks resemble both the Pre Uralides and the Pan African systems. The Paleozoic
805 development resembles at once to the northern Caucasian foreland and the Carnic Alps, a
806 clear part of Gondwana Land. The provenance of the Strandja will be known better once we
807 sort out the relationships of the Scythides (Natal'in and engör, 2005) and the Hercynides.
808 That is what is now being undertaken by our group in Đstanbul.
809 6. Conclusions 810 Presented results of studies of the Strandja Massif allowed as formulating the following
811 conclusions:
812 1) The massif consist of the Kırklareli (Paleozoic basement unconformably overlain Permian
813 – Triassic metasedimentary cover and showing a long duration of magmatism from the late
814 Carboniferous to Triassic) and Vise tectonic units (Neoproterozoic basement intruded by
815 Neoproterozoic – Cambrian granitoids and unconformably overlain by the Ordovician –
816 Carboniferous cover that was intruded by the late Carboniferous intrusions), Mahya and
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817 Yavuzdere complexes representing paired accretionary wedge and magmatic arc, and the
818 Jurassic Nappe.
819 2) The tectonic subdivision of the Strandja Massif is supported by new 18 U Pb (SHRIMP
820 and ICP MS methods) ages determinations of magmatic and one detrital zircons.
821 3) The long duration of subduction related magmatism in the region and its continuity in the
822 Triassic contradicts with the widely accepted ideas about the dominance of the passive
823 continental margin settings in the tectonic evolution of the Strandja Massif.
824 5) The massif is interpreted as a fragment of the long lived, Cambrian to Triassic Silk Road
825 magmatic arc. Since the late Paleozoic, this arc evolved on the northern side of Paleo Tethys.
826 7. Acknowledgments Draft
827 This study has been supported by grants from the Istanbul Technical University (BAP
828 Projects no: 32766 and 23128 ) and the TUBITAK (CAYDAG 101Y010 and 110Y177
829 projects). We warmly thank S. Aksay and Ö. Ta for assistance in the field studies. We thank
830 C. Zabcı and M. Yazıcı for careful reading of the manuscript and constructive comments. We
831 sincerely thank O. engör who kindly reviewed manuscript and corrected its English. A.M.C.
832 engör is thanked for reading of the manuscript and making numerous changes and
833 constructive comments.
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886 Hsü, K., Nachev, I., Vuchev, V., 1977. Geologic evolution of Bulgaria in the light of plate 887 tectonics. Tectonophysics 40, 245–256. 888 Jackson, S.E., Pearson, N.J., Grıffın, W.L., and Belousova, E.A., 2004. The application of 889 laser ablation inductively coupled plasma mass spectrometry to in situ U–Pb zircon 890 geochronology. Chem Geol 211: 47 69. 891 Khain, E. V., 1984. Ophiolites and Hercynian Nappe Structure of the Peredivoi Range, 892 Greater Caucasus. Nauka, Moscow, 96p. 893 Kusky, T. M., and Bradley, D. C., 1999. Kinematic analysis of mélange fabrics: examples and 894 applications from the McHugh Complex, Kenai Peninsula, Alaska: Journal of 895 Structural Geology, v. 21, no. 12, p. 1773 1796. 896 Ludwig, K.R., 2001. User's Manual for Isoplot/Ex version 2.49. A Geochronological Toolkit 897 for Microsoft Excel. Special Publication, vol. 1A. Berkeley Geochronology Center, 898 Berkeley, CA, USA (59 pp.). 899 Ma, X., Shu, L., Jahn, B. M., Zhu, W., and Faure, M., 2012. Precambrian tectonic evolution 900 of Central Tianshan, NW China: Constraints from U–Pb dating and in situ Hf isotopic 901 analysis of detrital zircons: Precambrian Research, 222 223, 450 473. 902 Machev, P., Ganev, V., Klain, L., 2015. New LA ICP MS U Pb zircon dating for Strandja 903 granitoids (SE Bulgaria): evidence for two stage late Variscan magmatism in the 904 internal Balkanides, Turkish Journal of Earth Sciences, 24, 230 248. 905 Metelkin, D.V., Vernikovsky, V.A., Kazansky,Draft A.Y., Wingate, M.T.D., 2010. Late Mesozoic 906 tectonics of Central Asia based on paleomagnetic evidence. Gondwana Research 18, 907 400 419. 908 Miyashiro, A., 1972. Pressure and temperature conditions and tectonic significance of 909 regional and ocean floor metamorphism: Tectonophysics, v. 13, no. 1 4, p. 141 159. 910 Mizutani, S., 1990. Mino terrane, in Ichikava, K., Mizutani, S., Hara, I., Hada, S., and Yao, 911 A., eds., Pre Cretaceous terranes of Japan: Osaka, IGCP, p. 121 136. 912 Moore, J. C., 1989. Tectonics and hydrogeology of accretionary prisms: role of the 913 decollement zone: Journal of Structural Geology, v. 11, no. 1 2, p. 95 106. 914 Natal'in, B. A., 1993. History and modes of Mesozoic accretion in Southeastern Russia: The 915 Island Arc, v. 2, p. 15 34. 916 Natal'in, B. A., and Borukayev, C. B., 1991. Mesozoic sutures in the southern Far East of the 917 USSR: Geotectonics, v. 25, no. 1, p. 64 74. 918 Natal'in, B. A., and engör, A. M. C., 2005. Late Palaeozoic to Triassic evolution of the 919 Turan and Scythian platforms: The pre history of the Palaeo Tethyan closure: 920 Tectonophysics, v. 404, no. 3 4, p. 175 202. 921 Natal'in, B. and Say, A. G., 2015. Eocene–Oligocene stratigraphy and structural history of 922 the Karaburun area, southwestern Black Sea coast, Turkey: transition from extension 923 to compression, Geological Magazine, 152 (6), 1104–1122. 924 Natal’in, B., Sunal, G., and Toraman, E., 2005a. The Strandja arc: anatomy of collision after 925 long lived arc parallel tectonic transport, in Sklyarov, E. V., ed., Structural and 926 Tectonic Correlation across the Central Asia Orogenic Collage: North Eastern 927 Segment. Guidebook and abstract volume of the Siberian Workshop IGCP 480: 928 Irkutsk, IEC SB RAS, p. 240 245.
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929 Natal’in, B. A., Satir, M., Sunal, G., and Toraman, E., 2005b. Structural and metamorphic 930 evolution of the Strandja massif. Final report of the 101Y010 Project: Ankara, Türkiye 931 Bilimsel Teknik Ara tırma Kurumu, Yer Deniz Atmosfer Bilimleri ve Çevre 932 Ara tırma Grubu, p. 183+maps. 933 Natal’in, B. A., Satır, M., Sunal, G., and Toraman, E., 2005c. Structural and metamorphic 934 evolution of the Strandja massif: Ankara, The Scientific and Technical Research 935 council of Turkey, Proje No: 101Y010, p. 183+maps. 936 Natal’in, B. A., Sunal, G., and Toraman, E., Tectonics of the Strandja Massif: Example of the 937 Collision after Long Lived Arc Parallel Tectonic Transport, in Proceedings 2nd 938 International Symposium on the Geology of the Black Sea Region, Abstract book, 939 Ankara, 2009, p. 134 136. 940 Natal'in, B., Sunal, G., Satır, M., and Toraman, E., 2012a. Tectonics of the Strandja Massif, 941 NW Turkey: History of a Long Lived Arc at the Northern Margin of Palaeo Tethys: 942 Turkish Journal of Earth Sciences, v. 21, p. 755 798. 943 Natal'in, B., Sunal, G., Gun, E., Wang, B., 2012b. Istranca Masifinin, KB Türkiye, 944 Prekambriyenden Erken Mesozoyiğe Kadar Olan Kayaçları Üzerine Jeokronolojik ve 945 Jeokimyasal Sınırlandırmalar. Proje No: 110Y177. TUBITAK, Ankara, p. 76. 946 Natal’in, B., Sunal, G., and Toraman, E., 2012c. Kinematics of the Mesozoic deformations in 947 the Strandja Massif: Transition between arc parallel tectonic transport to collision, in 948 Kocbay, A., Esat, K., and Hasancebi, N., eds., 65th Geological Congress of Turkey. 949 Abstracts Book: Ankara, ChamberDraft of Geological Engineers, p. 454 455. 950 Natal’in, B., Sunal, G., Zhiqing, Y., and Gün, E., 2012d. Late Paleozoic subduction accretion 951 orogeny in the eastern part of the Turkish Strandja Massif (Vize Kıyıköy region), in 952 Kocbay, A., Esat, K., and Hasancebi, N., eds., 65th Geological Congress of Turkey. 953 Abstracts Book: Ankara, Chamber of Geological Engineers, p. 452 453. 954 Nzegge, O., Satır, M., Siebel, W., & Taubald, H., 2006. Geochemical and isotopic constraints 955 on the genesis of the Late Paleozoic Delikta and Sivrikaya granites from the 956 Kastamonu granitoid belt (Central Pontides, Turkey). Neues Jahrbuch für Mineralogie 957 Abhandlungen, 183, 10–27. 958 Okay, A. I., 2008. Geology of Turkey: A Synopsis, in Yalçın, Ü., ed., Anatolian Metal IV: 959 Bochum, Vereinigung der Freunde von Kunst und Kultur im Bergbau e.V. 960 Okay, A. I., and Tüysüz, O., 1999. Tethyan sutures of northern Turkey, in Durand, B., Jolivet, 961 L., Horvath, F., and Seranne, M., eds., The Mediterranean Basins: Tertiary Extension 962 within the Alpine Orogen, Geological Society, London, Special Publication, 156, p. 963 475 515. 964 Okay, A., and Yurtsever, A., 2006. Trakya Bölgesi: Litostratigrafi birimleri, Ankara, Maden 965 Tetkik ve Arama, Genel Müdürlüğü, Stratigrafi Komitesi, Litostratigrafi Birimleri 966 Serisi 2. 967 Okay, A.I., engör, A.M.C., Görür, N., 1994. Kinematic history of the opening of the Black 968 Sea and its effects on the surrounding regions. Geology, v. 22, p. 267 270. 969 Okay, A. I., Satır, M., and Siebel, W., 2006. Pre Alpide Palaeozoic and Mesozoic orogenic 970 events in the Eastern Mediterranean region: Geological Society, London, Memoirs, v. 971 32, no. 1, p. 389 405.
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972 Okay, A.I., Satır, M., Tüysüz, O., Akyüz, S., and Chen, F., 2001. The tectonics of the Strandja 973 Massif: late Variscan and mid Mesozoic deformation and metamorphism in the 974 northern Aegean: International Journal of Earth Sciences, v. 90, no. 2, p. 217 233. 975 Okay, A.I., Satır, M., Maluski, H., Siyako, M., Monie, P., Metzger, R., and Akyüz, S., 1996. 976 Paleo and Neo Tethyan events in northwestern Turkey: geologic and geochronologic 977 constraints, in Yin, A., and Harrison, M., eds., The Tectonic Evolution of Asia: 978 Cambridge, Cambridge University Press, p. 420 441. 979 Passchier, C., Trouw, R., 2005. Microtectonics. Berlin, Springer Verlag, 366pp. 980 Poller, U., Huth, J., Hoppe, P., & Williams, I. S., 2001. REE, U, TH, and HF distribution in 981 zircon from western Carpathian Variscan granitoids: A combined and ion microprobe 982 study. American Journal of Science, 301, 858–876. 983 Ricou, L. E., Burg, J.P., Godfriaux, I., Ivanov, Z., 1998. Rhodope and Vardar: the 984 metamorphic and the olistostromic paired belts related to the Cretaceous subduction 985 under Europe. Geodinamica Acta, 11, 285–309. 986 engör, A. M. C., and Yılmaz, Y., 1981. Tethyan evolution of Turkey: A plate tectonic 987 approach: Tectonophysics, v. 75, no. 3 4, p. 181 190. 988 engör, A.M.C., Natal'in, B.A., 1996. Palaeotectonics of Asia: Fragments of a synthesis, in: 989 Yin, A., Harrison, M. (Eds.), The Tectonic Evolution of Asia. Rubey Colloquium, 990 Cambridge University Press, Cambridge, pp. 486 640. 991 engör, A. M. C., Özgül, N., 2010. “Đstanbul’unDraft Jeolojisi”, Đstanbul Ansiklopedisi, NTV 992 Yayınları, Đstanbul. 993 engör, A. M. C., Yılmaz, Y., and Sungurlu, O., 1984. Tectonics of the Mediterranean 994 Cimmerides: nature and evolution of the western termination of Palaeo Tethys: 995 Geological Society, London, Special Publications, v. 17, no. 1, p. 77 112. 996 Steiger, R.H., Jäger, E., 1977. Subcomission on Geochronology: convention on the use of 997 decay constants in geochronology and cosmochronology. Earth and Planetary Science 998 Letters 36, 359 – 362. 999 Stern, R.J., Johnson, P., 2010. Continental lithosphere of the Arabian Plate: A geologic, 1000 petrologic, and geophysical synthesis. Earth Science Reviews 101, 29 67. 1001 Sunal, G., Natal’in, B. A., Satır, M., and Toraman, E., 2006. Paleozoic magmatic events in the 1002 Strandja Massif, NW Turkey: Geodinamica Acta, v. 19, no. 5, p. 283 300. 1003 Sunal, G., Satır, M., Natal’in, B. A., and Toroman, E., 2008. Paleotectonic Position of the 1004 Strandja Massif and Surrounding Continental Blocks Based on Zircon Pb Pb Age 1005 Studies: International Geology Review, v. 50, p. 519 545. 1006 Sunal, G., Satır, M., Natal’in, B., Topuz, G., and Vonderschmidt, O., 2011. Metamorphism 1007 and diachronous cooling in a contractional orogen: the Strandja Massif, NW Turkey: 1008 Geological Magazine, v. 148, no. 4, p. 580 596. 1009 Türkecan, A., and Yurtsever, A., 2002. Geological map of Turkey. Istanbul. Scale 1: 500 000: 1010 General Derectorate of Mineral Researc and Exploration, scale 1:500 000. 1011 Topuz, G., Altherr, R., Siebel, W., Schwarz, W. H., Zack, T., Hasözbek, A., Barth, M., Satır, 1012 M., en, C., 2010. Carboniferous highpotassium I type granitoid magmatism in the 1013 Eastern Pontides: The Gümü hane pluton (NE Turkey). Lithos, 116, 92–110.
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1014 Ustaömer, P. A., 1999. Pre Early Ordovician Cadomian arc type granitoids, the Bolu Massif, 1015 West Pontides, northern Turkey: geochemical evidence: International Journal of Earth 1016 Sciences, v. 88, no. 1, p. 2 12. 1017 Ustaömer, P.A., Ustaömer T., Gerdes A., Zulauf G., 2009. "Detrital Zircon Ages From A 1018 Lower Ordovician Quartzite Of The A Degrees Stanbul Exotic Terrane (Nw Turkey): 1019 Evidence For Amazonian Affinity", International Journal Of Earth Sciences, vol.100, 1020 pp.23 41, 2011 1021 Ustaömer, P.A., Ustaömer, T., & Robertson, A.H.F., 2012a. Ion probe U Pb dating of the 1022 central Sakarya basement: A peri Gondwana terrane intruded by late lower 1023 Carboniferous subduction/collision related granitic rocks. Turkish Journal of Earth 1024 Sciences, 21, 905–932. 1025 Ustaömer, T., Robertson, A.H.F., Ustaömer, P.A., Gerdes, A., & Peytcheva, I., 2012b. 1026 Constraints on Variscan and Cimmerian magmatism and metamorphism in the 1027 Pontides (Yusufeli–Artvin area), NE Turkey from U Pb dating and granite 1028 geochemistry. In A. H. F. Robertson, O. Parlak, & U. C. Ünlügenç (Eds.), Geological 1029 development of Anatolia and the easternmost Mediterranean region (pp. 49–74). 1030 London: Geological Society.Special Publications 372/1. 1031 Van der Voo, R., Levashova, N.M., Skrinnik, L.I., Kara, T.V., Bazhenov, M.L., 2006. Late 1032 orogenic, large scale rotations in the Tien Shan and adjacent mobile belts in 1033 Kyrgyzstan and Kazakhstan. Tectonophysics 426, 335 360. 1034 Vernon, R. H., 2004. A Practical GuideDraft to Rock Microstructure, Cambrige, Cambrige 1035 University Press, 594 p. 1036 Wang, X. L., Zhou, J. C., and Griffin, W. L., 2007. Detrital zircon geochronology of 1037 Precambrian basement sequences in the Jiangnan orogen: dating the assembly of the 1038 Yangtze and Cathaysia blocks: Precambrian Research, v. 159 p. 117 131. 1039 Williams, I.S., 1998. "U Th Pb geochronology by ion microprobe", In: McKibben, M.A.; 1040 Shanks III, W.C.; Ridley, W.I.; (Editors), "Applications of microanalytical techniques 1041 to understanding mineralizing processes", Reviews in Economic Geology Special 1042 Publication 7: 1–35 1043 Yanev, S., 2000. Paleozoic terranes of the Balkan Peninsula in the framework of Pangea 1044 asembly. Palaeogeography, Palaeoclimatology, Palaeoecology, 61(1), 151 177. 1045 Yanev, S., Göncüoglu, M. C., Gedik, I., Lakova, I., Boncheva, I., Sachanski, V., Okuyucu, C., 1046 Özgül, N., Timur, E., Maliakov, Y., and Saydam, G., 2006. Stratigraphy, correlations 1047 and palaeogeography of Palaeozoic terranes of Bulgaria and NW Turkey: a review of 1048 recent data, in Robertson, A. H. F., and Mountrakis, D., eds., Tectonic Development 1049 of the Eastern Mediterranean Region, Volume 260, Geological Society, London, 1050 Special Publications, 260, p. 51 67. 1051 Yazıcı, M., and Natal’in, B. A.. tructural geology and sedimentology of the Sermat Quartzites, 1052 Strandja Massif, NW Turkey, in Proceedings Geophysical Research Abstracts 2015, 1053 Volume 17. 1054 Yiğitba , E., Kerrich, R., Yılmaz, Y., Elmas, A., and Xie, Q., 2004. Characteristics and 1055 geochemistry of Precambrian ophiolites and related volcanics from the Istanbul 1056 Zonguldak Unit, Northwestern Anatolia, Turkey: following the missing chain of the 1057 Precambrian South European suture zone to the east: Precambrian Research, v. 132, 1058 no. 1 2, p. 179 206.
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1059 Yılmaz, Y., Tüysüz, O., Yiğitba , E., Genç, S. C., and engör, A. M. C., 1997. Geology and 1060 tectonic evolution of the Pontides, in Robinson, A. G., ed., Regional and Petroleum 1061 geology of the Black Sea and surrounding region, AAPG Memoir 68, p. 183 226. 1062 Yilmaz ahin, S., Aysal N., Güngör Y., Peycheva I., Heubauer F., 2014. Geochemistry and 1063 U–Pb zircon geochronology of metagranites in Istranca (Strandja) Zone, NW 1064 Pontides, Turkey: implications for the geodynamic evolution of Cadomian orogeny. 1065 Gondwana Res 26: 755–771. 1066 1067 Figure captions
1068 Figure 1. Tectonic map of north western Turkey and surrounding regions (compiled using 1069 data obtained in this study as well as information in published sources: engör and Yılmaz 1070 1981; engör et al. 1984; Yılmaz et al. 1997; Okay et al. 2001; Ricou et al. 1998; Okay and 1071 Tüysüz 1999; Yanev 2000; Gerdjikov 2005). The Balkan tectonic unit corresponds to the 1072 Balkan and Thracian “terranes” (Yanev 2000) or Balkan Terrane (Yanev et al. 2006) or the 1073 Balkan and Srednogorie zones of Hsü et al. (1977). Keys to abbreviations: IA – Đzmir Ankara 1074 suture, M – Maritsa Fault, NAF – the North Anatolian fault, V – Vardar suture, WBS – the 1075 West Black Sea Fault. 1076 Figure 2. Studied regions in the Strandja Massif. Areas marked as Fig. 3, Fig. 4, Fig. 5, Fig. 1077 7, Fig. 8, Fig. 9, and Fig. 12 outline theDraft regions discussed in the text. 1078 Figure 3 . Tectonic units of the Kırklareli region after Natal’in et al. (2005b, 2012a). See 1079 Figure 2 for the geographic location. Keys to abbreviations: AH– the Ahmetce Fault, SG – the 1080 Sergen Fault. 1081 Figure 4. – Geological map (a) and cross section (b) of the Kırklareli region of the Strandja 1082 Massif. In Fig. 4a, A and B indicate the cross section position shown in the Fig. 4b. Ductile 1083 faults (dash lines) were formed during the late Jurassic early Cretaceous synchronously with 1084 S2 foliation and L 2 lineation. Their kinematics is based on stretching lineation sense of shear. 1085 Note that the S 2 foliation is generally highly oblique to lithologic boundaries as it is shown in 1086 Fig. 4b. The map is compiled using the Universal Transverse Mercator projection UTM Zone 1087 35N and European Datum 1950. 1088 Figure 5. Tectonic unites of the eastern part of the Strandja Massif (Kıyıköy region, see Fig. 2 1089 for location). Almost all tectonic units are fault bounded. Symbols used for thrusts shows the 1090 kinematic sense of the north and northeast vergent thrusts. This symbol does not indicate dip 1091 direction of the fault plane. For instance, to the east of the Yavuzdere Complex, all fault 1092 planes of this type are northeast dipping. 1093 Figure 6. a – Metaconglomerate of the Evciler lithostratigraphic units with the well 1094 developed S 2 foliation. Rounded clasts of metagranites contain their own foliation (see 1095 discussion in the text). b – Basal conglomerate of the ermat Quartzite above the contact with 1096 the Neoproterozoic – early Cambrian metagranites. Quartz pebbles are strongly flattened in 1097 the plane of the S 2 foliation. c – Alternation of metacherts and marble in the Paleozoic rocks 1098 of the Vize Unit. d – Fine grained laminated microquartzites (metacherts) are a characteristic 1099 lithology of the Mahya Complex.
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1100 Figure 7. Geological setting of marble/metachert alternation (pelagic facies) exposed to the 1101 southwest of Kıyıköy in the upper part of the Rampana schists (see Figure 2 and 5 for the 1102 general location of this map). 1103 Figure 8. Structural relationships between the Mahya and Yavuzdere complexes and ermat 1104 Quartzite in the Kızılağac region (see Figure 2 for the location of this figure). The Mahya 1105 Complex (lower structural position) and the Yavuzdere complex (higher structural position) 1106 are sandwiched between thrust sheets made of the Ordovician Carboniferous metamorphic 1107 rocks containing the ermat Quartzites – the key unit of the Vize Unit. 1108 Figure 9. Structure and succession of the lithological units in the Yavuzdere section (see 1109 Figure 2 for the location). Frequent zones of mylonites that separate marbles and quartzite 1110 packages ( ermat Quartzites ?) suggest intense tectonic mixing of rocks. 1111 Figure 10. a – Intrusive contact between granite gneiss and biotite schist in the Yavuz Dere 1112 section. Granite gneisses of the similar composition yield U Pb zircon SRIMP age of 303.6 1113 ±2.5 Ma. b – Metatuff in the Yavuz Dere section. The metatuff yield U Pb zircon age of 305.9 1114 ±2.5 Ma. c – Carbonate mylonites at the the contact base of the Dolapdere Formation. d – 1115 Fractured nonmetamorphosed dolomite of the Dolapdere formation above the mylonitic base. 1116 Figure 11. Thrust contact between the late Jurassic foliated schist of the Balaban Formation 1117 and Lower Jurassic Dolapdere Formation in the Kula region (see Fig. 4a for location). The 1118 foliation in the dolomite decreases to the SW and thus the lower strain rocks occur structurally 1119 higher the higher strain rocks. Draft 1120 Figure 12. Structural relations of the Jurassic Dolapdere Formation and the Mahya Complex 1121 (see Fig. 2 for the location). The southern exposure of the Jurassic carbonate is a simple thrust 1122 sheet within the Mahya Complex in the hanging wall while the northern exposure of the 1123 carbonates represents a tectonic window. 1124 Figure 13. Concordia diagrams of the Cambrian rocks; (a) and (b) Kazandere Pluton (the 1125 samples KI 252 and 227, respectively), (c) Lala Pluton (the sample KI 225), (d) Vize Pluton 1126 (the sample KI 247), and (e) and (f) two granite gneiss pebbles from the Evciler 1127 metaconglomerate (the samples KI 255.1 and 252.2, respectively). For sample coordinates 1128 and locations see Table 1 and Fig. 5. 1129 Figure 14. Probability density plot of the detrital zircon U Pb ages obtained from the ermat 1130 quartzite (the sample KI 246). The youngest peak is ~ 479 Ma. For sample coordinates and 1131 locations see Table 1 and Fig. 5. 1132 Figure 15. Concordia diagrams of the samples (KI 239.1 and 242, respectively) collected 1133 from the Carboniferous Üsküp Pluton. For sample coordinates and locations see Table 1 and 1134 Fig. 3. 1135 Figure 16. Distribution of the zircon ages belong to a mafic sample (KI 235) collected from 1136 the Kuruköy complex (figure in the middle). Figure on the left is close up view of the 1137 Carboniferous ages that is interpreted as emplacement of the unit and right one is inherited 1138 Cambrian ages. For sample coordinates and locations see Table 1 and Fig. 3. 1139 Figure 17. Concordia diagrams of the samples collected from the Carboniferous Yavuzdere 1140 Complex (the samples 255 and 260, and 257, respectively). For sample coordinates and 1141 locations see Table 1 and Fig. 5 and 9.
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1142 Figure 18. Concordia diagrams of the samples belong to granite gneisses collected from (a) 1143 the Kaletepe (the sample 263) and (b) the Kasatura regions (the sample 265). For sample 1144 coordinates and locations see Table 1 and Fig. 5. 1145 Figure 19. Concordia plots of (a) Ömeroba Pluton (the sample KI 233.3), (b) dyke cutting 1146 Kırklareli Pluton (the sample KI 231), and (c) and (d) dyke cutting the Koruköy Complex 1147 (the sample KI 237). For sample coordinates and locations see Table 1 and Fig. 3.
Draft
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Table 1. Summary chart of the dating study.
Sample No Unit or Location KI 252 Kazandere Pluton,Vize Unit KI 227 Kazandere Pluton,Vize Unit KI 225 Lala Pluton, Vize Unit KI 247 Vize Pluton, Vize Unit KI 255.1 Pabble in the Evciler metaconglomerate, Vize Unit KI 252.2 Pabble in the Evciler metaconglomerate, Vize Unit KI 246 ermat Quartzite (Kızılağaç road) KI 239.1 Üsküp Pluton, Kırklareli Unit KI 242 Üsküp Pluton, Kırklareli Unit 255 Yavuzdere Unit 260 Yavuzdere Unit 257 Yavuzdere Unit KI 235 Kuruköy Complex, Kırklareli Unit 263 Kaletepe region, Vize Unit 265 Kasatura region, Vize KI 233.3 Ömeroba Pluton, Kırklareli Unit KI 231 Dyke cutting Kırklareli Pluton, Kırklareli Unit KI 237 Dyke cutting the Koruköy Complex, Kırklareli Unit Draft
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Coordinate Method 27°52'53.215"E; 41°41'11.418"N LA ICPMS 28°1'8.831"E 41°35'31.637"N SHRIMP 27°35'35.951"E 41°44'24.79"N SHRIMP 27°47'7.263"E; 41°34'30.777"N LA ICPMS 27°35'35.911"E; 41°44'24.918"N LA ICPMS 27°35'35.911"E; 41°44'24.918"N LA ICPMS 27°52'54.84"E; 41°41'13.462"N LA ICPMS 27°27'16.935"E; 41°46'27.899"N LA ICPMS 27°27'18.143"E; 41°45'48.372"N LA ICPMS 27°53'3.909"E 41°41'10.213"N SHRIMP 27°56'15.877"E 41°42'45.628"N SHRIMP 27°54'22.008"E 41°44'50.099"N SHRIMP 27°14'28.264"E 41°51'59.724"N LA ICPMS 28°4'37.939"E 41°36'38.349"N SHRIMP 28°7'36.193"E 41°34'41.85"N SHRIMP 27°2'44.287"E; 41°56'42.828"N LA ICPMS 27°6'28.537"E; 41°45'34.199"N LA ICPMS 27°16'15.776"E; 41°52'31.14"N LA ICPMS Draft
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Age (Ma) 542.6 ± 3.5 Ma, Cambrian 535.8 ± 4.2 Ma, Cambrian 546.4 ± 4.7 Ma, Cambrian 506.1 ± 4.5 Ma, Cambrian 507.9 ± 5.8 Ma, Cambrian 533.1 ± 6.1 Ma, Cambrian 2049 Ma, Paleoproterozoic (Orosirian) 478 Ma, early Ordovician (Tremadocian Floian) 299.1 ± 2.7 Ma, Permo Carboniferous 300.6 ± 2.8 Ma, Carboniferous 303.6 ± 2.5 Ma, Carboniferous 302.7 ± 3.3 Ma, Carboniferous 305.9 ± 2.5 Ma, Carboniferous 304.9 ± 7.9 Ma, Carboniferous 311.3 ± 3.1 Ma, Carboniferous 312.5 ± 2.4 Ma, Carboniferous 251.8 ± 3.4 Ma, Permo Triassic 243.8 ± 5.8 Ma, Triassic 213.1 ± 4.1 Ma, Triassic Draft
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24° 26° 28° 30° 32° 100 km Moesian block
43°
B alkan Zone
Black Sea M 42° S S 42° akar tra nd ja M T . WBS
Thrace k lda Basin gu on Z 41° Istanbul NAF Marmara Sea
V Aegean Sea 40° 40° IA
24° 26° 28° 30° 32°
Istanbul and Moesian block BaDraftlkan Zone/Strandja Massif Rhodope Massif Zonguldak zones Fore-Balkan Zone Valeka Unit Serbo-Mace- Sakarya zone donian Zone East-Srednogorie Mandritsa arc Pelagonian Anatolide- volcanic zone Zone Tauride block
Late Cretaceous arc Cenozoic volcanic rocks Cenozoic basins
suture shear zones thrust faults
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Draft
139x103mm (300 x 300 DPI)
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0 Cainozoic Kuzulu Compex ´ 0
° Kula pluton 2
4 Jurassic Nappe Kirklareli Complex Triassic Metasedimentary Paleozoic metasedimentary Complex rocks and metagranitoids
Korukuy Complex Faults
K apa KI-233.3 kli s KI-242 sample locations ync Ömeroba line pluton 0 1 2 3 4 5 km
SG KI-237
K1-235 ´ ´ 0 ´ 0 5 ° 1 4 AH
Kırklareli pluton
KI-239-1 KI-231 Draft KI-242
Üsküp pluton
27°0´0´´ 27°20´0´´ 27°30´0´´
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0 Kula 45 x s
´ 0 1 2 3 4 5km metaconglomerate e 80 60 s limestones l
0 2 a p ° A 60 85 r u 2 50 50 32 m J marble gneiss 4 65 46 40 o
15 C 15 80 60 y
46 26 Cainozoic ö 57 26 metasandstone
60 k x calc-schist
46 60 u 45 e r 23 40 30 l o 15 70 Late Jurassic p chlorite - sericite
60 K quartzite
30 m 35 50
80 o 30 black shale schist
1 C 50
20 80 35 and schist y green schist 14 30 12 25 r 12 20 a 20 t 12 55 metasandstone
40 n
e green Kuzulu Complex 24 60 45 m 18 10 25 i metaconglomerate 8 d 28 15 10 40 e biotite schist
15 35 s 28 c 14 i 22 a green diamictite t o
50 e 44 26 z
35 o biotite gneiss 3 K 35 M white 10 a e p l 26 a c k i li metaconglomerate a 52 s s undivided 10 y P n s 42 20 cli n a metasediments e i
60 28 r 5 40 white metasandstone
60 26 40 5 T
20 biotite-hornblende s
46 leucocratic n 45 25 52 20 orthogneiss o metagranite i
64 12 s 15 14 15 u
15 r
biotite-hornblende t 12 25 meta- 50 40 n 30 i 40 18 serpentinite metagranite 30 n 31 22 38 a 14 20 15 20 i 13 biotite-muscovite 52 36 20 25 m 50 30 32 20 r 58 15 metagranite
38 e 46 23 22 27 25 30 22 30 25 P 80 - 25 45 40 22 25 e 26 46 15 35 16 32 40 88 biotite-muscovite r
35 40 p 10 33 38 20 62 5 orthogneiss 62 15 32 46 30 39 25 30 38 22 15 56 44 28 70 25 46 34 35 70 35 20 87 19 S foliation 44 70 25 20 20 28 2 30 80 28 40 80 Draft 50 82 24 32 60 44 89 24 50 30 bedding 46 5 70 18 32 20 20 28 30 22 62 40 45 60 30 20 24 18 78 64 60 28 80 55 54 10 12 85 50 45 50 20 36 70 40 20 72 45 20 46 80 50 24 15 34 83 50 45 10
´ 46
´ 15 50 24 50
0 83 74 20 64 42 ´ 62 24 33 35 22 0 87 60 32 24 30
5 70
° 70 26
1 40 70 34 70 4 55 40 48 42 22 64 27 52 85 30 72 74 45 32 46 50 55 78 45 68 44 45 25 30 Ah 38 36 72 19 72 m 58 72 70 etc 47 35 36 e F 44 65 au lt 56 55 60 42 48 22 50 52 22 88 34 56 80 80 57 10 74 70 46 37 77 80 76 42 34 35 48 74 48 68 45 84 24 32 30 55 32 48 36 35 57 50 37 75 35 24 25 84 30 62 35 30 60 58 10 72 84 30 65 10 70 32 30 65
Permian intrusins (Kirklareli Complex) Structural rocks 18 quartz-feldspathic mylonitic granite gneiss 22 metagranite 62 carbonate mylonite gneiss (Kirklareli Complex) blastomylonite (Kirklareli Complex a 62 brittle fault:a) undiffe1r4entiated; granite foliated granite gneiss b c b) thrust; c) s42trike-slip B and metaconglomerates) 45 Seytandere a ductile fault:a) undifferentiated; augen gneiss metagranites mylonite cataclasite b c d b) thrust; c) strike-slip; d) inferred 27°0´0´´ https://mc06.manuscriptcentral.com/cjes-pubs27°20´0´´ 27°30´0´´ Page 51 of 66 Canadian Journal of Earth Sciences
S N B Paleozoic basement Mesozoic cover A Kırklarei pluton Jurassic Kula carbonates pluton biotite metagranite foliated mylonitic schist metagranite mylonite orthogn. congl. green marble Draft metasand. dolomite 0 0
1 1
2 km 2 km
0 1 2 3 4 10 km Litholpgic contact Late Jurassic-Early Cretaceous (S2) foliation
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27°50'0"E 28°0'0"E Neogene-Quaternary 27°40'0"E Eocene Upper Cretaceous Igneada volcanic rocks Jurassic phyllite and metasandstone
41°50'0"N Jurassic dolomite Demirköy Mahya Complex
Yavuzdere Complex Carboniferous(?) marble and chert Sıvrıler Ordovician - Carboniferous
Ü quartzite and schist s k Lower Paleozoic Evciler ü p gneisses p l Neoproterozoic u KI-255 Draft 257 t o metasediments n Cretaceous granite 7 Evciker 255 Carboniferous metagranite 260 Akoren Sergen KI-246Kızılağac Kışlacık KI-227 KI-252 Neoproterozoic - Cambrian 1 metagranite 41°40'0"N North vergent thrust Fault (mainly dextral 1 Kazandere Kıyıköy strike-slip) 2 Vize KI-247 Samples for U-Pb dating 3 Avacık 8 Cambrian 6 4 Bahçeköy intrusions Aksicim 28°10'0"E 5 Lala 263 6 Aksicim 5 9 7 Evcıler KI-225 KI-247 8 Kale Tepe Carboniferous 2 265 9 Kastura intrusions Vize 4 3 0 5 10km
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28°4'0"E 28°5'0"E 28°6'0"E
1,200 600 0 Meters Quaternary
Eocene h h 47
h60 marble
N
" h D h 45
a 0 marble and chert
' h 85 m
7 h 54 h
3
° 50 52 h Q-Musc schist 1 h h 4 30 Q-Musc-Cl schist
water reservoir h48 24 h
h 38 Şermat Quartzite h 54
h h44 h 46 40
44 h 60
54 h h h
55 h 28
h50 20 60 h h h Draft h h 54h Sm. 263 h 55 70 h 311±3 Ma h h 42 h 44 40 56 43 h 26 h
h 40 h h 66 52 32 44 h h h 40 h h h50 h40 42 60 h6h2 h h21 hh h 44 h40
h 36 N h " 0 '
6 h40 3
h 40
° h 24 1 30 Carb. metagranite 4
a h Carb. granite gneiss b fault (a) and inferred fault (b) 46 Carb. leucogranite h S foliation gneiss 2
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27°51'0"E 27°52'0"E 27°53'0"E
h
h h 30
20
75 h 38
h 38 h
h 30 h
h h
64 30 Sam. 255
h 40 303.6 ±2.5 Ma 5 10 h h 30
38 1h5
h 46 4h0h
h h 32 32 h 42 h50 50 j h52h 76 3h5 40 h h 45 50 41°43'0"N
h30 6h2 h65
h h 28h35 h 45 h h h 55 60 35 17 h35 h15 h10
2, h12 h Draft 625 0 Meters
Quaternary greenschist Mahya Complex Şermat Quartzite Ordovician- talk schist and mylonite Carboniferous quartz-muscovite-chlorite Vize Unit h30 S foliation schist 2
orthogneisess L2 lineation (top-to-north sense of shear) Carboniferous metagranite Yavuzdere thrust (synchronous to S2 and L2) Complex quartz-feldspatic strike-slip fault U-Pb age orthogneiss 304±3
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quartz-feldspatic granite gneiss orthofneiss h70 metagabbro and metagranite 60 mafic metavolcanics hh Ü52 Bt schist Sm. 257 h 305.9±2.5 Ma h metasandstone Ü 50
amphibolite h
25 intermediate h30 metavolcanics Ü h h Ü Ü10 25 metatuff Draft h N h 14 marble and chert h20 h42 greenschist 40 hÜ 30 and chert hÜ
30 Üh 30 h h 20 greenschist h65 h45 h quartzites hh65 42 40 30 S foliation h 2 h h h65 Ü60 7 h
L2 lineation 40 h Ü Ü 64
mylonite 750 0 Meters
306±3 U-Pb age
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Jurassic dolomite 27°46'0"E 27°47'0"E 27°48'0"E
Jurassic dolomitic marble and schist 1,200 0 h50 h
10 Ü25 Mahya Complex jj j 14 quartzite 20
Neoproterozoic? biotite schist
Neoproterozoic - Cambrian h
35 quartzofeldspatic gneiss h 50 Neoproterozoic - Cambrian 41°44'0"N
K-feldspar metagranite Üh 1
mylonite h Üh 25 20
carbonate mylonite Draft
D2 thrust h
46 later thrust h
h30 46 j bedding h
45 Üh h
foliation and lineation 50 41°43'0"N h
hÜ 40
Ü25 N 60 h
15
hÜ
h
h 12 h
h Ü 10 h Üh 6 h 22 70 Ü50 25 14 hÜ
h 35 5 41°42'0"N
h 25 Ü Ü 45 26 hÜ h 25hhÜ
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