Miocene Sandstones Related to the Tethyan Development of Cyprus', Journal of the Geological Society

Edinburgh Research Explorer U-Pb detrital zircon ages used to infer provenance and tectonic setting of Late Triassic- Miocene sandstones related to the

Tethyan development of Cyprus

Citation for published version: Chen, G, Robertson, A & USTAÖMER, TMUR 2019, 'U-Pb detrital zircon ages used to infer provenance and tectonic setting of Late Triassic- Miocene sandstones related to the Tethyan development of Cyprus', Journal of the Geological Society. https://doi.org/10.1144/jgs2018-207

Digital Object Identifier (DOI): 10.1144/jgs2018-207

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Published In: Journal of the Geological Society

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Download date: 10. Oct. 2021 1 U-Pb detrital zircon ages used to infer provenance and tectonic setting of Late Triassic- 2 Miocene sandstones related to the Tethyan development of Cyprus

4 Guohui Chen1*, Alastair H. F. Robertson1 & Timur Ustaömer2

5 1 School of GeoSciences, University of Edinburgh, West Mains Road, Edinburgh, EH9 3JW, UK

6 2 Department of Geology, Istanbul University-Cerrahpaşa, 34320-Avcılar, Istanbul, Turkey

7 *Correspondence ([email protected])

9 Abstract

10 Zircons from Late Triassic deep-water sandstone turbidites of the Mamonia Complex (W Cyprus) 11 have prominent Ediacaran-Cryogenian and Tonian-Stenian-aged populations, with smaller 12 populations at c. 2.0 Ga and 2.7-2.5 Ga but only minor concordant Paleozoic zircons. Late Jurassic- 13 Early Cretaceous deep-water gravity-deposited sandstone, also from the Mamonia Complex, has a 14 greater proportion of Ediacaran-Cryogenian and Tonian-Stenian zircons, but less abundant 15 Paleoproterozoic, Archean and Paleozoic ones. Similar zircon populations characterise an Early 16 Cretaceous shallow-marine sandstone block in the Moni Melange (S Cyprus). The dominant 17 Ediacaran-Cryogenian and Tonian-Stenian zircon populations originated in the NE Africa/Arabian- 18 Nubian Shield (N Gondwana). However, they were probably recycled from Paleozoic sandstones 19 within Anatolia following South Neotethyan rifting that also gave rise to sparse Permian-Triassic 20 zircons. Paleozoic zircons reflect Variscan magmatism within Anatolia. Both Late Cretaceous and 21 overlying Eocene sandstone turbidites in the Kyrenia Range (N Cyprus) contain prominent 22 Ediacaran-Cryogenian populations, together with small Archean, Tonian, Carboniferous and Late 23 Cretaceous populations, with additional Triassic zircons in the Eocene sample. Late Cretaceous 24 zircons dominate an overlying Late Miocene sandstone turbidite, together with minor Ediacaran- 25 Cryogenian, Eocene and Miocene populations. The Late Cretaceous zircons record continental 26 margin arc and/or ophiolite-related magmatism, whereas Eocene and Miocene zircons represent 27 collision-related magmatism, both in S Turkey.

28 Supplementary materials: Detailed zircon U–Pb geochronological data and supplementary figure are 29 available at XXXX. 30 Detrital zircon dating aids understanding of the tectonic development of Tethys in the Eastern 31 Mediterranean area, as elsewhere (Zulauf et al. 2007; Ustaömer et al. 2014; Avigad et al. 2015; 32 Buckman et al. 2018). Cyprus is best known for the Late Cretaceous (c. 90 Ma) Troodos ophiolite 33 (Gass 1968, 1990; Moores & Vine 1971; Pearce 1975; Mukasa & Ludden 1987; Robinson & Malpas 34 1990; Robertson 2002) that formed within the Southern Neotethys. An understanding of the tectonic 35 setting of the ophiolite depends on taking account of the sedimentary provenance of two adjacent 36 allochthonous terranes. The first is the Mamonia Complex in west Cyprus, together with the related 37 Moni Melange in south Cyprus (Lapierre 1975; Robertson 1977; Robertson & Woodcock 1979). The 38 second is the Kyrenia Range in northern Cyprus (Ducloz 1972; Baroz 1979; Robertson & Woodcock 39 1986) (Fig. 1). The two allochthonous crustal units also need to be considered in the wider context of 40 North Africa to the south and the mosaic of continental, ophiolite-related and magmatic arc-related 41 units that make up Anatolia, including the Taurides in the south and the Pontides in the north (Okay 42 & Tüysüz 1999) (Fig. 2). 43 The depositional ages of the sedimentary successions associated with the Mamonia Complex 44 and the Kyrenia Range are mainly well known, based on micropaleontological studies and some 45 strontium isotope dating (e.g. Baroz 1979; Urquhart & Banner 1994; Hakyemez et al. 2000; Lord et 46 al. 2000; McCay et al. 2013). The facies and petrography of these units have been extensively 47 studied and combined with other geological and geophysical evidence to produce regional tectonic 48 reconstructions (McCay & Robertson 2012; Robertson et al. 2012a; Torley & Robertson 2018). 49 However, conventional petrographic studies do not indicate the age of source constituents. In this 50 paper, we provide the first high-quality radiometric age data of detrital zircons from Late Triassic 51 and Cretaceous sandstones from the Mamonia Complex (and the Moni Melange), and also from Late 52 Cretaceous-Miocene sandstones from the Kyrenia Range. Our results emphasize the contribution of 53 detrital zircon dating to regional provenance analysis and tectonic reconstruction, while also 54 highlighting the complexities inherent in any region involving the dispersal and amalgamation of 55 continental fragments, such as characterise the Tethyan orogen. 56 57 Role of detrital zircon dating 58 There are four main ways in which detrital zircon dating can shed light on Tethyan development in 59 the Cyprus region: (1) to help constrain the maximum age of sediment deposition; i.e., the youngest 60 detrital zircon ages will be compared to existing age data; (2) to identify sedimentary provenance by 61 comparing the ages of tectono-thermal events recorded in the zircon grains with possible source units; 62 e.g. major cratons, epi-cratonic basins and peri-Gondwanan terranes; (3) to help identify 63 sedimentary provenance by comparison of zircon ages with known igneous events in the region, 64 notably ophiolite genesis, subduction-related arc magmatism and collision-related volcanism in the 65 surrounding region; and (4) to test, and if appropriate, modify existing tectonic models of the 66 Mesozoic-Cenozoic Tethys in the easternmost Mediterranean region. 67 68 Regional geological setting 69 Cyprus is a microcosm of Tethys because it includes remnants of: (1) a rifted passive margin in the 70 form of the Triassic-Cretaceous Mamonia Complex in west Cyprus and the related Moni Melange in 71 south Cyprus; (2) supra-subduction zone (SSZ)-oceanic crust represented by the Late Cretaceous 72 Troodos ophiolite; and (3) An active (convergent) margin represented by the latest Cretaceous- 73 Neogene rocks of the Kyrenia Range, north Cyprus (Fig. 1). The easternmost Mediterranean region 74 and Anatolia include the remnants of several Mesozoic oceanic basins, including the Southern 75 Neotethys (Şengör 1984; Robertson & Dixon 1984; Stampfli & Borel 2002; Göncüoğlu et al. 2003; 76 Barrier et al. 2018). The Southern Neotethys is widely considered to have formed by rifting of the 77 northern margin of Gondwana during Late Permian-early Mesozoic time (Şengör 1984; Robertson & 78 Dixon 1984; Stampfli & Borel 2002; Göncüoğlu et al. 2003). The Southern Neotethys closed during 79 Late Cretaceous-early Cenozoic time probably related to northward subduction (Şengör & Yılmaz 80 1981; Robertson & Dixon 1984; Barrier et al. 2018). Remnants of the Southern Neotethys including 81 ophiolites in SE Turkey were emplaced onto the northern margin of the North African-Arabian Plate 82 as a consequence of Late Cretaceous subduction and subsequent trench-passive margin collision. 83 However, the Troodos ophiolite remained in a remnant oceanic basin during the Cenozoic. The 84 ophiolite was emplaced against Tauride continental crust to the north by the Late Miocene-Early 85 Pliocene (Harrison et al. 2004; McCay & Robertson, 2013; Robertson et al. 2014) and collided with 86 the leading edge of African continental crust represented by the Eratosthenes Seamount during the 87 Plio-Quaternary with corresponding uplift of the Troodos Massif (Robertson, 1998).

88 Mamonia Complex/Moni Melange 89 The entirely sedimentary Ayios Photios Group of the Mamonia Complex in west Cyprus 90 encompasses the Late Triassic Vlambouros Formation, the Late Triassic Marona Formation and the 91 Late Triassic-Early Cretaceous Episkopi Formation (Robertson & Woodcock 1979; Torley & 92 Robertson 2108) (Figs. 3, 4). The Vlambouros Formation is characterised by grey, thin, medium and 93 thick-bedded turbiditic sandstones, intercalated with siltstones/mudstones, together up to 30 m thick 94 (Lapierre 1975; Robertson & Woodcock 1979; Torley & Robertson 2018). The Marona Formation, 95 where present, depositionally overlies the Vlambouros Formation (e.g. Dhiarizos Valley), where it 96 comprises bioturbated hemipelagic limestones and mudstones, up to 25 m thick (Lapierre 1975; 97 Robertson & Woodcock 1979; Torley & Robertson 2018). The overlying deep-water Episkopi 98 Formation (as redefined by Torley & Robertson, 2018) comprises non-calcareous reddish mudstones, 99 shales, metalliferous sediments, ribbon-bedded radiolarites and redeposited shallow-water carbonates, 100 together with fine to medium-bedded quartzose sandstones (Robertson & Woodcock 1979; Torley & 101 Robertson 2018). The upper part of the succession is characterised by locally distributed, medium to 102 coarse-grained quartzose sandstones (Akamas Member), that are locally very thick-bedded (e.g. 103 Akamas Peninsula) (Robertson & Woodcock 1979). 104 In addition, the related Moni Melange of southern Cyprus (Fig. 5) includes two allochthonous 105 components. First, there are detached blocks of Mamonia Complex-type rocks including alkali basalt, 106 radiolarite and pelagic limestone. Large detached blocks of Early Cretaceous-aged shallow-marine 107 quartzose sandstone (c. 60 m thick) are known as the Pareklisia Member. Secondly, there are thrust 108 sheets of serpentinite associated with emplacement of the Troodos oceanic lithosphere (Robertson 109 1977). 110 During this study, detrital zircons were dated from sandstones of the Late Triassic Vlamborous 111 Formation, the Late Jurassic-Early Cretaceous Akamas Member (Episkopi Formation) and the Early 112 Cretaceous Pareklisia Member.

113 Kyrenia Range 114 The intact stratigraphy the Kyrenia Range (Fig. 6) begins with the Trypa (Tripa) Group, c. 700 m 115 thick, which is dominated by Triassic-Cretaceous shallow-marine carbonates. These lithologies were 116 brecciated, recrystallized and regionally metamorphosed to greenschist grade during the Late 117 Cretaceous (Ducloz 1972; Baroz 1979; Robertson & Woodcock 1986). The Trypa (Tripa) Group is 118 unconformably overlain by the Campanian-Middle Eocene Lapithos (Lapta) Group (up to c. 1500 m 119 thick), which is mainly carbonate breccias, pelagic carbonates, basic volcanics and calcareous 120 sandstones. Unconformably above comes a very thick (up to c. 4000 m), variably deformed 121 succession of dominantly siliciclastic sedimentary rocks, mainly conglomerates, sandstone turbidites 122 and mudstones, forming the Late Eocene-Late Miocene Kythrea (Değirmenlik) Group (Fig. 6) 123 (Baroz 1979; Hakyemez et al. 2000; McCay & Robertson 2012; McCay et al. 2013). The intact 124 succession ends with Messinian evaporites and was followed by southward-directed thrusting during 125 latest Cretaceous-earliest Pliocene time, related to regional continental collision (McCay & 126 Robertson 2013; Robertson & Kinnaird, 2016). 127 During this work, detrital zircons were analysed from sandstone turbidites of the Late 128 Campanian-Maastrichtian Kiparisso Vouno (Alevkaya Tepe) Member and the Middle Eocene 129 Kalograia-Ardana (Bahçeli–Ardahan) Formation (Lapithos (Lapta) Group), the Late Miocene Davlos 130 (Kaplıca) Formation and the Middle-Late Miocene Mia Milia (Dağyolu) Formation (Kythrea 131 (Değirmenlik) Group). 132 133 Analytical methods

134 Zircon separation 135 The zircon separation followed previously reported procedures (McLennan et al. 2001; Fedo et al. 136 2003; Ustaömer P. A. et al. 2012a), with slight modifications. Approximately 10 kg of sandstone 137 were collected from each typical medium to coarse-grained sandstone. A polished thin-section was 138 made from each sample for optical microscope examination. The samples were crushed and sieved 139 using 4 meshes of 63 to 500 μm to maximize detrital zircon recovery. The heavy minerals were 140 concentrated hydrodynamically using a Wilfley table, then washed and dried. A hand magnet was 141 used to remove strongly magnetic minerals. Less magnetic minerals were then removed using a 142 Frantz Isodynamic magnetic separator at progressively higher magnetic currents (0.4, 0.8 and 1.5 143 amps), with side slopes of 20° and tilt of 25°. Non-magnetic heavy minerals were next 144 gravitationally separated using the heavy liquid, lithium polytungstate (specific gravity: 2.85 g/ml). 145 For each sample, ~150-200 zircon grains were randomly picked under a binocular microscope, 146 mounted in epoxy resin and polished sufficiently to expose the centre of the grains.

147 Scanning electron microscopy 148 Zircon morphology and internal micro-texture were observed, using cathodoluminescence (CL), with 149 a Carl Zeiss SIGMA HD VP Field Emission Scanning Electron Microscope (SEM) at the School of 150 GeoSciences, University of Edinburgh. Back-scattered electron detector (BSED) images were used 151 to examine zircon morphology (including inclusions).

152 SIMS U-Pb dating of zircon 153 U-Pb isotopic measurements were made on a CAMECA ims-1270 SIMS at the Edinburgh Ion 154 Microprobe Facility (EIMF), in the Material and Micro-Analysis Centre (EMMAC) of the School of 155 GeoSciences, University of Edinburgh using the methods detailed by Kelly et al. (2008) and 156 Ustaömer P. A. et al. (2012b). U/Pb ratios were calibrated against measurements of the Geostandard 157 91500 zircon (~1062.5 Ma) (Wiedenbeck et al. 1995). Measurements over a single ‘session’ (a 158 period during which no tuning or changes to the instrument took place) gave a standard deviation of 159 c. 1σ (1%) for 206Pb/238U measurements, for individual repeats of 91500. Rapid (‘short protocol’) 160 analysis (7 minutes per analysis) was used, in which pre-sputter was limited to 60 seconds and

161 measurements to peaks of Zr2O (all four lead isotopes), ThO2 and UO2. Eight cycles were measured 162 (none were excluded). The 91500 standard was re-analysed after every 10 measurements. Correction 163 for in situ common Pb was made using measured 204Pb counts above that of the detector background 164 and modern-day common Pb composition. The modern Pb correction assumes that in nearly all cases 165 measured common Pb results from contamination on the sample surface and in exposed cracks. 166 Age determinations were derived from the U-Th-Pb isotope data (632 analyses), of which 578 167 were 90-110% concordant. Six of the eight samples analysed (80-100 randomly analysed zircons) 168 provide significant detrital zircon age distributions (e.g. Andersen 2005). The remaining two samples 169 have fewer analyses because few zircons could be separated; these are viewed as exploratory data. 170 Full isotopic results are given in supplementary material Table S1. 171 Data reduction utilised geochronological plots that were produced using ISOPLOT spreadsheets 172 (Ludwig 2012) and AgeDisplay (Sircombe 2004). The International Chronostratigraphic Chart of the 173 International Commission on Stratigraphy (Cohen et al. 2018) is used here for the timescale. 174 175 Sampling and petrography

176 Mamonia Complex & Moni Melange

177 Vlambouros Formation 178 Two samples of medium to coarse-grained sandstone were analysed from the Late Triassic 179 Vlambouros Formation (W Cyprus). Sample GC14-3 (GPS: 34°46′55″ N, 32°31′33″ E) is a thin to 180 medium-bedded sandstone turbidite from the upper part of the Vlambouros Formation, south of 181 Episkopi village (Fig. 4). Sample GC14-9 (GPS: 34°58′33″ N, 32°21′39″ E) is a medium to thick- 182 bedded sandstone turbidite from the upper part of the formation, south of Fasli (Fig. 4). Both 183 sandstones have angular to sub-angular, poorly to moderately sorted grains, with a grain-supported 184 texture, set in a micritic matrix. Quartz grains predominate, commonly with undulose extinction, 185 together with plagioclase, orthoclase, hornblende, epidote, muscovite and occasional heavy minerals 186 (including zircon) and opaque grains. Lithic fragments include metamorphic quartzite (Torley & 187 Robertson 2018).

188 Akamas Member 189 Sample GC14-16 (GPS: 34°51′37″ N, 32°36′18″ E) is a thick-bedded, coarse-grained quartzose 190 sandstone (grains up to 3 mm in diameter) of Late Jurassic-Early Cretaceous age, from near Ayios 191 Photios (Fig. 4). This sandstone has sub-rounded to well-rounded grains that are moderately to well- 192 sorted with a grain-supported texture. Quartz dominates, with occasional very fine-grained quartzite, 193 microcline, plagioclase and muscovite (Torley & Robertson 2018). 194 Pareklisia Member (Moni Melange) 195 Sample GC14-17 (GPS: 34°44′09″ N, 33°09′27″ E) was collected from a detached block of medium 196 to coarse-grained, pale-yellow, poorly cemented, cross-bedded, pebbly quartzose sandstone of the 197 Early Cretaceous Pareklisia Member, from south of Pareklisia village (Fig. 5). The sandstone is 198 petrographically similar to the Akamas Member of the Mamonia Complex (Robertson 1977; 199 Swarbrick & Robertson 1980). The grains are sub-angular to sub-rounded and poorly sorted, with a 200 grain-supported texture. Quartz grains predominate, with occasional feldspar, hornblende, muscovite 201 and zircon (Robertson 1977).

202 Kyrenia Range

203 Kiparisso Vouno (Alevkaya Tepe) Member 204 A sandstone turbidite, sample GC14-47 (GPS: 35°19′40″ N, 33°08′28″ E), was collected from the 205 Late Campanian-Maastrichtian type section of this member, to the north of the E-W ridge-crest road 206 (Fig. 7). This sample is dominated by monocrystalline and polycrystalline quartz and muscovite 207 schist, together with rare, angular fragments of basalt, angular to sub-rounded grains of red 208 radiolarian chert, red mudstone, pyroxene and biotite. Bioclastic detritus, includes plankic 209 foraminifera and echinoderm debris (Robertson et al. 2012b).

210 Kalograia-Ardana (Bahçeli–Ardahan) Formation 211 Sample GC14-32 (GPS: 35°22′25″ N, 33°51′58″ E) is an Eocene-aged, normal-graded sandstone 212 turbidite from the Mersinlik (Flamoudi) area, eastern Kyrenia Range (Fig. 7). The sandstone has 213 sand-sized, angular to subangular, ophiolite-derived grains, mainly serpentinite, with common red 214 radiolarian chert and minor basalt. Terrigenous grains include unstrained quartz, muscovite, biotite 215 and lithic grains (e.g. siltstone, quartzite, schist and limestone). Bioclastic grains include fragmented 216 benthic foraminifera and bivalve shells; carbonate intraclasts are also present (Robertson et al. 2014).

217 Davlos (Kaplıca) Formation 218 Sample GC14-25 (GPS: 35°20′40″ N, 33°34′44″ E) is a Late Miocene, medium-grained sandstone 219 turbidite, from west of Bahçeli (Kalograia) (Fig. 7). The sandstone is poorly-sorted, medium-grained 220 and contains angular to sub-rounded grains of quartz (mainly monocrystalline), plagioclase and 221 carbonate rocks, together with igneous rock fragments (e.g. serpentinite, diabase) and metamorphic 222 rock fragments (e.g. muscovite schist). Rare benthic and planktic foraminiferal fragments are also 223 present (McCay & Robertson 2012). 224 Mia Milia (Dağyolu) Formation 225 Sample GC14-36 (GPS: 35°18′52″ N, 33°43′50″ E) was collected from a thick-bedded sandstone in 226 the higher levels of the Middle-Late Miocene Mia Milia (Dağyolu) Formation, near Arıdamı (Artemi) 227 (Fig. 7). The sandstone comprises relatively well-sorted grains of quartz, igneous lithic fragments 228 and carbonates. Metamorphic lithic grains (e.g. muscovite schist) occur in small amounts, together 229 with rare opaque grains (McCay & Robertson 2012). 230 231 Geochronological results

232 Mamonia Complex & Moni Melange

233 Vlambouros Formation 234 Zircons are abundant, varying in size and opacity. The grains range from rounded to stubby prisms 235 and slightly elongate prisms (e.g. Fig. 8a: grains 25, 54 and 83; Fig. 8b: grains 8-9, 39-41). 236 Individual zircon crystals vary in length from 70-200 μm. Most zircons exhibit oscillatory zoning in 237 CL images (e.g. Fig. 8a: grains 25, 37, 49 and 83; Fig. 8b: grains 40, 43 and 65) but a few lack 238 compositional zoning or show patchy zoning (e.g. Fig. 8a: grains 15 and 53; Fig. 8b: grains 39, 46 239 and 57). Inherited cores occur rarely (e.g. Fig. 8a: grain 12; Fig. 8b: grain 8). 240 In sample GC14-3, most zircons have relatively high Th/U ratios (>0.1) (see supplementary 241 material Table S1), suggesting a magmatic derivation (Rubatto 2002; Teipel et al. 2004). Lower 242 Th/U ratio (Th/U<0.1) occur in three grains, together with relatively dark CL images showing 243 metamict cores (Fig. 8a: grains 12 and 46) and faint internal structures (Fig. 8a: grain 43). 244 Concordance-filtered (90-110%) zircon ages indicate a polymodal age distribution, with major 245 groups of 548-635 Ma (Ediacaran; 14%), 637-691 Ma (Cryogenian; 14%), 724-999 Ma (Tonian; 246 36 %), 1037-1188 Ma (Stenian; 6%), 1839-2020 Ma (Orosirian; 9%) and 2512-2745 Ma 247 (Neoarchean; 9%) (Fig. 9a-b). 1.2-1.8 Ga-aged zircons are represented by only two grains (1240 and 248 1409 Ma, respectively). An age gap of 2.1-2.5 Ga is observed (Fig. 9b; see supplementary material 249 Figure S1), with one exception (grain 72), with an age of 2151 Ma. The youngest concordant zircon 250 grain is subhedral (Fig. 8a: grain 25), with a 206Pb/238U age of c. 320 Ma (mid-Carboniferous). 251 Zircons from sample GC14-9 mainly have high Th/U ratios (>0.14) (see supplementary material 252 Table S1), with the exception of grains 47 and 57 (Th/U=0.02-0.03) that have homogeneous dark CL 253 images (Fig. 8b). The population age ranges are 505-537 Ma (Cambrian; 10%), 549-630 Ma 254 (Ediacaran; 15%), 639-705 Ma (Cryogenian; 10%), 759-987 Ma (Tonian; 33%) and 1009-1095 Ma 255 (Stenian; 15%) (Fig. 9c-d). Comparable age gaps of c. 1.1-1.8 Ga and 2.1-2.6 Ga are present in this 256 sandstone (Fig. 9d) (see supplementary material Figure S1), other than grains 83 (1.66 Ga), 85 (2.21 257 Ga) and 3 (2.42 Ga) (see supplementary material Table S1). The youngest relatively concordant age 258 is 525 Ma (Cambrian; Fig. 8b: grain 46).

259 Akamas Member 260 Sample (GC14-16) contains abundant zircons that are mostly subhedral to subrounded and variably 261 sized (100-250 μm). CL images (Fig. 8c) exhibit various internal structures, including core-mantle 262 structure (e.g. Fig. 8c: grains 1, 88), banded zonation (Fig. 8c: grain 39) and common oscillatory 263 zoning (Fig. 8c: grains 8, 21). Most grains have Th/U ratios of >0.1 (see supplementary material 264 Table S1), with two exceptions; of these, grain 42 has a dark, irregular inherited core (i.e. metamict), 265 whereas grain 88 has a bright, sub-rounded inherited core with a dark structureless rim (Fig. 8c). 266 Concordance-filtered (90-110%) zircon populations cluster mainly in the Neoproterozoic, with 267 components of 578-633 Ma (Ediacaran; 27%), 636-713 Ma (Cryogenian; 29%), 725-1000 Ma 268 (Tonian; 32%) and 1018-1094 Ma (Stenian; 7%) (Fig. 10a-b). Smaller age groups occur at 2560- 269 2607 Ma (Neoarchean; 2%). The youngest 100% concordant age is 588 Ma (Ediacaran). Only one 270 grain (no. 17; 2034 Ma) is in the c. 1.1-2.5 Ga range (Fig. 10b).

271 Pareklisia Member (Moni Melange) 272 The zircons are 80-250 μm long, subhedral (e.g. Fig. 8d: grains 3, 40) to rounded (e.g. Fig. 8d: grain 273 59). Most grains exhibit igneous-derived oscillatory zonation (e.g. Fig. 8d: grains 3, 87) (Corfu et al. 274 2003). Core-mantle structures are common, with various internal patterns and colours (e.g. Fig. 8d: 275 grains 27, 82). Inherited protolith cores are generally surrounded by concentric pale to dark-grey 276 rims (e.g. Fig. 8d: grain 86). Common rounding is inferred to have resulted from abrasion during 277 long-distance sedimentary transport or sedimentary recycling (e.g. Corfu et al. 2003; Ustaömer et al. 278 2013). The zircons (90-110% concordant) group at 571-633 Ma (Ediacaran; 25%), 638-719 Ma 279 (Cryogenian; 27%), 766-981 Ma (Tonian; 25%) and 1004-1126 Ma (Stenian; 13%) (Fig. 10c-d). The 280 youngest 100% concordant age is 630 Ma (Ediacaran). There is a wide age gap from c. 1.1 Ga to 2.6 281 Ga (Fig. 10d; see supplementary material Figure S1), other than a 2.0 Ga for one grain (no. 88; see 282 supplementary material Table S1).

283 Comparison of zircon populations 284 The Mamonia Complex and Moni Melange sandstones are dominated by Late Neoproterozoic zircon 285 populations. Ediacaran-Cryogenian and Tonian-Stenian zircon populations dominate the sandstones 286 of the Vlambouros Formation, specifically. The sandstone of the Akamas Member has similar but 287 more age-restricted zircon populations (Figs. 9-10; see supplementary material Figure S1). The 288 sandstones of the Pareklisia and Akamas Member share similar Late Neoproterozoic and Tonian- 289 Stenian zircon populations. Zircon populations of c. 1.1-1.8 Ga and c. 2.0-2.5 Ga are absent in both 290 units, although a few grains lie within these age ranges (Fig. 9-10; see supplementary material Figure 291 S1). Minor Paleozoic zircon populations in sandstones of the Vlambouros Formation mainly cluster 292 in the Cambrian, together with sparse zircons of Ordovician, Devonian, Carboniferous and Permian 293 ages. Of these, 13 out of 32 grains have reliable (90-110%) concordance levels.

294 Kyrenia Range

295 Kiparisso Vouno (Alevkaya Tepe) Member 296 Zircon grains range from mainly subhedral to subrounded to rounded, and range from 50 to 230 μm 297 long. CL images reveal detrital cores, generally enclosed by concentric oscillatory zonation (Fig. 8e: 298 grains 2 and 4). The zircons typically have relatively high Th/U ratios (>0.1; see supplementary 299 material Table S1), consistent with an igneous origin (Rubatto 2002; Teipel et al. 2004). A single 300 zircon has a Th/U ratio of 0.01 (no. 103; see supplementary material Table S1), suggestive of a 301 metamorphic origin (e.g. Rubatto 2002). Concordant ages dominantly group at 551-615 Ma 302 (Ediacaran; 13%), 646-702 Ma (Cryogenian; 8%), 729-1091 Ma (Tonian-Stenian; 25%), 1849-2045 303 Ma (Orosirian; 13%) and 2542-2701 Ma (Neoarchean; 9%) (Fig. 11a-b). Paleozoic zircons (<541 Ma; 304 36 grains) mainly cluster in the Carboniferous (312-346 Ma), Late Silurian (c. 422 Ma) and 305 Ordovician (451-475 Ma); of these, six grains provide highly reliable 97-103% concordant ages (Fig. 306 11a-b; see Discussion). There is also a minor c. 98% concordant Late Cretaceous (87 and 95 Ma) 307 fraction (Fig. 8e: grain 4). The youngest 100% concordant zircon is Ordovician (461 Ma). There is a 308 large age gap from 1.1 to 1.8 Ga, and a small age gap between c. 2.1-2.5 Ga (with only 3 concordant 309 ages) (Fig. 11b; see supplementary material Figure S1).

310 Kalograia-Ardana (Bahçeli–Ardahan) Formation 311 Zircon crystals are mainly rounded to subrounded to subhedral, from 40-300 μm long. Core-mantle 312 structure and oscillatory zoning are seen in most CL images (e.g. Fig. 8f: grains 3, 12, 56 and 80). 313 Inherited cores are generally surrounded by a pale-grey rim with concentric zoning or weak zoning 314 (e.g. Fig. 8f: grains 3, 74). The zircons typically have relatively high Th/U ratios, ranging from 0.14- 315 2.74 (see supplementary material Table S1), suggesting a magmatic origin (Rubatto 2002). A single 316 rounded grain with a low Th/U ratio (Th/U=0.04) has an irregular dark, inherited core and a pale- 317 grey, unzoned outer rim (Fig. 8f: grain 74), indicative of a metamorphic event (e.g. Rubatto 2002; 318 Corfu et al. 2003). Concordant (90-100%) ages of significant zircon populations range from 559-620 319 Ma (Ediacaran; 15%), 647-705 Ma (Cryogenian; 10%), 753-999 Ma (Tonian; 22%) and 1040-1140 320 Ma (Stenian; 7%), with age gaps from c. 1.1-2.1 Ga and 2.2-2.7 Ga (Fig. 11c-d; see supplementary 321 material Figure S1). There are also trace, to minor, zircon fractions with Paleozoic (311-363 Ma; 322 Late Devonian-Late Carboniferous), Mesozoic (219-232 Ma; Triassic and 87-94 Ma; Late 323 Cretaceous) and Cenozoic (61 Ma; Paleocene and 45 Ma; Eocene) ages (Fig. 11c). The youngest 324 100% concordant age is 45 Ma (Eocene) (Fig. 8f: grain 56).

325 Davlos (Kaplıca) Formation 326 Detrital zircons are mostly colourless or brownish, euhedral to rarely subhedral or rounded (e.g. Fig. 327 8g: grain 13), ranging from 130-250 μm in length. CL images reveal common oscillatory zoning (e.g. 328 Fig. 8g: grains 1, 7 and 11) suggesting a magmatic origin (Corfu et al. 2003); other zircons have 329 inherited, irregular cores and concentrically zoned or structureless rims (e.g. Fig. 8g: grains 22, and 330 30). Th/U ratios are typically >0.15 (see supplementary material Table S1), consistent with an 331 igneous origin (e.g. Rubatto 2002). Concordant zircons are characterised by ages of 71-91 Ma (Late 332 Cretaceous; peaks of 74 and 84 Ma; 83% of total), with minor fractions of 689-1017 Ma 333 (Neoproterozoic; 10%), c. 51 Ma (Eocene; 2%) and c. 21 Ma (Miocene; 2%) (Fig. 12a-b; see 334 supplementary material Figure S1). The youngest 100% concordant zircon age is 74 Ma (Late 335 Cretaceous; Fig. 8g: grain 30).

336 Mia Milia (Dağyolu) Formation 337 Most zircons are euhedral (Fig. 8h) and 120-280 μm in length. Core-mantle structure is common; 338 where present, inherited cores are rimmed by fine oscillatory zonation (e.g. Fig. 8h: grains 5, 6), or 339 dark structureless zircon (e.g. Fig. 8h: grain 3). Th/U ratios are >0.1 (see supplementary material 340 Table S1), suggesting an igneous origin (e.g. Rubatto 2002). Only six dateable zircon grains could 341 be extracted, yielding ages of 13-16 Ma (Miocene), 24-25 Ma (Oligocene) and 558-813 Ma 342 (Ediacaran-Tonian) (Fig. 12c-d). None of these zircons have 100% concordance. The youngest age is 343 13 Ma (Serravallian) (grain 3; Fig. 8h).

344 Comparison of zircon populations 345 The Kyrenia Range sandstones are characterised by Ediacaran-Cryogenian and Paleoproterozoic 346 zircons, with a minor fraction of Tonian-Stenian ages. Paleozoic, Mesozoic and Cenozoic zircon 347 populations generally increase in sandstones of younger depositional age (Figs. 11-12; see 348 supplementary material Figure S1). Late Cretaceous (Turonian-Campanian) zircons form a 349 significant age population in the Cenozoic sandstones. Cenozoic zircons are rarely present in the 350 Eocene and Late Miocene sandstones. Age gaps of c. 1.1-2.1 Ga and 2.2-2.7 Ga exist in the Late 351 Cretaceous and Eocene samples (see supplementary material Figure S1), in contrast to the Late 352 Miocene one, although few grains were analysed in these sandstones. 353 354 Discussion

355 Depositional age based on zircon geochronology 356 After formation and cooling by igneous or metamorphic processes, detrital zircons were eroded, 357 transported and deposited to form the sandstones studied. For extrusive igneous rocks this requires 358 only erosion and deposition. However, for intrusive igneous rocks and metamorphic rocks, variable 359 exhumation is required prior to erosion and deposition (e.g. Gray & Zeitler 1997; Bernet et al. 2004; 360 Chew et al. 2007). Similar paleontologically determined and radiometrically determined ages for 361 intrusive and metamorphic rocks suggest rapid exhumation, erosion and deposition (e.g. Ghiglione et 362 al. 2015; Sickmann et al. 2018). 363 The youngest valid (highly concordant) detrital zircon ages from the sandstones can be usefully 364 compared with the paleontologically determined ages of the interbedded finer-grained sediments (Fig. 365 13): (1) The youngest 100% concordant ages of the Vlamborous Formation sandstones are mid- 366 Carboniferous (320 Ma; GC14-3) and Cambrian (525 Ma; GC14-9) and, therefore, have little 367 bearing on the paleontologically determined Late Triassic age, based mainly on the presence of the 368 pelagic bivalve Halobia sp. and Radiolaria (Ealey & Knox 1975; Lapierre 1975; Robertson & 369 Woodcock 1979; Bragin & Krylov 1996; Bragin 2007); (2) Similarly, the youngest 100% concordant 370 age of the overlying Akamas Member sandstone (GC14-16) is Ediacaran (588 Ma), compared to the 371 Late Jurassic-Early Cretaceous depositional age based on Radiolaria (Bragin & Krylov 1996, 1999; 372 Bragin 2007); (3) The youngest 100% concordant age of the sandstone represented by Pareklisia 373 Member is Ediacaran (630 Ma). Organic carbon-rich mudstones interbedded with the sandstones are 374 tentatively dated as Early Cretaceous based on sporomorphs (Robertson 1977). Also, the clay-rich 375 matrix of the Moni Melange has been dated as Late Cretaceous using Radiolaria (Urquhart & Banner 376 1994); (4) In marked contrast, the Kiparisso Vouno (Alevkaya Tepe) Member in the Kyrenia Range 377 contains a youngest acceptable (c. 98% concordant) detrital zircon age of 87 Ma (Coniacian) and 95 378 Ma (Cenomanian). This unit is dated as Maastrichtian based on planktic foraminifera within 379 interbedded pelagic limestones (Baroz 1979; Robertson et al. 2012b). Detrital zircons, of inferred 380 igneous origin, crystallised, eroded and were deposited, all during Late Cretaceous time, indicating a 381 rapid succession of tectonic-magmatic events; (5) The 100% youngest concordant age of the 382 Kalograia-Ardana (Bahçeli–Ardahan) Formation is Middle Eocene (45 Ma). Planktic foraminifera 383 from hemipelagic marl in the lower to mid parts of the succession indicate a similar, Middle Eocene 384 age (Baroz 1979; Robertson et al. 2014), showing that magmatic cooling, exhumation, erosion and 385 deposition again all took place rapidly; (6) For the Davlos (Kaplıca) Formation, the 100% youngest 386 concordant detrital zircon ages are Campanian (74 Ma). Tortonian (c. 10 Ma) and Serravallian (c. 12 387 Ma) zircons have 77% and 120% concordance levels, respectively. The depositional age of this 388 formation is Tortonian based mainly on planktic foraminifera (Baroz 1979); and (7) The Mia Milia 389 (Dağyolu) Formation is dated as Burdigalian-Tortonian based on combined planktic foraminifera and 390 nannofossil dating (Baroz 1979; Hakyemez et al. 2000; McCay et al. 2013). 391 Summarising, there is no evidence of rapid (several Ma) recycling of zircons in the Mamonia 392 Complex sedimentary succession or in the Moni Melange detached blocks (Pareklisia Member), both 393 of which are interpreted as parts of a rifted Mesozoic passive margin succession (e.g. Robertson 394 1977; Robertson & Woodcock 1979; Torley & Robertson 2018). Detrital zircons in passive margin 395 successions generally lack syn-depositional magmatism and are therefore dominated by older detrital 396 grains (e.g. Cawood et al. 2012). In contrast, detrital zircons in active margin successions commonly 397 exhibit similar-aged magmatism, as observed for the Late Cretaceous-Miocene sandstones of the 398 Kyrenia Range.

399 Zircon provenance

400 Late Precambrian 401 The Late Precambrian zircon populations can be compared to the radiometrically determined ages of 402 the Amazonia, Baltica, Siberia, West Africa, Arabian-Nubian Shield and Saharan cratonic provinces 403 (Fig. 14). Amazonia-derived terranes (microplates) in northern South America (e.g. Tassinari & 404 Macambira 1999) are characterised by several-aged populations: i.e. 0.9-1.1 Ga (Tonian-Stenian) 405 related to the Grenvillian orogeny, and also Mesoproterozoic (~1.5 Ga) and Paleoproterozoic (1.7- 406 2.2 Ga), both related to the Rondonian orogeny (Fig. 14; Tassinari & Macambira 1999; Linnemann 407 et al. 2004; Winchester et al. 2006; Nance et al. 2008; Drost et al. 2011). The absence of significant 408 Mesoproterozoic and Paleoproterozoic zircon populations is inconsistent with derivation from 409 Amazonia. Baltican provenance is characterised by an undifferentiated (continuous) age population 410 of 900-3200 Ma, with a large gap between 550 and 750 Ma (e.g. Hartz & Torsvik 2002; Linnemann 411 et al. 2004; Nance et al. 2008). The prominent Late Neoproterozoic zircon population in the 412 sandstones therefore opposes a Baltican provenance (Fig. 14). The Siberia Craton can also be ruled 413 out in view of its Late Neoproterozoic magmatic quiescence (e.g. Meert & Torsvik 2003; Sunal et al. 414 2008). The W Africa Craton is characterised by several orogenic events resulting in zircon groupings 415 at 500-750 Ma (Pan-African orogeny; Liégeois et al. 1994), 2.0-2.2 Ga (Eburnean orogeny; 416 Abouchami et al. 1990; Liégeois et al. 1994), ~2.7 Ga (Liberian orogeny; Hurley et al. 1971) and 417 3.1-3.3 Ga (Leonian orogeny; Beckinsale et al. 1980; Linnemann et al. 2004). The prominent 418 Tonian-Stenian zircon population in the sandstones (Fig. 14) contrasts with the known 0.8-1.7 Ga 419 magmatic quiescence in the W Africa Craton (e.g. Liégeois et al. 1994). 420 The dominant Neoproterozoic zircon populations are, instead, compatible with a NE 421 Africa/Arabian-Nubian Shield origin. Predominant Neoproterozoic zircon populations in NE Africa 422 and the Arabian-Nubian Shield (Avigad et al. 2003; Kolodner et al. 2006; Drost et al. 2011) group at 423 550-650 Ma, reflecting voluminous plutonic and volcanic rocks of this age within this region (e.g. 424 Bentor 1985; Stern 1994). Subordinate pre-Neoproterozoic zircons populations of Tonian-Stenian, 425 1.65-1.85 Ga and c. 2.5 Ga are consistent with derivation from central Africa (Cahen et al. 1984), 426 southeast Africa (Kröner et al. 2001), the Saharan Metacraton (Abdelsalam et al. 2002), and/or the 427 Afif terrane of southeast Saudi Arabia (Stacey & Hedge 1984) (Fig. 2). The corresponding Pre- 428 Neoproterozoic zircons in the Late Triassic sandstones scatter around a comparable time span (Fig. 429 14), although without significant zircon populations. In the Saharan Metacraton, zircon ages in the 430 basement ranges from 1.65-2.7 Ga, with a further orogenic event around 1.0 Ga (Abdelsalam et al. 431 2002; Linnemann et al. 2004) (Fig. 14). The absence of significant Paleoproterozoic zircon 432 populations in the sandstones opposes a Saharan Metacraton origin. However, Cambrian and 433 Ordovician sandstones from Jordan, peripheral to the Arabian-Nubian Shield, have similar 434 Precambrian-aged zircon populations to the samples studied (Kolodner et al. 2006) (Figs. 2, 14). 435 The zircon age data indicate an ultimate origin related to Gondwana. However, during Late 436 Permian-early Mesozoic time, fragments of Gondwana rifted and drifted northwards to open the 437 Southern Neotethys (Şengör & Yılmaz 1981; Robertson & Dixon 1984; Stampfli & Borel 2002; 438 Göncüoğlu et al. 2003). Consistent with this interpretation, Gondwana-derived zircons exist in the 439 Taurides to the north of Cyprus (e.g. Ustaömer et al. 2012, 2018; Zlatkin et al. 2013; Abbo et al. 440 2015). The occurrence of Gondwana-derived zircons in both the Vlamborous Formation and the 441 Pakeklisia Member sandstones cannot therefore be used to indicate the paleogeographic source 442 during the Late Triassic and Early Cretaceous when these lithologies accumulated. Sedimentological 443 evidence has, however, established close similarities between the sedimentary and volcanic rocks of 444 the Ayios Photios Group (Mamonia Complex) and the Isparta Angle area of SW Turkey (Taurides) 445 suggesting derivation from the north or northwest of the present outcrops in Cyprus (Robertson, 446 2000; Torley & Robertson, 2018) (Fig. 2). Specifically, the Lower Paleozoic siliciclastic cover of the 447 Menderes Massif in western Turkey (Zlatkin et al. 2013) and the Paleozoic to Triassic siliciclastic 448 rocks of the Karacahisar dome in the Taurides (Abbo et al. 2015) both contain Gondwana-derived 449 zircons. The zircon grains in the Triassic and Early Cretaceous Cyprus sandstones are likely to have 450 been recycled from Paleozoic sedimentary successions of southern and central Turkey (Fig. 15). 451 Paleozoic 452 For time periods prior to the Permo-Triassic rifting of the Southern Neotethys, any zircons with 453 Gondwanan signatures, in principle, could have been derived directly from the NE Africa/Arabian- 454 Nubian Shield, or from Turkey to the north. Paleozoic zircons (<540 Ma) constitute a trace to minor 455 fraction of the sandstones analysed, except for the Late Miocene sandstone of the Kyrenia Range 456 (although this could be an artefact of limited analysis). Although poorly concordant, the oldest of 457 these zircon populations (Ediacaran-Early Cambrian) is similar to that of granitic arc rocks in the 458 Bitlis Massif of southeast Turkey (Ustaömer P. A. et al. 2009, 2012a) (Fig. 2). Prominent zircon 459 populations of Early Cambrian, Late Neoproterozoic and Tonian-Stenian ages in this area are again 460 suggestive of an Arabian-Nubian Shield origin (Ustaömer P. A. et al. 2009, 2012a). The prolonged 461 Ediacaran-Early Cambrian age is likely to record Andean-type magmatism along the northern margin 462 of Gondwana in the Eastern Mediterranean region (Ustaömer P. A. et al. 2009). Zircons of Early 463 Cambrian (~500-550 Ma) age could represent either circum-Gondwana convergent magmatism or 464 late Pan-African amalgamation of the Gondwana continent. 465 The second-oldest Paleozoic zircon population includes detrital zircons of Ordovician- 466 Carboniferous age with peaks during Middle Ordovician, Late Silurian and mid-Carboniferous times. 467 Ordovician magmatism (specifically Middle Ordovician) is known in the Armutlu Peninsula and also 468 in the Tavşanlı zone (Orhaneli region), both in NW Turkey (Okay 2002; Okay et al. 2008a, b; Özbey 469 et al. 2013) (Fig. 2). The Silurian magmatism implied by the zircon ages could be represented by the 470 known bimodal volcanism along the northern margin of the Tauride-Anatolide platform (Göncüoğlu 471 & Kozlu 2000; Eren et al. 2004). Only minor local volcanic activity (pre-Late Permian) is known in 472 the Antalya (SW Taurides) and Feke (E Taurides) regions (Göncüoğlu & Kozlu 2000) (Fig. 2). The 473 Carboniferous of the northern margin of the Anatolide-Tauride block (e.g. Afyon zone; Konya area) 474 (Fig. 2) is characterised by a melange (Konya Melange) that includes terrigenous-derived siliciclastic 475 sandstones, Late Paleozoic shallow-water carbonates, Silurian-Devonian black chert and 476 Carboniferous-aged subduction-influenced volcanic rocks (Robertson & Ustaömer 2009a, b, 2011). 477 Carboniferous granites were recently reported from the Afyon zone elsewhere (Candan et al. 2016). 478 Carboniferous volcanic rocks are also documented in the Sultan Dağ area of the Tauride platform 479 (Göncüoğlu et al. 2007; Mackintosh & Robertson 2012) (Fig. 2). In one hypothesis, all of the above 480 units are related to magmatism and tectonic accretion along northern margin of the Anatolide- 481 Tauride continental block that rifted from Gondwana during Late Permian-Late Triassic time 482 (Göncüoğlu et al. 2003; Robertson & Ustaömer 2009a). In an alternative hypothesis (Stampfli & 483 Borel, 2002), zircons associated with the Anatolide crustal block (e.g. Afyon zone; Konya area) were 484 partly derived from the Pontides farther north, requiring Gondwana-derived crust to have accreted to 485 Eurasia during the Paleozoic. 486 Carboniferous magmatism is also well-documented in the Pontides of northern Turkey. For 487 some authors, this Carboniferous magmatism was related to northward subduction to create a south- 488 Laurasian continental margin magmatic arc during the Variscan orogeny (Stampfli & Borel 2002; 489 Topuz et al. 2010; Ustaömer P. A. et al. 2012b; Ustaömer et al. 2013; Okay & Nikishin 2015). 490 Alternatively, others infer southward subduction and formation of a major continental margin arc 491 (Sakarya crustal unit) adjacent to the northern margin of Gondwana (Şengör & Yılmaz 1981; Yılmaz 492 et al. 1997; Göncüoğlu et al. 2000). 493 Zircons with ages indicative of a north-Gondwana derivation have also been reported from 494 Paleozoic sandstones of the Pontides, including the pre-Lower Carboniferous meta-sedimentary 495 schists of the Central Sakarya Basement, western Pontides (Ustaömer P. A. et al. 2012b), the Mid- 496 Devonian and early Carboniferous Karadağ paragneiss and the Ordovician to early Carboniferous 497 Narlık schist, eastern Pontides (Ustaömer et al. 2013). These Pontide meta-sandstones are interpreted 498 to have been derived from crustal units that rifted from Gondwana, drifted across Paleotethys and 499 accreted to Eurasia during the Paleozoic, prior to the rifting of the Southern Neotethys during Permo- 500 Triassic time (e.g. Ustaömer et al. 2013). However, some authors reposition these crustal units 501 adjacent to the northern margin of the Anatolide crustal block, as noted above (Şengör & Yılmaz 502 1981; Yılmaz et al. 1997; Göncüoğlu et al. 2000). In the absence of agreement on the regional 503 tectonic setting, the source of the Carboniferous magmatism represented in the Cyprus sandstones 504 analysed remains an open question (see Ustaömer et al. 2014, 2016a; Ustaömer P. A. et al. 2014).

505 Mesozoic 506 Extensive Triassic rift-related magmatism is documented from the Mamonia Complex (Dhiarizos 507 Group), SW Cyprus (Lapierre 1975; Robertson & Woodcock 1979; Chan et al. 2008) and in the 508 Antalya Complex (Gödene Zone), SW Turkey (Juteau 1975; Robertson & Woodcock 1981a, b, c). 509 Triassic, rift-related volcanic rocks (mostly evolved) also occur widely in the more northerly-derived 510 Beyşehir-Hoyran-Hadim Nappes, central Taurides (Fig. 2) (Özgül 1984; Andrew & Robertson 2002). 511 Stratigraphic evidence from the central Taurides (e.g. Hadim and Bolkar nappes) suggests that rifting 512 began during the Late Permian (Mackintosh & Robertson 2012). The rare Permian zircons within the 513 Cyprus sandstones are therefore interpreted to reflect rift-related magmatism in southern Turkey, 514 although magmatic rocks of this age are poorly known. Only the Eocene sandstones of the Kyrenia 515 Range were observed to contain Triassic zircons during this study (Fig. 11d). The Triassic igneous 516 rocks in W Cyprus (Dhiarizos Group; Mamonia Complex) formed in a relatively distal (oceanic) 517 setting and were therefore unavailable as a source for more proximal rift and passive margin 518 sediments (i.e. Ayios Photios Group; Mamonia Complex). In contrast, the Eocene sandstones of the 519 Kyrenia Range accumulated in a foredeep setting, derived from deformed lithologies, including 520 Triassic rift-related sandstones, as widely exposed in the Taurides farther north (e.g. Antalya 521 Complex) (Robertson & Woodcock 1984). 522 Late Cretaceous (71-95 Ma) zircons characterise the Late Cretaceous-Neogene sandstones of 523 the Kyrenia Range. Occasional Turonian-Coniacian (86-94 Ma) zircon grains are present, with Th/U 524 ratios (>0.1) and typical zoning structures of igneous rocks (Rubatto 2002; Corfu et al. 2003; Teipel 525 et al. 2004). These sandstones contain abundant, well-mixed detritus that, taken together, includes 526 serpentinite, variably recrystallised radiolarian chert/shale and minor amounts of basalt/diabase, 527 which are indicative of an ophiolite-related origin (McCay & Robertson 2012; Robertson et al. 528 2012b, 2014). Supra-subduction zone (SSZ)-type ophiolites that overlie the Tauride platform in 529 southern Turkey (e.g. Antalya, Beyşehir and Mersin areas; Fig. 2) have yielded similar Late 530 Cretaceous radiometric ages (~85-95 Ma) (e.g. Parlak & Delaloye 1999; Çelik et al. 2006; Karaoğlan 531 et al. 2012, 2013a). The Mersin ophiolite and related accretionary melange (Parlak & Robertson 532 2004; Robertson et al. 2012a) are the nearest appropriate units to have supplied the Late Cretaceous 533 zircons within the Late Cretaceous-Neogene sandstones of the Kyrenia Range, although the exact 534 source remains uncertain. 535 The abundant Santonian-Campanian-aged zircons (73-86 Ma) in the Kyrenia Range sandstones 536 (e.g. Davlos (Kaplıca) and the Mia Milia (Dağyolu) Formations) are likely to have a source area to 537 the east, as inferred from generally westward paleocurrents in these sandstones (Weiler 1970; McCay 538 & Robertson 2012). There are two main c. NE-SW trending belts of ophiolitic rocks of Late 539 Cretaceous age (c. 84-92 Ma) in SE Turkey and N Syria. The southerly one is characterised by a 540 chain of ophiolites and related accretionary melange. These include the Baer-Bassit ophiolite (Al- 541 Riyami et al. 2002) in northern Syria, the Hatay ophiolite (Boulton & Robertson 2007; Karaoğlan et 542 al. 2012, 2013a), the Amanos ophiolite (Duman et al. 2017) and the Koçali ophiolite (Robertson et 543 al. 2016), which are located in southern Turkey or northernmost Syria (Fig. 2). Some areas of SE 544 Turkey (e.g. Göksun–Afşin (Kahramanmaraş), Doğanşehir (Malatya) and Baskil (Elazığ) regions) 545 include subduction-related granitic rocks (77-85 Ma) (e.g. Aktaş & Robertson 1990; Parlak 2006; 546 Rızaoğlu et al. 2006, 2009; Robertson et al. 2007) (Fig. 2). The nearest appropriate source is the 547 combined Hatay and Amanos ophiolites. In summary, any of the above Late Cretaceous ophiolitic or 548 arc-related igneous rocks of SE Turkey are potential sources of the Santonian-Campanian zircons in 549 the Kyrenia Range. 550 Cenozoic 551 Traces of Paleocene, Eocene and Miocene-aged zircons occur in the Eocene and Miocene sandstones 552 of the Kyrenia Range. Convergence of the African and Eurasian plates took place during Late 553 Cretaceous-Cenozoic time, related to northward subduction of the Southern Neotethys (Livermore & 554 Smith 1985; Savostin et al. 1986; Barrier et al. 2018). In the Kyrenia Range, Maastrichtian-Early 555 Eocene within-plate-type basalts (with a local subduction influence) are interpreted to represent an 556 extensional setting related to on-going development of the inferred South Neotethyan active 557 continental margin (Robertson & Woodcock 1986; Huang et al. 2007; Chen 2018). 558 The Paleogene volcanism represented by the Ayios Nikolaos (Yamaçköy) Formation in the 559 Kyrenia Range rarely extended into the Early Eocene, based on planktic foraminiferal dating of 560 interbedded pelagic carbonates in the eastern range (Robertson et al. 2012b). The Early Eocene 561 zircons in the overlying sandstone turbidites (Kalograia-Ardana (Bahçeli–Ardahan) Formation) 562 might therefore have been derived from local coeval volcanism in the Kyrenia Range. However, the 563 sedimentology and petrography of these sandstones point to a more distal source, which included 564 abundant ophiolitic detritus (especially serpentinite and boninite) and also radiolarian chert 565 (Robertson et al. 2014). These Eocene sediments accumulated in a foredeep during continued 566 development of the South-Neotethyan active continental margin, with sediment supply mainly from 567 the north (Robertson et al. 2014). Northward subduction of Southern Neotethys (Aktaş & Robertson 568 1990; Elmas & Yılmaz 2003; Robertson et al. 2012b) gave rise to widespread subduction-related, 569 andesitic volcanism (e.g. Helete Formation) in SE Turkey, as documented from a thrust belt 570 overlying the northern margin of the Arabian platform (Robertson et al. 2006; Karaoğlan et al. 571 2013b; Nurlu et al. 2016). Paleocene volcanogenic rocks are also exposed farther north, along the 572 northern margin of the Anatolide-Tauride, specifically in the Ulukışla Basin (Clark & Robertson 573 2002) (Fig. 2), although this remote area is a less likely source. 574 Late Oligocene zircons occur in the Miocene sandstone of the Kyrenia Range. Oligocene 575 volcanics (Gövelek unit) occur in the Lake Van area, SE Turkey (Robertson et al. 2006; Oyan 2018) 576 (Fig. 2), although this is c. 900 km to the east of Cyprus, suggesting that a more local source remains 577 to be identified. 578 Miocene zircons are likely to have been supplied by local reworking of tuffaceous layers within 579 the nearby Panagra (Geçitköy) Formation (c. 19.8 Ma) in the Kyrenia Range (Baroz 1979; Chen 580 2018). Accumulation as air-fall tuff is supported by the relatively euhedral shape of the zircons. The 581 probable source of the tuff was Early Miocene rhyolitic and tuffaceous volcanism to the northwest, 582 within the Isparta Angle (SW Turkey) (Yağmurlu et al. 1997; Dilek & Altunkaynak 2010; Seghedi & 583 Helvacı 2016) (Fig. 2). Miocene volcanics of the Amanos Mountain to the northeast are unlikely to 584 have been a source because these are mainly basic to intermediate-composition lava flows rather than 585 tuffs (Robertson et al. 2006; Duman et al. 2017) (Fig. 2). Miocene collision-related volcanism occurs 586 in eastern Turkey (i.e. Eastern Anatolian Volcanic Province; Innocenti et al. 1982; Pearce et al. 587 1990), but as noted above this area is too far away to represent a realistic source.

588 Implications for tectonic reconstructions 589 The dominance of Ediacaran-Cryogenian and Tonian-Stenian detrital zircon populations is indicative 590 of ultimate derivation from the NE Africa/Arabian-Nubian Shield (Figs. 15-16; see above). During 591 the Late Permian-Early Jurassic the Tauride continental units rifted from North Africa giving rise to 592 several microcontinental units to the north of Cyprus, as noted above (e.g. Robertson & Woodcock 593 1984; Göncüoğlu et al. 2003; Garfunkel 2004; Robertson et al. 2009; Ustaömer et al. 2016b; Barrier 594 et al. 2018). By the time that the first MORB (mid-ocean ridge basalt) appeared in western Cyprus, 595 represented by the Dhiarizos Group (Mamonia Complex) (Fig. 4), any Precambrian zircons could 596 have either a southerly source (NE Africa/Arabian-Nubian Shield) or a northerly source (rifted away 597 Gondawan crust) (Fig. 15). 598 The facies and age of the sedimentary and igneous rocks of the Mamonia Complex are 599 markedly similar to those of the Antalya Complex within the Isparta Angle (SW Taurides) to the 600 northwest (Robertson & Woodcock 1981a, b, c) (Fig. 2). The western limb of the Isparta Angle, 601 today continues southwards offshore as the submarine Anaximander Mountains (Zitter et al. 2003). 602 This crust could represent the hinterland of the Mamonia Complex during the Mesozoic (Clube & 603 Robertson, 1986; Torley & Robertson 2018). A related study of Triassic sandstones associated with 604 the Tauride continental block (Ustaömer et al. 2014, 2016a, 2018; Ustaömer P. A. et al. 2014) 605 identifies possible source areas within Paleozoic shallow-marine shelf successions, including 606 Devonian-Triassic quartz-rich sandstones of the Hadim and Bolkar Nappes (central Taurides) (Özgül 607 1984; Mackintosh & Robertson 2012) (Fig. 2). These lithologies are interpreted to have been derived 608 from local basement highs of Late Precambrian age (Göncüoğlu et al. 2003; Mackintosh & 609 Robertson 2012), notably the Sandıklı Basement Complex (Fig. 2). The lithologies include Late 610 Precambrian-Cambrian low-grade meta-sedimentary rocks and siliceous volcanic rocks (Gürsu et al. 611 2004; Ghienne et al. 2010). A northerly derivation is inferred for the Late Triassic and Early 612 Cretaceous sandstones of the Mamonia Complex after rifting of the Southern Neotethys, despite their 613 ultimate derivation from Gondwana (Figs. 15, 16). The Ediacaran-Cryogenian and Tonian-Stenian 614 zircon populations in the sandstones of the Eocene Kalograia-Ardana (Bahçeli–Ardahan) Formation, 615 the Late Miocene Davlos (Kaplıca) Formation and the Middle to Late Miocene Mia Milia (Dağyolu) 616 Formation of the Kyrenia Range are also likely to have been recycled from Paleozoic siliciclastic 617 sedimentary rocks within Anatolia, with initial derivation (prior to Triassic rifting) from the NE 618 Africa/Arabian-Nubian Shield of N Gondwana. 619 During Campanian-Early Miocene, northward subduction was active along the northerly 620 continental margin of the Southern Neotethys (Aktaş & Robertson 1984; Robertson & Dixon 1984; 621 Yılmaz 1993; Yılmaz et al. 1997; Robertson et al. 2012b; Barrier et al. 2018) (Fig. 16). Large 622 volumes of clastic sediments accumulated in an active margin (foredeep) setting along the southern 623 margin of the Tauride continental crust in Cyprus, including the Maastrichtian Kiparisso Vouno 624 (Alevkaya Tepe) Member in the Kyrenia Range (Fig. 16b). The overlying Maastrichtian-Early 625 Eocene basaltic rocks erupted in an extensional active margin setting (Pearce 1975; Robertson & 626 Woodcock 1986; Huang et al. 2007; Chen 2018). The clastic detritus was probably derived from by- 627 then emplaced ophiolite and arc-related units to the north (e.g. Mersin ophiolite and melange; Parlak 628 & Robertson 2004; Robertson et al. 2012b), where suitable source rocks are exposed. 629 The Taurides were affected by regional-scale southward thrusting during Early-Middle Eocene 630 time, driven by suturing of the İzmir–Ankara–Erzincan ocean farther north (Şengör & Yılmaz 1981; 631 Özgül 1984; Okay et al. 2001; Mackintosh & Robertson 2013). In addition, the Arabian platform 632 was also deformed to the northeast of Cyprus, notably in the Amanos Mountains (Duman et al. 2017). 633 The pre-existing active continental margin in the Kyrenia Range was reactivated to create a regional 634 foredeep that filled with Eocene gravity deposits, including sedimentary melange, as represented by 635 the Kalaograia–Ardana (Bahçeli–Ardahan) Formation (Robertson et al. 2014) (Fig. 16c). 636 Limited paleocurrent evidence (McCay & Robertson 2012; Robertson et al. 2014) suggests a 637 general south-Tauride source for the basal, Late Eocene interval of the Bellapais (Beylerbey) 638 Formation, similar to the inferred provenance of underlying Maastrichtian and Eocene sandstones. In 639 contrast, westerly-directed paleocurrents evidence suggests SE Turkey as the main source of the 640 Oligocene part of the Bellapais (Beylerbeyi) Formation, upwards to and including the Late Miocene 641 Mia Milia (Dağyolu) Formation (McCay & Robertson 2012). In SE Turkey, a wide range of 642 lithologies were emplaced southwards onto the Arabian platform during Oligocene-Early Miocene 643 time, including Mesozoic platform carbonates, greenschist facies metamorphic units, Late 644 Cretaceous ophiolites, Mesozoic-Early Cenozoic sedimentary and volcanic units, and both Late 645 Cretaceous and Eocene arc-related magmatic rocks (Aktaş & Robertson 1984; Perinçek & Kozlu 646 1984; Yılmaz 1993; Robertson et al. 2006; Bağci et al. 2008; Karaoğlan et al. 2016). During and 647 after this emplacement, the thrust stack supplied clastic sediment (Lice Formation) to the Neogene 648 foreland basin to the south, extending westwards into the Oligocene-Miocene foredeep represented 649 by the Kyrenia Range thrust belt farther west (McCay & Robertson 2012, 2013) (Fig. 16d). Collision 650 between the Kyrenia Range and the Troodos Massif was achieved by Late Miocene-Early Pliocene 651 time although strike slip offset continues along the intervening Ovgos (Dar Dere) Fault. 652 653 Conclusions 654  Late Triassic sandstones of the Mesozoic passive margin, represented by the Ayios Photios 655 Group (Mamonia Complex) in W Cyprus are dominated by Ediacaran-Cryogenian (c. 540-720 656 Ma) and Tonian-Stenian-aged (c. 750-1100 Ma) zircon populations, indicating an ultimate north- 657 Gondwana origin (NE Africa/Arabian-Nubian Shield). Based on facies comparisons, the direct 658 source lithologies are likely to be Paleozoic siliciclastic shelf successions in the Taurides (to the 659 north) that were detached from Gondwana as part of a microcontinent during Late Permian-Early 660 Jurassic rifting of the Southern Neotethys. 661  The Late Jurassic-Early Cretaceous deep-water slope sandstones of the Late Jurassic-Early 662 Cretaceous Ayios Photios Group have similar zircon populations to those of the underlying Late 663 Triassic sandstones, as do the shallow-marine sandstones of the Early Cretaceous Pareklisia 664 Member (detached blocks) of the Moni Melange (S Cyprus), suggesting a similar provenance. 665  Late Cretaceous (Maastrichtian) and Eocene sandstones from successions in the Kyrenia Range 666 are also dominated by Edicarian-Cryogenian and Tonian-Stenian zircons, again indicating an 667 ultimate northern Gondwana source prior to rifting of continental crust from Gondwana to open 668 the Southern Neotethys. These zircons were probably derived from Tauride units to the north 669 during and after Late Cretaceous regional deformation related to the initial stages of closure of 670 the Southern Neotethys. 671  A minor fraction of Late Cretaceous zircons in the Maastrichtian and Eocene sandstones of the 672 Kyrenia Range was derived from a nearly contemporaneous continental margin arc and/or 673 ophiolite-related units that were probably located within the Taurides to the north. 674  The new detrital zircon age data confirm that the sandstones of the Mamonia Complex (W 675 Cyprus) and the Moni Melange (S Cyprus) relate to a Mesozoic rifted passive margin, whereas 676 the Late Cretaceous-Miocene sandstones of the Kyrenia Range (N Cyprus) represent active 677 margin and collisional settings. 678

679 Acknowledgements 680 We particularly thank Dr. Richard Hinton, Dr. Steffen Kutterolf and Prof. Dick Kroon for scientific 681 discussion. Dr. Linda Kirstein and Prof. Simon Harley advised on zircon separation. Mr. Mike Hall 682 prepared the polished blocks for zircon analysis. In addition, the manuscript has benefited from the 683 detailed and constructive comments of Solomon Buckman, an anonymous reviewer and the editor, 684 Prof. Peter Clift. 685 686 Funding 687 The first author gratefully acknowledges the receipt of a joint studentship of the Principal’s Career 688 Development PhD Scholarship and Edinburgh Global Research Scholarship. The authors are grateful 689 for financial support from the Natural Environment Research Council-Ion Microprobe Facility (to A. 690 H. F. Robertson) to carry out SIMS U-Pb dating of detrital zircons. 691

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1197

1198 1199 Figure captions 1200 Fig. 1. Simplified geological map of Cyprus, indicating the locations of the Mamonia Complex (W 1201 Cyprus), the Moni Melange (S Cyprus) and the Kyrenia Range (N Cyprus) (modified from McCay & 1202 Robertson 2012).

1203 Fig. 2. Outline tectonic map of the Eastern Mediterranean region including North Africa and much 1204 of Turkey indicating the main tectonic units mentioned in the text. Main sources: Precambrian 1205 basement (Bozkurt et al. 1993; Guiraud et al. 2001; Yiǧitbaş et al. 2004; Ustaömer P. A. et al. 2005); 1206 Paleozoic cover (Göncüoğlu & Kozlu 2000). Note the location of the Mamonia Complex, the Moni 1207 Melange and the Kyrenia Range in Cyprus.

1208 Fig. 3. Summary log of the sedimentary Ayios Photios Group, one of the two main tectonic units 1209 making up the Mamonia Complex, Cyprus. Note the parts of the succession sampled for zircon 1210 dating. Simplified after Torley and Robertson (2018).

1211 Fig. 4. Outline geological map of the Mamonia Complex, showing sample locations in the Ayios 1212 Photios Group. Modified after Robertson & Woodcock (1979).

1213 Fig. 5. Outline geological map of part of the Moni Melange showing sample location. Modified after 1214 Robertson (1977).

1215 Fig. 6. Summary log of the lithologies making up the Kyrenia Range, Cyprus. Note the parts of the 1216 succession sampled for zircon dating. Simplified from Robertson & Woodcock (1986) and McCay & 1217 Robertson (2012). Abbreviations: S, south of the Kyrenia Range; N, north of the Kyrenia Range.

1218 Fig. 7. Outline geological map of the Kyrenia Range showing sample locations. Modified after 1219 Baroz (1979), Robertson & Woodcock (1986) and Robertson et al. (2012b).

1220 Fig. 8. Selected cathodoluminescence images of zircon grains analysed from sandstones of the 1221 Mamonia Complex (a-c), the Moni Melange (d) and the Kyrenia Range (e-h). Note the analysis spots 1222 and corresponding ages (±1σ Ma). Scale bar is 20μm.

1223 Fig. 9. (a, c) Concordia diagrams for detrital zircon ages obtained from Late Triassic sandstones 1224 (Vlambouros Formation, Mamonia Complex). Inset: enlarged portion of the Concordia diagram for 1225 source rock ages from 200-1500, 200-1200 Ma. (b, d) Probability-density distribution of zircon ages 1226 from these sandstones. Grey field on the probability-density diagram indicates discordant ages. 1227 206Pb/238U is used for ages <1000 Ma and 207Pb/206Pb for >1000 Ma. 1228 Fig. 10. (a, c) Concordia diagrams for detrital zircon ages obtained from the Akamas Member 1229 (Mamonia Complex) and the Pareklisia Member (Moni Melange). Inset: enlarged portion of the 1230 Concordia diagram for source rock ages from 100-1200, 300-1200 Ma. (b, d) Probability-density 1231 distribution of zircon ages obtained from these sandstones. Grey field on the probability-density 1232 diagram indicates discordant ages. 206Pb/238U is used for ages <1000 Ma and 207Pb/206Pb for >1000 1233 Ma.

1234 Fig. 11. (a, c) Concordia diagrams for detrital zircon ages obtained from the Late Cretaceous 1235 sandstone (Kiparisso Vouno (Alevkaya Tepe) Member) and Eocene sandstone (Kalograia-Ardana 1236 (Bahçeli–Ardahan) Formation). Inset: enlarged portion of the Concordia diagram for source rock 1237 ages from 0-1100, 0-1200 Ma. (b, d) Probability-density distribution of zircon ages obtained from 1238 the above sandstones. The grey field on the probability-density diagram indicates discordant ages. 1239 206Pb/238U is used for ages <1000 Ma and 207Pb/206Pb for >1000 Ma.

1240 Fig. 12. (a, c) Concordia diagrams for detrital zircon ages obtained from the Miocene sandstones 1241 (Davlos (Kaplıca) Formation and Mia Milia (Dağyolu) Formation). Inset: enlarged portion of the 1242 Concordia diagram for source rock ages from 0-150, 0-50 Ma. (b, d) Probability-density distribution 1243 of zircon ages obtained from the above sandstones. Grey field on the probability-density diagram 1244 indicates discordant ages. 206Pb/238U is used for ages <1000 Ma and 207Pb/206Pb for >1000 Ma.

1245 Fig. 13. Composite successions of the Troodos Massif (including the Moni Melange), the Mamonia 1246 Complex and the Kyrenia Range (including their related sedimentary cover). Published ages for the 1247 Troodos ophiolite are from Mukasa & Ludden (1987); biostratigraphically dated ages are mainly 1248 from Ealey & Knox (1975), Baroz (1979), Urquhart & Banner (1994), Bragin & Krylov (1996, 1249 1999), Hakyemez et al. (2000) and Lord et al. (2000). Strontium isotopic ages are from McCay et al. 1250 (2013). Youngest concordant zircon and the proposed main source ages are illustrated for 1251 comparison.

1252 Fig. 14. Distribution of detrital zircon ages and/or igneous events known from the major cratons, epi- 1253 cratonic basins and peri-Gondwanan terranes. Data source: Amazonia, Friedl et al. (2004), Nance et 1254 al. (2008); Baltica, Linnemann et al. (2004); Siberia (Angara), Sunal et al. (2008); W Africa, 1255 Linnemann et al. (2004), Murphy et al. (2004a, b, c); Arabian-Nubian Shield, Avigad et al. (2003), 1256 Drost et al. (2011); Saharan Metacraton to Tepla-Barrandian, Drost et al. (2011) and reference 1257 therein; Istanbul terrane, Ustaömer P. A. et al. (2011); Central Sakarya, Ustaömer et al. (2012b); 1258 Pontides, Ustaömer et al. (2013); Menderes Massif, Kröner & Şengör (1990), Zulauf et al. (2007) 1259 and Zlatkin et al. (2013); Taurides, Abbo et al. (2015); Jordan, Kolodner et al. (2006). The numbers 1260 within the bars refer to the number of concordant zircons in the prominent zircon population. 1261 Abbreviations: NP, Neoproterozoic; C, Cambrian; Ord., Ordovician; Sil., Silurian; Dev., Devonian; 1262 Carb., Carboniferous; P., Permian; Tria., Triassic; TS, Tuareg Shield; BNS, Nenin-Nigeria Shield.

1263 Fig. 15. Tectonic model showing possible provenance and sediment transport of the Ayios Photios 1264 Group (Mamonia Complex) in W Cyprus. (a) The Mamonia Complex formed part of the north- 1265 Gondwana continent, which rifted during the Triassic. (b) By the Late Triassic, the Mamonia 1266 Complex was fully separated from Gondwana and the Tauride platform by the embryonic Southern 1267 Neotethys. (c) Passive margin subsidence allowed the accumulation of deep-water, mixed clastic- 1268 carbonate slope facies. Abbreviations: s. l., sea level. 1269 Fig. 16. Tectonic model showing the possible provenance and sediment transport of the Late 1270 Cretaceous, Middle Eocene and Late Miocene sandstones in the Kyrenia Range. (a) Arc magmatism 1271 in the Kyrenia Range during the Campanian. (b) Deposition of terrigenous turbidites (Kiparisso 1272 Vouno (Alevkaya Tepe) Member) along the northern, active continental margin of the Southern 1273 Neotethys. (c) Deposition of Middle Eocene gravity-flows (Kalograia-Ardana (Bahçeli–Ardahan) 1274 Formation) in a foredeep, driven by thrusting to the north of the Kyrenia Range and/or initial 1275 continental collision in SE Turkey. (d) Deposition of Late Miocene sandstone turbidites in a foredeep 1276 related to closure of the Southern Neotethys. Abbreviations: s. l., sea level; ES, Eratosthenes 1277 Seamount. 1278 1279 Supplementary publication 1280 Table S1 Zircon U-Pb dating results of the sandstones analysed from Cyprus.

1281 Figure S1. Histograms show U-Pb analytical zircon data for analysed sandstones from Cyprus. Two 1282 main age populations (Ediacaran-Cryogenian, Tonian-Stenian; highlighted with dotted shading) are 1283 identified in the sandstones analysed (see text for discussion). Histograms of each sample analysed in 1284 this study are shown in Figs. 9-12. Peak ages for the Paleozoic and younger zircons are given as 1285 specific numbers besides the columns. Only grains with 90-110% concordance are included. 1286 n=number of grains analysed. Fig. 1 Click here to access/download;figure;Fig. 1.pdf

Terraces (Pleistocene) e

g t Athalassa (Gürpınar) Fm. (U. Pliocene-Pleistocene) ul n a

a ) F Nicosia (Lefkoşa) Fm. (Pliocene) lik en a R Mermer Tepe (Lapatza) Fm. (U. Miocene) m i r ği n Kythrea (Değirmenlik) Group (U. Eocene-U. Miocene) e

e D r Lapithos (Lapta) Group (U. Cretaceous-M. Eocene) a ( y re N th K Trypa (Tripa) Group (Permian-Cretaceous) Ky KYRENIA RANGE

35°15′N 10 km

Ovgos (Da r Dere) Fault

35°N TROODOS MASSIF

South Troodos Transform Troodos Massif Fault Zone Terraces (Pleistocene) Athlassa Fm. (U. Pliocene-Pleistocene) Ar 34°45′N cuat Nicosia Fm. (Pliocene) li e Fa MAMONIA neam ult Kalavasos Fm. (U. Miocene) ent COMPLEX s MONI MELANGE Pakhna Fm. (Miocene) Mamonia Complex Moni Melange Lefkara Fm. (Paleogene) (Triassic - U. Cretaceous) (U. Cretaceous) Extrusive rocks (U. Cretaceous) 32°30′E 33°00′E 33°30′E Intrusive rocks (U. Cretaceous) Fig. 2 Click here to access/download;figure;Fig. 2.pdf

30°E BLACK SEA 40°E

AP Intra-Pontide Suture Pontides 40°N Sakarya Z S OR E Ta IA A v f şa yo n n lı z ANATOLIAN -B E. Taurides o on PLATE SA lk e Lake Van MM ar D EL B SD FE li M ı ağ Z ça n r KD MA PM Ko ia la K o ırın c s ğ B C n nd Ly e a m H e KM is-A B pp r H Mis re itlis S a fo IA utu n y D t BO UB S utu e la Amanos re B p ME Hatay AC AM Antalya K e SYRIA y ng Baer Suture renia Ra Mamonia Bassit Troodos Massif Complex Moni Melange ARABIAN PLATE Eratosthenes EASTERN High MEDITERRANEAN SEA N JORDAN

NORTH AFRICAN 30°N 100 km PLATE

EGYPT Key Late Proterozoic rocks Paleozoic rocks Suture zone S A U Transform fault D I A Spreading axis R A B AC: Antalya Complex I Aﬁf A AM: Alanya Massif AP: Armutlu Peninsula BO: Bolkar Massif ARABIAN-NUBIAN SHIELD BHH: Beyşehir-Hoyran-Hadim Nappes 20°N BM: Bitlis Massif R NUBIA E EL: Elazığ D S FE: Feke IA: Isparta Angle E A KM: Kahramanmaraş KC: Konya Complex KD: Karacahisar dome MA: Malatya N ME: Mersin ophiolite DA SU MM: Menderes Massif OR: Orhaneli PM: Pütürge Massif SA: Sandıklı SD: Sultan Dağ 30°E 40°E UB: Ulukışla Basin Fig. 3 G

Ayios Photios Group p . F V M r o l o a r a F s F m m r m o b Episkopi Formation a . n m o t i a u o . - n T T r r L L A i i a a a a g s s t t

Late Triassic-Early Cretaceous e e e s s i i c c L ? o ? g l a M i m i m l C T P L T Y i n i n m m o e h n h e o e a e t c o m c l i l i d a e e l m s t n l a n u a a o

r s s s - g n d b s l l w b t i t r l l i v i o o e e y i i e i c l i e n n f i e b n n d - s r e d g g g ) n S b h e e i i r . d u m

, r t o s s a - o

o a e m r o u . e n a e i W, r d s r s n - s s

n d n a b e t t d m d r d o n e r a d e a u i

e n g d n , t s d d c d s e ﬁ e d d h i u t h i m s a n , D e s u , o

i i d c t h c r e e l n s o m n e a k a n s n t g n o l - o e r l d m c e t a - b e e n i s ( n r d u s l t e s s i c - e e i s p p c , t , i d u i L u s t s t w a d m e i a n h . d q , o l e - a

t t c i s u - n e c n e d s

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e o e e a n d d o s s c u n s t d d d s ; l o e h s s t s e e e e

a d e i o t c d c d w d s o s r i c r s ) m s n

i . a a l e a e t w a e l i n s i d t l s n s n h r c d t i - , p o e t d t i s g h t a n d s u e t r

a o r e t . a r d o y s r n b s i e

e n n s e i / p d m e i s e d s n o i s e d e t u g u s e . q ( , p d

i A s a t u o s e m p k e t s d w a o n n o i m n d a t s c e e r t e a d l d s y s , s Fig. 4 Click here to access/download;figure;Fig. 4.pdf

Key Cenozoic sediments

Loutra tis Kathikas Formation (Maastrichtian) Aphroditis Kannaviou Formation (Campanian) Troodos ophiolite (also Akamas ophiolite), Akamas Late Cretaceous Peninsula Polis Ayios Photios Gp. (Triassic-Cretaceous) Dhiarizos Gp. (mainly Triassic), with intersliced ophiolitic rocks 35°00′ N Sample locality

Fasli GC14-9

P o A l is g r Kannaviou l c in u r e a a t b a e F m e n e a n u t s lt Ayios Photios GC14-16 Mavrokolympos Dam Faleia Pentalia Mediterranean Sea

Armou Episkopi Kelokedara N GC14-3 Nata 0 5km Mamonia

Marona 37°N Anatolian Plate Souskiou Agia Varvara

Arabian Plate Kapotami River Cyprus N Mediterranean Sea 34°N 33°E 37°E 32°30′ E Petra Tou Romiou Fig. 5 Click here to access/download;figure;Fig. 5.pdf

P Pareklisia

GC14-17 N

P 100 m 34°44′N

P P P P

P P 33°09′E 33°10′E Neritic limestone Pareklisia Member (Late Miocene) P (Early Cretaceous) Troodos ophiolite, extrusive Detached blocks in melange rocks (Late Cretaceous) Exposed boundaries Localised boundaries

Road Sample locality Fig. 6 Epoch/Age Cretaceous Paleocene Eocene Oligocene Miocene Maastrichtian T riassic-Cret. Serravallian Burdigalian Aquitanian Messinian Langhian T Rupelian Chattian ortonian

Lapithos (Lapta) Group Kythrea (Değirmenlik) Group Group (Bah (T (Büyüktepe) Cong. Mermer Kalograia-Ardana

(Beylerbeyi) Fm. Mia Milia Kiparisso V S (Alevkaya (Y Formation Y ripa) Group Y A (Mall (Arapk (T ı az ama

yios Nikolaos (Dağyolu) Fm. lmazk T (Esentepe) Fm. ç Melounda (Ge Bellapais Flamoudi irmen) Fm. (Kapl rypa eli–Ardahan) ı Kythrea Klepini l ı ı tepe Fm. da Mbr ç Panagra Fm. T N T ç Davlos k ö rapeza epe Fm. itk ö ö ğ y) Fm. ı y Fm. ca) Fm. y) Fm. ) Fm. . T ö ouno epe) y)

Fm. Log Limestone breccias,pelagiccarbonatesandbasalticlavas. Fine-grained sandstones,siltstonesandmarls. Brown marls,mudstonesandsandstones. Sandstone turbiditesanddebris- Medium- to Coarse tomedium-grainedlithicsandstones. Gypsiferous units. Calcareous sandstonesandsandycalcarenites;localised. Shallow-marine carbonates;undi diagenetic chert;intercalatedwithbasalts. marls. sandstones and Fine-grained Grey-, pink-colouredpelagiccarbonates,locallywith Chalk clay Conglomeratic units;channellised,clast-supported. , limestones,sandstonesandmarls. fi Red hemipelagicmarls. ne-grained calcareoussandstonesandmarls. Description Click heretoaccess/download;figure;Fig.6.pdf Grey/white marls. Massive fl ff fi ow deposits. erentiated. ne-grained sandstones. Fig. 7 Click here to access/download;figure;Fig. 7.pdf

Mersinlik (Flamoudi)

Bahçeli GC14-32 Lapta GC14-25 (Kalograia) (Lapithos) Girne GC14-47 (Kyrenia) Arıdamı GC14-36 (Artemi) Kyt hrea ( Değ irme nlik) F N aul t Değirmenlik O vgo (Kythrea) 5 km s (Da r der e) Fa 35°10′ N ult 33°30′ E Pliocene&Quaternary Kythrea (Değirmenlik) Gp. (Late Eocene-Miocene)

Kalograia-Ardana (Bahçeli–Ardahan) Fm. (Eocene) Lapithos Melounda (Mallıdağ) and Ayios Nikolaos (Yamaçköy) Fm. (Lapta) Gp. (Late Cretaceous-Eocene) Trypa (Tripa) Gp. (Permian-Cretaceous) Sample locality Fig. 8 Click here to access/download;figure;Fig. 8.pdf

633±4 571±5 654±4 711±4 24±0.4 625±5 932±23 1091±41 813±7

7 13±0.3 16±0.2 6

1 558±4 25±0.3 3 - - 4 4 1 1 C C

) G 3 27 29 40 44 45 47 ) G d h

( 850±7 807±7 476±3

1005±31 ( 2627±15 951±6 1 2 3 4 5 6

84±0.7 12±0.3 1017±80 88±0.6 48±0.5 796±6 59 81 82 84 86 87 983±10 592±5 674±4 693±41000±53 606±5 765±6 5 2 - 4 1 6 1 C

- 1 6 7 11 13 22

4 10±0.5

) G 74±0.7 51±0.9 1 91±0.9 328±3

1 2 7 8 10 21 32 g C 1062±22 1018±22 ( 588±6 503±4661±4 2607±9 715±5 584±5 ) G c (

23 28 30 36 37 33 34 39 42 49 52 65 88 918±6 589±4 1095±30 1051±52 3052±14 321±2 335±2 759±10 93±1 3139±11 707±6 1140±21 87±1 9 581±4 - 4 1 C

) G 8 9 32 37 39 40 41 2 b

( 600±3 525±3 951±5 602±3 987±9 505±4 3 3 12 25 29 45 46 47 1006±14 - 4 1

C 809±5 1719±1161±0.5 647±6 45±0.5 999±37 ) G f 43 46 47 57 60 65 86 ( 2020±11 1931±23 565±4 320±2 751±6 636±4

3 3221±7 -

4 49 56 72 73 74 80 1 C

7 422±5 458±5 ) G 6 12 15 18 25 37 43 4 a 346±4 87±1 - (

1037±32 4 665±5 923±5 287±2 2664±10 975±21 1 C ) G e ( 46 49 53 54 63 83 1 2 3 4 Fig. 9 Click here to access/download;figure;Fig. 9.pdf

data-point error ellipses are 2σ 8 0.8 0 0 .

0 Vlambouros Formation (GC14-3) 3400 10 n=77/97, 90-110% conc. 6

3000 2.5 3 0

0.6 0 0.26 . 8 Frequency 1400 0 2600

U 0.22 1200 4

238 6 2200 3 0 0

0.4 0.18 1000 . Pb/ 0

206 1800 0.14 800 Probability 4 1400 2 2 600 0 0 0.2 0.10 . 1000 0 2 0.06 400 1 200 0 1000 1200 1400 1600 1800 3000 3200 800 600 200 2000 2200 2400 2600 2800 0.02 400 0 0 0.5 0.0 0 4 8 12 16 20 24 28 a 207Pb/235U b Age (Ma)

data-point error ellipses are 2σ 6 0.8 0

0 10 .

0 Vlambouros Formation (GC14-9) n=60/87, 90–110% conc. 9 1.8 2.2 8 0.6 3000 1200 4

0 7 Frequency 0 2600 0.18 1000 . 0 U 2.2 6 238 2200 0.4 0.14 800 5 Pb/ 1.8 Probability 206 1800 2 4 0

0.10 0 600 1.4 . 3

1400 0 0.2 400 2 1000 0.06 1.0 1 200 0.6

0.02 0 1 1300 1500 1700 1900 700 300 500 900 3100 2100 2300 2500 2700 2900 0 0.2 0.4 100 0.0 0 4 8 12 16 20 24 c 207Pb/235U d Age (Ma) Fig. 10 Click here to access/download;figure;Fig. 10.pdf

data-point error ellipses are 2σ 8 0.6 0 0 .

0 Akamas Member (GC14-16) 14 n=59/83, 90–110% conc. 0.5 2600 6 12

2.0 0 0 2200 0.20 . 1100 0

0.4 10Frequency U

0.16 4

238 1800 2.0 0 8 0

0.3 900 . Pb/ 0.12 700 0 206 1400 6 1.6 Probability

0.2 2 1000 0.08 0 4 500 0 1.2 .

300 0 0.04 2 0.1 600 0.8 100 0 1000 1200 1400 1600 1800 800 600 2000 2200 2400 2600 0.00 400 0 0.0 0.0 0.4 0 2 4 6 8 10 12 14 a 207Pb/235U b Age (Ma) data-point error ellipses are 2σ 8 0.6 0 0

. 14

0 Pareklisia Member (GC14-17) 0.5 2600 n=60/79, 90–110% conc. 12 6 0 0 .

2200 0.20 0 10 0.4 1100 Frequency U 4 8

2.2 0 238 1800

0.16 900 0 0.3 . 0 Pb/ 6 206 1400 1.8 Probability

0.12 700 2 0.2 0 4 1000 0

1.4 . 0.08 0 500 2 0.1 600 1.0 300 0 1000 1200 1400 1600 1800 800 600 2000 2200 2400 2600 0.04 400 0 0.0 0.2 0.6 0 2 4 6 8 10 12 14 c 207Pb/235U d Age (Ma) Fig. 11 Click here to access/download;figure;Fig. 11.pdf

data-point error ellipses are 2σ 2 0.8 1

0 8 .

0 Kiparisso Vouno Member (GC14-47) n=64/99, 90–110% conc. 7 3000 0.6 6 8

0.20 0 0 Frequency

1100 . 2600 5 0 U 0.16 238 2200 900 0.4 4 Pb/ 0.12 700 206 1800 4 Probability

1.6 0 3 0 0.08 .

1400 500 0 1.2 2 0.2 0.04 300 1000 0.8 1 100 0.00 0 1000 1200 1400 1600 1800 3000 800 600 200 2000 2200 2400 2600 2800 0.0 0.4 400 0 0.0 0 0 4 8 12 16 20 24 a 207Pb/235U b Age (Ma) data-point error ellipses are 2σ 7 Kalograia-Ardana Formation (GC14-32)

0.6 3000 0 n=41/74, 90–110% conc.

2 6 0 . 0 2600 5 1100 Frequency

U 0.16 0.4 2200 4 238 900 3 0 Pb/

1800 1 0.12 3 0 206 700 . 0 1400 Probability 0.08 2 0.2 500 1000 2 0.04 300 1 100 0 1000 1200 1400 1600 1800 3000 800 600 200 2000 2200 2400 2600 2800 0.00 400 0 0.0 0 1 0 0 4 8 12 16 20 c 207Pb/235U d Age (Ma) Fig. 12 Click here to access/download;figure;Fig. 12.pdf

0.4 data-point error ellipses are 2σ

0 24 6 Davlos Formation (GC14-25) 1 . n=42/53, 90–110% conc. 1800 0 0.024 20 0.3 150 0 2

130 1 . 0.020 16 Frequency 1400 0

U 0.16 110 238 0.016 0 0.2 90 8 12 0 Pb/ . 0 206 1000 0.012 70 Probability 0.12 8 0

0.008 50 4 0 0.1 600 . 30 0 4 0.004 0.08 10 0 1000 1200 1400 1600 1800 800 600 200 2000 200 0.000 400 0 0.00 0.04 0 0.0 0 2 4 6 a 207Pb/235U b Age (Ma) data-point error ellipses are 2σ 3 0.16 900 Mia Milia Formation (GC14-36) 0 n=6/7, 90–110% conc. 0 2 . 0 0.12 700 Frequency 2

U 45 238 0.006 35 Pb/ 500 0 0 206 0.08 0.05 1 Probability

25 . 0 1 300 0.003 15 0.04 0.03 0.001 5 100

0.00 0.01 0 1000 800 600 200 400 0 0.00 0 0.0 0.2 0.4 0.6 0.8 1.0 1.2 1.4 c 207Pb/235U d Age (Ma) Fig. 13 2 2 2 2 1 1 1 1 1 1 1 1 1 1 M 3 2 1 0 9 8 7 6 5 4 3 2 0 1 9 8 7 6 5 4 3 2 1 0 0 0 0 0 0 0 0 0 0 0 0 0 0 a 0 0 0 0 0 0 0 0 0

Mesozoic Cenozoic Era Q

Triassic Jurassic Cretaceous Paleogene Neogene u Period . p p d g P O l i P i a M a l a E a l M l b l i o E E g l b i o i g L L L e o b o i w l i a a a c o d a a a o o c r c s e r r o c d t t t g c e e

l l Epoch e e e e d a n e y y l e r n n e v a e n n e e a s T n e y e e i r k t o d e e o i m d o e s o n t 2 1 a 5 8 7 p 7 r 1 3 5 5 5 5 h 2 y c 7 m n m r s 2 9 4 9 4 0 i 4 a 2 5 a o o f f f f f f f a u - - 8 - 9 5 - d 5 7 4 2 1 2 3 2 1 o n n l 2 2 1 1 G G r d i - - - G i - 8 Plagiogranite, c. 90 Ma , f v t d - i o 7 0 1 6 0 7 5 1 s e & n m C C - e C s l 4 2 8 9 9 0 3 3 0 7 t e s a r t o 1 1 a 5 0 8 1 5 5 7 1 9 1 o r n 4 4 r M M M M M M M 4 i 4 3 n t i a e - - - s M n e M M e t a a a a 3 a a a 9 1 n e e o a a a 6 d d u

Ayios Photios Group m s i r m r s t b o o i e n n d h n i e i a a C t t e l a l o r f f f f f f f f f f C C C K 7 o y c 1 1 1 1 2 3 2 1 4 2 w i 5 a a a 6 m , f , f , f m - 7 r r l 6 o l n n p 4 2 3 G m o 1 - v i i l , f 1 v - a a e C e e 1 7 i n n x & 5 r a r 1 2 1 i - - , f n d 4 6 9 R N - g - M M 6 H h o 1 i p r c c s a a r a a 7 a e s M l a h i e n e a a u e e r a l o - t s n a t d b f l H i l e n t a l g i o i o i m a r i M c n m i n i w c u v e a e t i Click heretoaccess/download;figure;Fig.13.pdf - e n a a t e m s a e f C f f f f f f l t r n r 1 2 3 2 1 4 2 t a a r b a i o a v b , f n r o r S f f f f f f n m i y c o 6 B 5 C 4 B 3 C 2 P 1 R g i a n 3 n e 2 1 n e & p n a e 6 5 8 7 7 a o a t i e l 8 t o a a 4 4 2 6 5 5 e t v a v r n e n 9 n l d 2 9 9 1 5 o 3 a e n c i G G t G - 7 o i a - - - 5 9 n - l r a k h o 1 2 2 1 v 1 1 d n - - t C C t C r i l e 0 7 0 0 7 i 1 7 i c f a e - o u c f 1 1 1 s 1 9 0 4 9 0 4 0 r o n m i 4 4 i 4 7 1 1 5 1 2 o 0 5 u a t o - - s - K M M M M M M r M M s n 2 r 4 3 a s a y a a 5 n a a a a 7 e d d a a 2 v o m r m o o v e e a e t i o a l d i p b n n n c n p p u o r i n i a i f a R i e f o l s e o s n a e s r i - r f i t r c r i o ﬂ a c r t a a e o s f f f 8 4 1 f n h 2 2 2 4 s w o 7 M 5 M 0 M g e i , f , f c l e r s k 3 3 t a a a , S ( ( ( t t t h h h i i i s s s t t t u u u d d d y y y ) ) ) Fig. 14

Key THIS STUDY PERI-GONDWANAN TERRANES BASINS CRATONS S S S C P I V A P K T K M A s a h M B a o a l e v A a a t A i r a D M h e i Vo M p M a x a n a u a n e r i l A k m r J a n a M T ( o T a a e o S n r b W t a l l r t d e a o A S d ( o B m o i r r r d e i P g r i v u r k - b i b d s a d a t g m a a a r a a i n T r n i e a p l r a l n a u A s s a o o e b h e d o n n i n l S n B n N a n i i g K h r l l s a c s o i l l t a l z c u s e a f t a s a s a e - d f e e i s i a E a i u r r i s o a N a o c r r a r c - C n C o e i i a r a - s o G G r r o i a a c - C a o C - S a n A u a T a . a a u i r k t z C C d - s a O N n n n i a . s o i r r N r b f O l C ) a s a / o a a i . b 1 1 r a r O a g i r a n / P i b ğ i . r r n i d . 4 4 D a r . n c d -

400 c i r - . y l N B . - - 4 B a P d T n e ı C a . n e 9 3 k a . P . N r S v . ) d m 6 3 a .

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c 2200 i z e a o o a n n n 2300 i c 2400 L d o 3 C 2500 p e e 2 i t a 2 r n n i

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n 3400 3500 Fig. 15 Click here to access/download;figure;Fig. 15.pdf

S N Africa Taurides-Anatolides Antalya Paleotethys s.l.

a Late Permian-Early Triassic Taurides Vlambouros Fm.

S. Neotethys b Late Triassic (Norian)

Akamas Mbr.

c Early Cretaceous

Oceanic crust Continental crust Carbonate platform Clastic sediment Fig. 16 Click here to access/download;figure;Fig. 16.pdf

S N Africa Kyrenia Taurides ES Troodos s. l.

S. Neotethys Arc volcanism

a Campanian

Troodos Kiparisso Vouno Mbr. rotation

Rollback b Maastrichtian

Kalograia-Ardana Fm. Foredeep

Detached slab? c Middle Eocene Mia Milia Fm. Davlos Fm. Ovgos Fault

Renewed subduction d Late Miocene Kythrea Fault Thrust Fault Oceanic crust Troodos ophiolite Continental Carbonate Clastic Arc crust platform sediment Zircon U-Pb dating results of the sandstones analysed from Cyprus

Click here to access/download supplementary material Table S1 Zircon U-Pb dating results.xlsx Histograms show U-Pb analytical zircon data for analysed sandstones from Cyprus

Click here to access/download supplementary material Supplementary Figure S1.pdf