Polyphase Evolution of Pelagonia (Northern Greece) Revealed by Geological and ﬁssion-Track Data F

Home , Almopia, Pelagonia

Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | C C ◦ ◦ erent compressional ff 1 3076 3075 , and J.-P. Burg 1 C and erosion of the basement rocks. ZFT and AFT in western ◦ , M. G. Fellin 1,2 This discussion paper is/has beenPlease under refer review to for the the corresponding journal final Solid paper Earth in (SE). SE if available. Department of Earth Sciences, ETHInstitute Zurich, of Sonneggstrasse Earth 5, Sciences, 8092 University Zurich, of Switzerland Lausanne, 1015 Lausanne, Switzerland Abstract The Pelagonian zone, between theAxios/Vardar/Almopia zone External (AVAZ) and Hellenides/Cyclades Rhodope to to theCretaceous the east, and west was in and involved in Late the latecontroversial. Early Cretaceous-Eocene This orogenic events work whosepublished constrains zircon duration (ZFT) their are and still apatite late (AFT) thermal fission-track ages imprints. show cooling New below 240 and previously thrusting. Central-eastern Pelagonia cooled rapidly and uniformly from 240 to 80 and AVAZ are exposed between two nappe-complexes with di and eastern Pelagonia, respectively, set at 40 Ma the latest thermal imprint related to 1 Introduction The Pelagonian zone, in northernpoly-orogenic Greece (Fig. thrust 1a), is nappe aet NW–SE (cf. trending Schermer metamorphic al., etAxios/Vardar/Almopia al., 2014) zone 1990; (AVAZ; Kilias overlain Bernoulli et and al., by 2010; Laubscher, Schenker 1972). the The Permian–Early Pelagonia Jurassic passive margin of the of the metamorphic western AVAZPelagonia imbricates between between 102 and 86 93–90Rhodope Ma, and of at northern 68 72 Ma, Ma.subsidence of At of the the Late regional eastern100 scale, Ma Cretaceous AVAZ this marine the at heterogeneous basin(s) 8070 Early cooling Ma Ma that is Cretaceous in and unconformably coeval the (130–110 ofat with Ma) covered AVAZ 40–38 and western Ma. since thrust migrated Renewed thrusting across system.cooling in Pelagonia Pelagonia Thrusting below is to 240 attested restarted reach at the 68 at Ma External by abrupt Hellenides and rapid between 24 and 16 Maeven earlier, in at the footwall 33 Mainverse of modeling in a the of major western extensional AFTPliocene-to-recent sediment. fault. AVAZ. lengths. Post-7 Extension Ma It started rapid occurred cooling while is E–W inferred normal from faults were cutting Polyphase evolution of Pelagonia (northern Greece) revealed by geological and fission-track data F. L. Schenker Solid Earth Discuss., 6, 3075–3109,www.solid-earth-discuss.net/6/3075/2014/ 2014 doi:10.5194/sed-6-3075-2014 © Author(s) 2014. CC Attribution 3.0 License. 1 2 Received: 2 October 2014 – Accepted: 6Correspondence October to: 2014 F. L. – Schenker Published: (fi[email protected]) 10 November 2014 Published by Copernicus Publications on behalf of the European Geosciences Union. 5 15 25 10 20 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | C, Reiners ◦ C in the footwall ◦ 3078 3077 C coeval with E–W trending normal fault zones in central-eastern Pelagonia. ◦ This study identified four major cooling events: (i) post-collisional, Late Creataceous 1.1 Tectonic setting and geological overview The Pelagonian zone in thethe Internal AVAZ Hellenides to is the delimitedPelagonia northeast by block two and ophiolitic has the domains: together Pindos been with Ophiolites detached the to frombreakup lower the southern unit and southwest of (Fig. subsequent Eurasiaplate 1). Rhodope opening (Anders The convergence (Schenker of et and et the N–NE al.,Cretaceous al., Tethys southwestward dipping 2007), 2014), Ocean. obduction subduction during of In causedand an Gondwana the the AVAZ Laubscher, segment Late late onto 1972). Jurassic-to-Early hemipelagic Early Pelagonia The (Bernoulli marls, Jurassic, obducted ultramaficin Late rocks Fig. and Triassic-to-Cretaceous 3), carbonates metavolcanites areof attributed (schematically and the to represented Tethys the Oceancollision Permian–Early (Sharp between Jurassic and southwestern Eurasia and passive Robertson,Early margin Pelagonia 2006). Cretaceous (Schenker Subsequent tectono-metamorphic et events continent-continent al.,et (Yarwood 2014) and al., was Dixon, 1990). responsible 1977; Theunconformably for Schermer imbricated Pelagonian by and transgressive Vardarlimestones rocks passing Cenomanian-to-Early upwards were into eroded Campanian Paleocene andPapanikolaou, turbidites (e.g. 2009). (100 covered Mercier Maastrichtian-Eocene and to (ca. Vergely, 1994; mark 70–38 80 Ma) Ma) the syn-orogenic beginning massthe flows of Eocene-to-Miocene a (38–ca. 15 second Ma)External southwest-vergent compression accretionary Hellenides event system (Fig. (Jacobshagen ofextension the (Le 2) et Pichon that al., et migrated al.,were 1978). 1979; towards attested Brun Oligocene–Miocene and only (postCoutand Faccenna, in 2008) et 24 al., and Ma) the 2014). related Basins fast southeasternbasin, at cooling Fig. the Pelagonian 1) western margin (Mesohellenic Pelagonian trough)the margins (Lecassin and were Eocene eastern filled et (Axios with compressional al.,Pleistocene colluvial-proluvial and (post sediments 2007; 7 during Ma) the coalbasement Miocene and (Koukouzas lacustrine et extensional al., sediments 1979; events. locally Mavridou covered Late et the al., Pelagonian Miocene 2003; Steenbrink to et al., 2006). of a normal fault in80 the central-eastern Pelagonia, (iv) post-7 Ma fast cooling below ca. histories (Figs. 1abetween and the 2). LateTo To Jurassic the the southwest, and northeast, theEocene-to-Miocene the times fold-and-thrust the (Renz Early and belt Rhodope Reichel, Cretaceous ofboth 1945). complex The (references the thrust Pelagonia zone was External in events experienced imprinting (Godfriaux Hellenides built Burg, a et formed up complex 2012). al., during distributionfission-track of 1988; (ZFT), low-temperature Schermer, zircon thermochronometric (U-Th)/He 1993; data (ZHe),Th)/He (zircon Schenker apatite (AHe), fission-track et Most, (AFT) 2003; al., andZFT Vamvaka apatite 2014) et ages (U- al., range 2010; between Coutandthe 86 et younger al., and ages 2014). in 48 MaZHe To the the between and west. north, 53 AFT To the and agesand south 20 between 6 Ma, Ma ZFT 46 AFT with ages and the agesstructural range 25 frame, younger between Ma between these ages 42 76 with largely-distributed in and and low-temperature the (from 32 8 Ma, Ma east 240 to (Fig. and 70 1). AHe Integrated between into 26 a geological and AVAZ’s basins at ca. 68 Ma, (iii) fast 24 to 16 Ma cooling below 240 cooling and subsidencethe from development 102 of marine to basins;Pelagonia, ca. cooling AVAZ and was 68 western heterogeneous Ma Rhodope, in as (ii) timeLate faster and shown cooling Cretaceous space and by over are erosion ZFT rates coincident during ages with the coeval increased with detritus from Pelagonia into western and Brandon, 2006)of cooling ages tectonic can processessedimentary, substantially metamorphic and contribute and to their structuralAFT the observations duration and understanding with ZFT in ages bothadjacent a we published AVAZ aimed: in and multi-event (i) the new orogeny.space to multi-event unravel By and history the of time integrating roletectonics. the the of Hellenides the Eocene-to-Miocene and Pelagonian cooling zone (ii) and into to the characterize compressional in vs. extensional 5 5 10 15 20 25 10 25 15 20 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 2 C ◦ C for AFT to 70 ◦ erences between footwall and ff C for ZHe, 110 ◦ 3080 3079 C for ZFT, 180 ◦ erent elevations (Fig. 6). In 1995 an earthquake of ff from 240 1 − C Ma ◦ ZHe in southern Pelagonia yields 53–36 Ma ages to the west and 30–20 Ma close AFT ages are 46 to 25 Ma in northern Pelagonia (Most et al., 2001; Most, 2003), 41 AHe ages in southern Pelagonia show a general eastward younging trend fromDetrital 26 apatites from Eocene-to-Miocene sediments of the southern Mesohellenic The youngest, regionally distributed structures are E–W steep faults that bound Foliation in the low-grade AVAZ imbricates is sub-parallel to the lithological contacts. In the study area (Fig. 4) the regional main foliation and lithological contacts of The regional top-to-the-SW sense of shear is associated with collision of Pelagonia ZFT ages (Most et al., 2001; Most, 2003; Vamvaka et al., 2010) range between 86 40 Ma (Vamvaka et al., 2010). 2 New zircon and apatite fission-track2.1 dating Method The FT technique has been usedalong to a trace SW–NE the transect low-temperature history from of bothzones rocks the to collected footwall date and fault hanging activity wall and of deformation major from ductile shear age di to and within the13 Ma Olympos window to (Coutand the etregional south compilations al., of (Fig. 2014). 1) ZHe theour since ages Olympos data they are do are window younger, not available (Fig. at include inas ZHe 1b). they southern ages. have Pelagonia ZHe a Nevertheless, only similar they ages and age are are distribution implicitly as not taken the into plotted ZFTto account ages. for 25 Ma in thein southwest the (Vamvaka et southeast al., 2010; (Most,60–47 Ma Coutand 2003; et (Most Coutand al., et 2014) etages al., and from al., 18–11 68 2001; Ma 2014). to Most, 47 The Ma 2003). (Kydonakis few et The data al., western 2014). into Rhodope the 10 Ma yielded AVAZ (Coutand, are also 2014).6 This Ma AFT trend around is and associated in the with Olympos rapid window cooling (Coutand between et 12trough al., and (Fig. 2014). 1b) show two age populations: at ca. 65 Ma and, more prominent, at ca. the western part (Fig. 1b).Most, To 2003; the Vamvaka et south, al., they 2010). varyto Younger, from the 35–32 Ma 76 Olympos old to window ZFT 32 (Fig. ageswestern Ma 1b). are Rhodope (Most In located yielded et the close 72 al., Ma AVAZ, ZFT 2001; ZFT ages ages are (Wüthrich, 80 2009). Ma (Most, 2003). The placed lacustrine sediments at di to the westKoukouzas et the al., Late 1979; Steenbrink Miocene–Pliocene et Ptolemais-Kozani al., basins 2006). These (Figs. normal 3 faults displaced and and 5, both the low-grade imbricatessediments. and the Cenomanian-to-Maastrichtian unconformable magnitude 6.6 demonstrated recent activity of these faults (Pavlides1.2 et al., 1995). Previously published low-temperature thermochronometric data We present existing information incooling decreasing rates of order 10 of closure temperatures for mean It dips in general to thewith E, the locally Pelagonian to rocks (Fig. the 5). W Shearto-the-SW due bands to thrusting. and a SW-vergent Late roll-over drag antiform and folds close indicate widely to top- distributed the contact top-to-the-E normal faults (Fig. 5) cut brittle deformation features (Schenker et al., 2014). for AHe (e.g. Reiners and Brandon, 2006). and 61 Ma in the eastern part of north Pelagonia and span between 53 and 39 Ma in Pelagonia are mostly sub-horizontal. Bending of the foliation defines a 20-by-20 km with Rhodope (Schenker et al.,of-shear 2014). Discrete overprint shear the zones former withshear top-to-the-NE regional zone sense- separates foliation. Pelagonia The from most the prominent AVAZ (Fig. top-to-the-E–NE 5) and contains both ductile and dome with southwesternsouthern ones and (Fig. 5). northeastern Metamorphicto grade greenschist-facies evolves flanks from close amphibolite-facies to steeper in thethrust the than sheets flanks core of of the the the AVAZ. dome. northern The eastern and flank is covered by 5 5 25 10 15 20 20 15 10 25 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | C. C. ◦ ◦ erent ff values are standards. ζ ff in marls (Figs. 3 and 7c). method (Hurford, 1990), at a controlled temperature of 21 ζ 3 Globotruncana sp. 3082 3081 (Figs. 3 and 7b), setting the lower deposition limit erence along the SW–NE transect. The results show no ff 66 Ma based on the Late Cretaceous The samples 10-130 and 10-128 were collected in the upper beds of a ca. 350 m Zircons and apatites were extracted with acoustic shockwaves produced in the < 2.3 Results 2.3.1 Zircon fission-track results The pooled ZFTTable 1) ages with of no discernible the di granitoids vary between 24 and 20.7 Ma (Fig. 1 and in diameter orthogneissic10-130. boulder Sample from 10-128sequence a is and clastic characterized 10-130 layerolistolites by containing were marls stratigraphic Late Cretaceous not intercalated above rudistsshowing with (Appendix metamorphosed. sample A) pebbly an and The mudstones, conglomerates up-sequence (Fig. carbonatic typical sedimentary increase 3) for and the coarseningsourcing Pelagonian of from and these the zones AVAZ detritus.Rhodope, partially fauna where covered The attesting Rudists by rudists that carbonatic were2006). platforms not the are and found Marls studied not (cf. covering from Viquesnel, clasticsHelvetoglobotruncana the unconformably 1853; were Sharp helvetica the and AVAZ Robertson, thrust sheets contain the Turonian thick sedimentary sequenceSample unconformably covering 10–130 thequartz, is AVAZ feldspar, imbricates a serpentinites (Fig. and carbonatic 3). schists. matrix-supported Sample 10–128 conglomerate is a with single, pebbles about 50 of cm 2.2.2 AVAZ Sample 10-029 from theimbricated AVAZ is Upper a Jurassic–Lower grain-supported Cretaceous conglomerateClasts “Flysch-Phyllitic that Series” of belongs (IGME, to Cr-spinel 1991). the suggest and that these hemicrystalline sedimentsblasts were mafic in deposited sample in fragments 10-029 front indicate (likely of low-grade the metamorphism of AVAZ (Fig. obduction. ophiolitic 7a). Chlorite origin) between 93.5 and 90 Mais (Bolli, 1945). The upper age limit of the stratigraphic column metamorphic grades fromquartz, amphibolite plagioclase, to biotite greenschist or facies.actinolite. chlorite, They epidote, generally white mica, contain sphene, and horblende or hangingwall rocks (Figs. 3 andand 5). Fig. Elevations of 5). sampling FT sites ages were were recorded (Table calculated 1 with the All samples were irradiatedU at muscovite the discs OregonCN5 as State as external University fluence Reactor, detectors, along dosimeter CN1 with for as low- apatites, fluence Durango dosimeter and for Fish zircons or Canyon Tu textures from non-foliated to mylonitic and mineral assemblage attesting di 2.2 Sample location and description Sample location and details are given in Fig. 42.2.1 and Table 1. Pelagonia Samples 09-108, 09-120, 09-121,from 09-055, the Pelagonian 09-932, basement. 09-098 These granitoids and are 10-090 characterized by are variable gneissic granitoids Apatites were etched for 20 s in 5.5 MHNO After irradiation, the externalvisualization detectors of were the etched induced with tracks. 40 % HF for 45 min allowing SELFRAG apparatus), (http://www.selfrag.com ETH-Zürich. Standard heavy-liquidmagnetic and separation delivered fractions enrichedZircon in grains apatite and were zircon mountedpolished (Naeser, in 1976). to teflon expose discs theZircons and internal were apatites surfaces etched in of epoxy. for The minerals 25 mounts and to were etched 28 to h visualize with tracks. NaOH-KOH in an eutectic melt at 220 listed in Table 1. 5 5 25 15 10 20 10 20 15 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | )) )- 10 2 2 χ χ + ( ( is the P P C. C (AFT ◦ ◦ par D 16, Table 1) 3.1) Ma with − = 5.6) Ma and (ii) n + erence along the ff 1.5 Ma). Moreover, 3.4 ) value of 25.3 %. -probability ( 2 2 + + 6.1 χ χ ( − P 1.4 ) 15 % (Fig. 4 and 5 and − 2 χ and U-concentration values ( P par D ) values of the granitoid AFT cooling ecting significantly either the central or 5.2) Ma 2 ff 10) Ma with a + χ ( + P 9 4.8 − − 3083 3084 ) value. The large age distribution of this sample 42.8) Ma (Fig. 8b). 2 χ + ( P 56 − 16.1 Ma). The ) value of 1.7 % indicating that the age distribution consists values of sample 09-055 could partly explain the spread of = 2 2.8 %). The grain age distribution of this sample was strongly χ ( par = ) value of 17 % without a ) P D 2 2 χ χ ( ( values ranging between 1.5 and 2.2 µm (Fig. 9). The P P par (Figs. 3 and 7c). Therefore, young apatites in the ca. 66 Ma sediments D -test ( 2 χ 6.2) Ma with a ) value of 13.7 %. As discussed in the previous paragraph, sample 10-128 is + 22.9 Ma) is significantly older than the others: its upper 68 % confidence interval 2 C (Spear, 1995) that have partially or totally reset the zircons at 92.2 ( χ = ◦ ( ected by one grain with an old age (46.1 Ma) (Fig. 9). The omission of this outlier- 5.7 The ZFT pooled ages in the sedimentary rocks yielded ages between 92.2 and The only AFT age from the Vardar unit (10-128) is 32.7 ( P 9) Ma. The gneissic boulder (10-128) in the Upper Cretaceous sedimentary unit ff − ages were between 2.8 and 99.6 %. Exceptionally for magmatic rocks, sample 09-055 2.3.2 Apatite fission-track results The basement AFT ages arethese distributed ages between show 22.9 no and correlation 16.1 Ma. with As elevation the and ZFT no ages, discernible di a Late Jurassic one at 179.6 ( profile (Fig. 5 and Table 1). Onlyage the easternmost sample (10-090, Figs.is 4 and 1.3 5, Ma pooled olderwest that (09-098, the pooled lower age 68 % confidence interval of the closest sample to the Table 1). The unmetamorphosed rocks of( sample 10-130 showed a pooledof age multiple of 76.2 populations. Usingpopulations were the estimated: Binomfit (i) computer a program Late (Brandon, Cretaceous 1996), one two at 68 ( The age density histogram300 Ma. (Fig. The 8a) sparse exhibits amount a of broad countable scatter zircons of from data this from sample ca. ( 50 to prevented stating with statisticalNevertheless, methods the whether metamorphic its growth250 of ZFT chlorite ages indicates are peak reset− temperatures or above detrital. yielded a single age population at 67.4 ( a gneissic boulder inGlobotruncana the unmetamorphosed sediments containinghave Upper been Cretaceous totally reset at ca. 33 Ma or earlier, and they cooled below 110 a closure temperature) atimplies 32.7 Ma. that temperatures The that ZFT have reset age apatite did of not this rise beyond sample 220–240 was not reset which of this samples hintsample to is compositional heterogeneity, consistent and withits because a AFT the single ZFT age population age distributionpartial-resetting centered of reflects conditions. this at variable 23.1 annealing Ma, resistance we and conclude does that not relate to apatites of sample 09-055126 ppm showed high and spread of U-concentration with values up to may also be due todamage its of high apatites. spread Although ofdamage no U-concentration that experimental on causes data the significant exist radiation FTplay on a annealing the influence role kinetics of (Carlson in radiation et apatites, al., it 1999). is Because commonly both argued the that it may a failed the grain resulted in a the pooled age, which remain unchanged within error (17.6, its grain ages resulting in a low arithmetic mean maximum diameterinfer of the FT relative resistance etch-figures, to and annealingrelative this (Burtner wide et parameter range al., is 1994; of used Carlson et to al., 1999). The relationship between age and elevation (Fig. 1 and Table 1). The 67.4 Ma (Table 1).gave ZFT a ages single in the age low population metamorphic-grade of rock 92.2 of ( sample 10-028 ranged between 18.5 and 95.8test; %, this which is indicates well that1981). above the each 5 sample % threshold consists of of the a single age population (Galbraith, 5 5 20 20 15 25 25 10 15 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 1 C − ◦ C Ma 5.6) Ma ◦ + C is placed ◦ 6.1 − 5.2) Ma (gneissic + 4.8 − 10 Ma) that overlaps with + 9 − C between 86 and ca. 68 Ma in C as defined by unconformable ◦ ◦ 2.7) Ma and a mean track length of 240 − < 3.1 + from 21 to 7 Ma; and (iii) from below 80 3086 3085 1 − C Ma ◦ C as defined by the closing temperature of zircons (e.g. Reiners ◦ , Fig. 7d) not older than Pliocene (Fig. 10c). temperatures 2.33 µm for sample 09-055 (Fig. 10a and b). The best-fit model gave a goodness ± denudation of Pelagonia On the regional scale, marine conditions were installed over the Pelagonian and the The increase of detritus at ca. 66 Ma (Fig. 3) marks the end of the 20–30 Ma long HeFTy calculated an AFT age of 19.5 ( boulder of sample 10-128),time overlaps between the cooling, depositional erosionsediments age and within are deposition error. very The indicateserosion. short The coarse, fast gneissic lag denudation. suggesting clasts Thecatchment and short to clastic the be rudists-bearing in transport the olistolites nowage distances constrain eroded as southeastern the and northern Pelagonia, sediment which Pelagonia has mechanical during (Fig. a similar 11b). thrust cooling Abrupt migration and thatAVAZ rapid (Mercier first cooling and buried at Vergely, 1994) the ca. and ca. 681956; then Ma 70 Ferriére the Ma occurred et 40–38 syn-orogenic Ma al., External mass 2004). Hellenides Thrusting flows (Brunn, was of accompanied the by blueschist metamorphism AVAZ until 66 Ma, starting from anCenomanian unconformity and variable in the space Early andto time Aptian between a (100–80 the Ma). long Deepening history of of the residence basin at corresponds temperatures between 102 Ma, which is the10-029, upper and 68 % 93.5–90 Ma, confidence which interval is of the the ZFT erosional age unconformity. of sample (youngest detrital population of sample 10-130) and at 67.4 ( the age of the unconformity. As a consequence, cooling below ca. 240 period of regional cooling and sedimentation. The ZFT age at 68 ( 3 Discussion 3.1 Detrital fission-track ages of theIn the western studied area, AVAZ: the low-grade 68unconformably AVAZ imbricates Ma by (sample marine 10-029) abrupt have sediments been between covered andthese 93.5 and imbricates fast 90 Ma. at The 92.2 ZFT Ma cooling has age of a large uncertainty ( northern Pelagonian basement, at 80Rhodope Ma (Fig. in the 1b). eastern This AVAZ showsexternal and orogenic post-collisional at pile 72 cooling Ma throughout and in the thermal western late subsidence Cretaceous of (Fig. the 11a). between 27 and 21 Ma, (ii) 1–3 12.59 of fit index (GOF) of 0.96The for the inverse model age, modeling and(Fig. of of 0.97 10), for the the from track track lengths which (Fig. lengths we 10a). can resulted roughly in estimate three-steps cooling cooling rates history of: (i) 20–40 t-T-paths were forcedconfidence to interval (CI) cross from ZFT two agesbetween of 260 fields the and same 220 (Fig. sample) in 10a): the temperature (i) window from 20 tocoal 26.6 Ma and (95 % lacustrineRadix sediments Auriculata (Steenbrink et al., 2006) containing gastropods (art to surface temperatures in 2–4 Ma between 7 to 3 Ma. Thermal history reconstructionslengths were with performed the HeFTy using computer program inversemodel (Ketcham, modeling 2005) of according of (Ketcham to the the etsample annealing AFT 09-055 al., was 2007). thefor Due only statistical one to validity. that the As showedannealing discussed high enough behavior. in Taking U-content horizontal into Sect. confined account of 3.2, tracks thiswhich its complexity, (54) these we all apatites apatite performed resulted several grains (Fig. models, inFig. have 9), a a 10. consistent complex This thermal history model exemplified represents by the the model simplest shown case in of a single-ageand population. Brandon, The 2006),basement (ii) at from surface temperature) 7 between to 30 3 to Ma 0 (the time of exposure of the Pelagonian 2.3.3 Inverse modeling of fission-track lengths and estimate of closure 5 5 20 25 10 15 20 10 15 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | C ◦ erence between ZFT ects and extent were C to the surface. E–W ff ◦ ff ) at this time, the slab interface was at ca. ◦ 3088 3087 Ar on white micas (Fig. 11b, Schermer et al., C throughout the Eocene (Fig. 11b and c). / ◦ 3.4 Ma) AFT age of sedimentary sample 10-128. + 3.1 − C of the metamorphic western AVAZ imbricates between 102 ◦ Oligocene-to-Miocene extension Cooling below 240 and 93–90 Ma, of northern Pelagonia between 86 and 68 Ma, of the eastern i. Two mechanisms are envisaged for the 33–16 Ma extension in central-eastern constrained with ZFT(Fig. and 11): AFT ages recording protracted cooling events as follows normal faults cutting the4, lacustrine sediments and demonstrate 10c). recent500 m Footwalls extension (Figs. and of 3, were these(Fig. carved faults 6). by uplifted Therefore, rivers7 the Ma the in lacustrine (Fig. conspicuous a 11e). sediments relief These concave-uphorizontal more displacement E–W shape of in faults ca. than typical 20 the have kmare for (van been central Hinsbergen interpreted coeval active and Schmid, Pelagonia as and uplifting 2012) because sinistral was parallelour they strike-slips geological to built with map the after and sinistral directstrike observations North slip of movement Anatolia fault (Fig. striations fault 4).50 contradict km (Fig. Furthermore, any graving 11e). significant the the large Nevertheless, attests distribution intra-montane regional of basins N–S normal extension of faults rather Kosani over than and inferred, localized Ptolemais strike (Fig. slip faulting. 11e) tangibly 4 Conclusions Several compressive and extensive events occurred fromin the Mesozoic the to Pelagonian the Cenozoic and the adjacent AVAZ. Their late thermal e and north-easternmost thermalslab. expression of the southward rollback of3.3 the Hellenic Pliocene cooling and uplift During the Late Miocene–Pliocene lacustrine sedimentsbasement locally covered of the Pelagonian the studiedused to area constrain attesting the inverse exposure modelingafter ca. of after 7 the Ma 7 FT from Ma. lengths, the which These upper AFT discloses data partial rapid retention cooling have zone at been ca. 80 3.2 Cooling and exhumation of the central-eastern Pelagonian basement:New late ZFT andcrystalline rocks AFT of central-eastern ages Pelagonia. The indicate small age Late di Oligocene–Early Miocene cooling of the 1990). During the thermal overprint andPelagonia relaxation cooled of below this 240 compressional and event, western 110 and AFT data (locally thethe 65 track % lengths confidence suggest interval overlaps), fast and and inverse spatially modeling uniform of cooling from ca. 240 to ca. 80 dated between 61 and 42 Ma with Ar extension during southward rollbackBrun of and the Faccenna, 2008) Hellenic after slabtrench the (e.g. of Eocene–Oligocene Le compression. the At Hellenic Pichon ca. subduction etlocated 15 was Ma al., at already the 1979; ca. migrating westward 200 km over2011). 80 from km Assuming the and a was central-eastern slab Pelagonia with (Royden low and angle Papanikolaou, (30 Pelagonia: (i) localunderthrusting extension of above an the antiformal External stack Hellenides duplex during (Ferriére continuous et al., 2004), (ii) distributed between 24 and 21 Ma. In thesource absence (Schenker of et Late Oligocene–Early al., Miocene 2014),reactivated advected heat top-to-the this E–NE fast shear cooling zone hints atand to the 11d). eastern tectonic This margin denudation normal of along thereset shear the Pelagonia AFT zone (Figs. ages 5 now in separates thein ca. hanging the wall 68 Ma footwall from (Fig. detrital 24–20.7 Ma 5). ZFTincorporate ZFT In and and the the 32.7 22.9–16.9 hanging Ma Ma reset wall, AFT 32.7This extensional ages suggests tectonic ( that slices extension (Fig. in 11c the and AVAZ started d) even earlier, at ca. 33 Ma. 115 km below central-eastern Pelagonia.unrealistic, Because hypothesis a duplex (i) of is 115 km discarded. is Therefore, mechanically the 33–16 Ma cooling is the oldest 5 5 25 10 15 20 20 10 15 25 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ) (e.g. . These two Radiolitid C from 102 Ma ( ◦ . Although none ect lasted until ca. ff Durania . The 30–20 Ma-long and Plagioptychid is in the Upper Albian to the and (iii) Durania C of the Pelagonian basement at about 68 Ma 3090 3089 ◦ during Pliocene-to-recent, normal faulting in C ◦ Radiolitidae ), (ii) erent tectonic levels in the footwall of westward migrating ff C of the western AVAZ from 33 Ma and between 240 and ◦ Radiolitid ( with prominent ornaments in the outer layer Durania C of the central-eastern Pelagonian basement from 24 to 16 Ma ◦ AVAZ at 80 Maheterogeneous and regional of coolingCretaceous western is marine contemporaneous Rhodope basin(s) withnappe at covering pile subsidence formed 72 since Ma at of 130–110 100 Ma. Ma Late theAbrupt and external rapid cooling zones below 240 of the due to erosional denudation40 Ma during according thickening. to Its ZFT(cf. thermal and Fig. AFT e 11b). in western and eastern Pelagonia,Cooling respectively below 120 80 zones cooled from di normal faults with top-to-the-NEattributed to sense rollback of of the shear Hellenic (Fig. slab. post-7 11c Ma and cooling d). Extension below is 80 central-eastern Pelagonia (Fig. 11c). Radiolitidae Durania (Radiolitid) ii. ii. i. A shell fragment shows a multi-layered structure with a dark inner and a complex The shells consist of an internal thin layer and an external polygonal mesh, iv. iii. representing a traversepolygonal section (mostly through hexagonal) shell a ornament Rudist of valve the (Fig. outer A1b). layer The is regular characteristic Maastrichtian, even without anot regular typical outer for layer the (like UpperCenomanian Cretaceous the (e.g. Genus. Cobban shell This et in al., specimen Fig. 1991). is A1a), probably not which older is than outer layer. Thispart outer and layer a haslenticular 3 mm a structures thick ca. are lenticularon the 1 structure cm the expression, in surface thick in of the cellular transverseanother the external shell, section, shell, structure part which in of probably in this (Fig. was fineand case attached A1a). the the regular adjoining to regular The internal fine those riblets it. external outer The from ribletsCobban cellular a characterize et texture a superficial al., of fragment fragment 1991). of the In of need outer order layer to to observe confirm the thisthe absence generic identification, outer of however, a shell we ligamentary would layer,posteroventral as infolding flank; on well the unfortunately, as dorsal none distinctfragment. inner radial of The margin bands these of most with parts abundant finer of ribbing occurrence the on of shell its external is visible in this of these genericthe identifications Rudists can show independently yet theexistence be of same a lower considered carbonatic stratigraphic platform secure boundary. in This without the fixes Mid-Late-Cretaceous. the closer study, Appendix A: Descriptionsedimentary sequence of Rudist inLenticular or olistolites blocky olistolites of of recrystallizedand limestone the benthic contain Rudist, Foraminifera. Oyster, Upper Corals Threegenus: Rudists (i) Cretaceous show a post-Cenomanian to Maastrichtian The complex low-temperaturepreserved history the record of of the a Pelagonian long residence basement at and temperature the below 240 AVAZ onwards. Thus, since thatcrustal-scale time burial processes these invoking elevated tectonic thermaltectonic condition. units In context, have this the upper-crustal not combined beendata use was involved of essential in to fission-track unravel major dating, polyphaseinterval. tectonic structural processes and extending over stratigraphic a long time- 5 5 25 15 20 10 10 15 20 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | plagioptychids range from the upper Turonian to the . The first representative, with a poorly 3092 3091 plagioptychids Radiolitidae We thank the following people for help with fossil identification: P.Hochueli Plagioptychid iii. The outer valve layer displays radial lines that are interpreted as pallial canals 663–676, 1996. Planet Sc. Lett., 272, 1–7, 2008. Macédoine Occidentale, Ann. Geol. Pays. Hellen., 7, 1–358, 1956. structural data in2012. the geochronological frame, Journal of therocks Virtual in Explorer, the 42, Idaho-WyomingGeologists, thrust 44 78, belt, 1613–1636, pp., 1994. AAPG Bulletin-American Association of Petroleum kinetics: I. Experimental results, Am. Mineral., 84, 1213–1223, 1999. (Des Moulins, 1826)Geological Survey in Bulletin for the 1985, D1–D8, Upper 1991. CretaceousCrustal Cooling Greenhorn of the Limestone OlympusExtension Range Over in Propagation (Northern of Colorado, Aegean): the Major US North Role Anatolia of Fault Hellenic Zone, Back-Arc the Terra Nova, Upper 2014. Aptian of thePalaeontology, 49, Mediterranean 769–794, region and 2006. the origin of the rudist familyN., Radiolitidae, and Gardin, S.: Geologicpiggyback evolution Meso-Hellenic and basin, geodynamic Greece, controls Bull. of Soc. the Géol. Tertiary intramontane Fr., 175, 361–381, 2004. métamorphisme HP/BT:Greece, les XXX/1, 175–192, “schistes 1988. bleus” tertiairesrecommendation Thessaliens, for the Bullet. standardization of fission-trackNucl. Geol. dating Tracks Rad. calibration and Meas., Soc. data 17, reporting, 233–236, 1990. rocks from thewesternmost Pelagonian Internal Zone, Hellenides, Int. Greece: J. Earth constraints Sci., on 96, 639–661,Helv., the 2007. 65, 1007–1118, pre-Alpine 1972. evolution of the Geol. Helv., 37, 226–227, 1945. de la bordure orientale deGreece, la XXX/1, double 105–114, Fenêtre 1994. du Païkon (Macédoine, Grèce), Bull. Geol. Soc. Brandon, M. T.: Probability density plot for fission-track grain-ageBrun, samples, J. Radiat. P. and Meas., Faccenna, 26, C.: Exhumation of high-pressure rocksBrunn, driven by J.: slab rollback, Contribution Earth à l’étudeBurg, Géologique J.-P.: du Rhodope: Pinde from Mesozoic septentrional convergence et to d’une Cenozoic partie extension. Review deBurtner, of R. la L., petro- Nigrini, A., and Donelick, R. A.: Thermochronology of lower CretaceousCarlson, W. source D., Donelick, R. A., and Ketcham, R. A.: Variability ofCobban, apatite W., fission-track annealing Skelton, P., and Kennedy, W.: Occurrence of the rudistid DuraniaCoutand, I., cornupastoris Walsh, M., Louis, B., Chanier, F., Ferriére, J., and Reynaud, J.-Y.: Neogene Upper- Fenerci-Masse, M., Massr, J. P., Arias, C., and Vilas, L.: Archaeoradiolites, a newFerriére, genus J., from Reynaud, J.-Y., Pavlopoulos, A., Bonneau, M., Migiros, G., Chanier, F., Proust, J.- Galbraith, R. F.: On statistical modelsGodfriaux, for I., fission track Ferriere, counts, Math. J., Geol., and 13, 471–477, Schmitt, 1981. A.: Le développementHurford, en A. contexte J.: International-Union-of-Geological-Sciences continental subcommission d’un on geochronology for rudists of the family (the latter consists of thecanals two and calcitic the layers cavity with in no the internal internal structure). layer The are form typical of for the the left valve of separated by tightly bifurcatinglayer laminae. with Valve no inwards, there discerniblelighter is internal layer a textures, with followed 1 mm by noprobably white a constituted discernible calcitic 3 by mm internal detrital grey components, textures hinting layer (Fig. to and cavity A1c a fill 2 and in mm the d). inner-valve layer The grey layer is developed cellular layer, iscelluloprismatic Albian (Fenerci-Masse outer et al.,Cenomanian layer 2006). up to The (as the more Maastrichtian prominent in forms (e.g. Fenerci-Masse Fig. et al., A1b) 2006). is typically well developed in the (Fig. 7 of Skelton, 2013). The Maastrichtian (e.g. Skelton, 2013). Acknowledgements. (gastropod), D. Bernoulli and S. Spezzaferri (foraminifera), P. Skelton and I. Stössel (rudists). References Anders, B., Reischmann, T., and Kostopoulos,Bernoulli, D.: D. and Zircon Laubscher, H.: geochronology The of palinspasticBolli, problem H.: basement Zur of Stratigraphie the der Hellenides, Oberen Eclogae Kreide Geol. Bonneau, in M., den Godfriaux, höheren I., Moulas, helvetischen Y., Decken, Fourcade, Eclogae E., and Masse, J.: Stratigraphie et structure 5 5 10 15 20 25 30 10 15 25 20 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 3094 3093 Ar and zircon and apatite fission track dating, Geol. Soc. Greece Bull., 34, 91–95, 2001. / (Internal Hellenides, Macedonia, Greece), Bull. Geol. Soc. Greece, XXX/1,and 115–120, the 1994. Republic of Macedonia, GeowissenschaftlichenTübingen, Fakultät, Tübingen, Eberhardt-Karls-Universität 195 pp., 2003. and structural investigations ofK the northern Pelagonian crystalline zone – constraints from des Pays Helléniques, 37, 495–514, 1997. in the Hellenides, Lithos, 108, 262–280, 2009. The 13 May 1995 Westernresults, Macedonia, Terra Greece Nova, 7, (Kozani-Grevena) earthquake 544–549, – 1995. preliminary- Annu. Rev. Earth Pl. Sc., 34, 419–466, 2006. Jungpaläozoikums und dessen EinordnungHelv., 38, im 221–313, griechischen 1945. Gebirgsystem, Eclogae Geol. Hellenic arc, Geochem. Geophy. Geosy., 12, doi:10.1029/2010GC003280, 2011. Mesoproterozoic magmatism to collisional Cretaceousthe anatexis: Pelagonian tectonomagmatic Zone, history Greece, of Tectonics, 1552–1576, 2014. Alpine orogeny, Mt. Olympus region, Greece, J. Struct. Geol., 15,continental-crust, 571–591, Mount 1993. Olympos Region, Greece, Tectonics, 9, 1165–1195, 1990. of the Mesozoic Vardar Ocean: evidence from the Pelagonian and Almopias zones, Exploration, Greece, 1991. Cretaceous carbonate rocks of theregion, Circum-Rhodope NE Belt Greece), (Chalkidhiki Cretac. Peninsula Res., and 52, Thrace 25–63, 2015. Büttner, D.: Structure and geodynamicHellenides, evolution of edited the Aegean by:Verlagsbuchhandlung, Stuttgart, region, Cloos, 537–564, in: 1978. Alps, H., Appenines, Roeder, D.,Rev. Mineral. and Geochem., 58, Schmidt, 275–314, 2005. K., E.of Schweizerbart’sche fission-track annealing in apatite, Am. Mineral., 92, 799–810,architecture 2007. and kinematicsHellenides, of Austr. deformation J. Earth of Sci., the 103, 4–28, northern 2010. PelagonianAmynteon Nappe (W. Macedonia), Pile Mineral in Deposit22–34, Research, the 1979. Natl. Instit. Geol. Mining Res., 5–14, Upper Cretaceous exhumation ofPeninsula, northern the Greece), western Tectonics, 33, Rhodope 1–20, Metamorphic 2014. Province (Chalkidiki Mart, Y., Mascle,subduction J., to Matthews, transform D.,Planet motion Sc. Mitropoulos, Lett., – D., 44, seabeam 441–450, Tsoflias, 1979. survey P., of andexhumation the Chronis, of Hellenic metamorphic G.: rocks trench in From North system, Aegean, Earth eEarth, 2,Tectonophysics, 456, 51–63, 147–162, 2007. 2008. interpretation of the Amynteon-Ptolemaidapetrographic composition, lignite Int. deposit J. in Coal Geol., northern 56, Greece 253–268, based 2003. on its Papanikolaou, D.: Timing of tectonic emplacement of the ophiolites and terrane paleogeography Pavlides, S. B., Zouros, N. C., Chatzipetros, A. A., Kostopoulos, D. S., andReiners, Mountrakis, P. W. D. M.: and Brandon, M. T.: UsingRenz, thermochronology C. to and understand Reichel, orogenic M.: erosion, Beiträge zur Stratigraphie und Paläontologie desRoyden, Ostmediterranen L. H., Papanikolaou, D. J.: SlabSchenker, F. L., segmentation Burg, and J.-P., Kostopoulos, D., late Moulas, E., Cenozoic Larionov, disruption A., and of von Quadt, the A.: From Schermer, E. R.: Geometry and kinematicsSchermer, of continental E. basement R., deformation Lux, during D. the R., and Burchfiel, B. C.: Temperature–time history of subducted Naeser, C. W.: Fission-track dating, in:Papanikolaou, US Geological D.: Survey The Open File tectonostratigraphic Report, terranes 76–190, 1976. of the Hellenides, Annales Géologiques Sharp, I. R. and Robertson, A. H. F.: Tectonicsedimentary evolution of the western margin Mercier, J. and Vergely, P.: Is the Païkon MassifMost, a T.: tectonic Geodynamic window evolution in of the the Axios-Vadar Eastern zone? Pelagonia zone inMost, the T., Frisch, Northwestern W., Dunkl, Greece I., Kadosa, B., Boev, B., Avgerinas, A., Kilias, A.: Geochronological IGME: Kolindros Sheet, Geological Map of Greece 1 : 50Ivanova, 000, D., Bonev, Institute N., of and Geology Chatalov, A: and Biostratigraphy Mineral and tectonic significance of lowermost Jacobshagen, V., Dürr, S., Kockel, F., Kopp, K. O., Kowalczyk,Ketcham, G., R. Berckhemer, A.: H., Forward and and inverse modelingKetcham, of R. low-temperature A., Carter, thermochronometry A., Donelick, data, R. A., Barbarand, J., and Hurford,Kilias, A. J.: Improved A., modeling Frisch, W., Avgerinas, A., Dunkl,Koukouzas, C. I., N., Kotis, Falalakis, T., Ploumidis, G., M., and and Metaxas, A.: Gawlick, Coal Exploration H. of Anargiri J.:Kydonakis, Area, K., Alpine Gallagher, K., Brun, J. P., Jolivet,Le Pichon, M., X., Gueydan, Angelier, F., J., Aubouin, and J., Kostopoulos, Lyberis, D.: N., Monti, S., Renard, V., Got,Lecassin, H., R., Hsu, Arnaud, K., N., Leloup, P. H.,Lock, Armijo, J. R., and and Willett, Meyer, S.: B.: Low-temperature Syn-Mavridou, thermochronometric and E., ages post-orogenic Antoniadis, in P., fold-and-thrust Khanaqa, belts, P., Riegel, W., and Gentzis, T.: Paleoenvironmental 5 5 10 15 20 25 30 10 20 15 25 30 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | y 5.95 5.95 5.95 5.96 5.95 5.95 5.96 14.96 14.96 14.96 14.96 12.53 12.53 12.53 -CN ± ± ± ± ± ± ± ζ ± ± ± ± ± ± ± , total s local N value for σ 2 + 2 χ σ 2 − ) pooled age 2 χ ( P i N ] [%] 68 % CI [Ma] 2 − 06 3838 2.8 19.5 1.4 1.5 335.93 06 605 25.4 24 1.7 1.9 142.57 06 67306 99.6 97106 66.4 16.1 94706 17.6 94.5 1577 2.4 68.906 2.7 2.2 18.5 335.93 633 2.5 18.506 23.2 335.93 2.2 1091 2.6 1.7 13.7 22.9 335.93 1.9 339.54 32.7 2.8 3.2 3.1 339.54 3.4 339.54 06 684 18.5 23.1 1.6 1.7 142.57 06 427 95.8 24 1.9 2.1 142.57 06 568 61.6 20.7 1.5 1.7 142.57 06 156 25.3 92.2 9 10 142.57 06 431 15 67.4 4.8 5.2 142.57 06 376 1.7 76.2 5.7 6.2 142.57 + + + + + + + + + + + + + + i ρ ), probability of obtaining 2 s χ N 1). ( − P ] [tracks cm 2 − 05 326 6.59E 06 581 6.39E 04 4805 1.24E 6905 2.57E 7305 3.46E 131 6.30E 05 6905 2.03E 131 3.13E 06 666 8.27E 06 429 4.72E 06 479 6.02E 06 447 2.76E 06 901 4.41E 06 881 1.93E + + + + + + + + + + + + + + s ρ 3096 3095 ] [tracks cm induced and dosimenter track densities on external 2 − 06 5.60E 05 6.14E 06 8.84E 06 1.83E 06 2.67E 06 5.23E 06 2.21E 06 3.76E 05 8.05E 05 4.75E 05 5.08E 05 7.90E 05 9.22E 05 4.52E d + + + + + + + + + + + + + + d ρ ρ and i ρ number of crystals = [m] grains [tracks cm 320 27 1.37E 240 38 1.34E 160 25530 1.23E 20 1.60E 320 20 3.33E 250 20 3.36E 760 16 4.56E 530 21 4.55E 440 27 4.59E y 1330 20 3.51E 1020 241000 1.47E 1200 23 25 1.42E 1.31E 1020 20 3.45E total numbers of tracks; d 00 00 00 00 00 00 00 00 00 00 00 00 00 00 00 00 00 00 00 00 00 00 00 00 00 00 00 00 N 53.8 18.5 39.5 19.4 50.8 34.4 33.6 26.7 53.8 39.5 19.4 00.7 26.7 10.4 0 0 0 0 0 0 0 0 0 0 0 0 0 0 11.6 45.4 21.4 50.6 43.3 37.0 15.3 45.1 11.6 21.4 50.6 10.8 45.1 37.6 0 0 0 0 0 0 0 0 0 0 0 0 0 0 05 06 09 03 06 06 11 12 05 09 03 16 12 13 ◦ ◦ ◦ ◦ ◦ ◦ ◦ ◦ ◦ ◦ ◦ ◦ ◦ ◦ 19 23 21 19 16 13 24 27 19 21 19 26 27 27 ◦ ◦ ◦ ◦ ◦ ◦ ◦ ◦ ◦ ◦ ◦ ◦ ◦ ◦ and i N40 E022 N40 N40 N40 N40 N40 N40 N40 E022 E022 E022 E022 E022 E022 E022 N40 E022 N40 E022 N40 E022 N40 E022 N40 E022 N40 E022 N , spontaneous track densities measured in internal mineral surfaces; s ρ Pooled ages calculated using dosimeter glass CN5 and CN1 for zircons and apatites, ment/granodioritic gneiss ment/leucogneiss ment/leucogneiss ment/granodioritic gneiss ment/leucogneiss ment/granodioritic gneiss ment/granodioritic gneiss blockCretaceous inconglomerate Upper ment/granodiorite ment/leucogneiss ment/granodioritic gneiss Jurassic–Creta- ceous conglomerate blockCretaceous inconglomerate Upper ceous conglomerate northern Greece, in: Tectonic DevelopmentRobertson, of the A. Eastern H. Mediterranean F., and Region, Mountrakis, edited D., by: Geological Society, London,Invertebrate 373–412, Paleontology”, 2006. Caribb. J. Earth Sci., 45, 9–33, 2013. Washington, DC, 1995. Miocene to Early Pliocene depositionalBasin, history NW of Greece: the Interplay intramontane Florina-Ptolemais-Servia238, between 151–178, orbital 2006. forcing and tectonics, Palaeogeogr. Palaeocl., the Mesohellenic Trough andexhumation the of source Pelagonian areas, zone Int. in Geol. NW Rev., 52, Greece: 223–248, cenozoic 2010. accretion and tectonics extension since and the Eocene, Tectonics, 31,10.1029/2012TC003132 , doi: 2012. la Turquie d’Europe, Bull. Soc. Géol. Fr., 2, 454–475, 1853. Earth Sciences, Swiss Federal Institute of Technology Zurich, Zurich, 210rocks of pp., 2009. High Piera, Greece, in: 6th Colloq. Aegean Region, Athens, 1, 269–280, 1977. apatite FT ages 09-055 Pelagonian base- sample unit/rock typezircon FT age 09-032 coordinates Pelagonian base- elevation No. of 09-098 Pelagonian09-108 base- Pelagonian base- 09-120 Pelagonian09-121b base- Pelagonian base- 10-090 Pelagonian base- 10-128 AVAZ/gneissic 09-055 Pelagonian base- 09-098 Pelagonian base- 09-108 Pelagonian base- 10-029 AVAZ/late Upper 10-128 AVAZ/gneissic 10-130 AVAZ/Upper Creta- degrees of freedom (where respectively. Table 1. number of spontaneous tracks; mica detectors; Skelton, P. W.: Rudist classificationSpear, for the F. revised S.: Bivalvia Metamorphic volumesSteenbrink, of J., Phase Hilgen, the F. Equilibria “Treatise J., on Krijgsman, and W., Wijbrans, Pressure–Temperature–Time J. Paths, R., andVamvaka, Meulenkamp, A., J. Spiegel, E.: C., Late Frisch, W., Danisik, M.,van and Hinsbergen, Kilias, D. J. A.: J. and Fission Schmid, track S.Viquesnel, data M.: A.: Map Résumé from view des restoration observations géographiques of et Aegean-West géologiques Anatolian Wüthrich, faites, E. en D.: Low 1847, Temperature Thermochronology dans of the Northern Aegean RhodopeYarwood, Massif, G. A. and Dixon, J. E.: Lower Cretaceous and younger thrusting in the Pelagonian 5 20 10 15 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 54 44 47 87 53 52 30 km 30 km Most, 2003 Most, 2003 Wütrich, 2009 detrital apatites

41° 58 56

51 49 41° conmplex Rhodope Northern two extensional metamorphic Coutand et al., 2014 NE Vamvaka et al., 2010 Vamvaka et al., 2010 Vamvaka 50 57 72 Kydonakis et al., 2014 56 [Ma] [Ma] Aegeansea Aegeansea =

68 Thessaloniki

54 Southrn Rhodope conmplex Rhodope Southrn . Errors of the FT ages between 1.6 8 9 zircon fission track ages zircon fission

in apatite fission track ages Rhodope as <20 Ma Serbo-Macedonian b 10 (c) 0 10

s Olympos window

o 60 808 i 12 Ax 10 Thessaloniki

16 32

11 14 Paikon window 12 Paikon marine unconformity 30 35 31 22 11 33 18 76 49 15 51 22° 22° 47 AVA 49 52 29 41 28 51 23 62 ne 42 >20 Ma 31 25 46 71 o e Late Cretaceous/Early Terciary window in the 35 66 z 43 n the westernmost continental fragment of the

n o 37 a z 42 ni gh n NW 40 82 o u a

o i = 74 41 66 g r 75 n 71 la t o Pe c g = 3098 i a 3097 l 27-105 86 n 33 Pe 36 66 e

83 l 40

l 21-120 he >60 Ma extension AFT Pelagonia

63 o SE

s 32

e and AFT ages

70 <60 Ma M 80 37 43

45 Pindos

29 49 51 29 32

48 37 Corinth

(b) Gavrovo-Tripolitza 25 53 39 s s

31 61 o o

d 35 d

n Ionian

Pi Pin Paxos E Hellenides compression ZFT sea Aegean Cyclades SW 40 80 60 20 Sofia 120 100 140 160 [Ma] Rhodope Thessaloniki 20° 20° Athens 41° 41° AVA Tertiary basins Tertiary zone Serbo-Macedonian External Hellinides Ophiolites units Axios/Vardar/Ambelakia Pelagonian zone Mesozoic carbonate platforms Mesozoic basins c) b) Pelagonian zone Mediterraneansea a) Internal Hellenides: External Hellenides: 20° 24° 41° 37° Tirana Tirana overview map (centre left) and tectonic maps of the Hellenides (modified after Compilation of zircon and apatite FT ages (references in Fig. 1) with main tectonic typical localities of the first deposition of the syn-orogenic mass flow deposits) according to = core complexes) according to Burg (2012) and Ivanova et al. (2015). AVAZ) tectonism according toand Bonneau transgressions et al. ofRhodope) (1994); Serbo-Macedonian and Mercier Southern ( and and Vergely Northern (1994); Rhodope tectonism Complexes ( Papanikolaou (1997); Pelagonia unconformitySchenker et and al. tectonic (2014), according respectively; to Paikon ( Kilias et al. (2010); Figure 2. events. From southwest to northeast: tectonism( of Paxos, Ionian, Gavrovo-Tripolitza and Pindos Figure 1. (a) Burg, 2012) with publishes ZFT ages and 11 Ma. DetritalPelagonia, AFT ZHe data and are AHe reported agespattern. as of Working Countand area the (2014) shown range in similar of the to, single-grain black respectively, ZFT frame. ages. and In AFT the ages southern Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | E 10-029 confidence σ marble (middle Lower Cretaceous) conglomerate with gneiss and rudist bearing blocks ZFT 92.2 (83.2-102.2)

10-128

ZFT 67.4 (62.7-72.6) AFT 32.7 (29.6-36.1)

t i

m r

n u 10-130 flysch/phyllitic sequence (U. Jurassic- L.Cretaceous) and quartzites pebbly mudstones and undifferentiated undifferentiated Mélange zone Axios/Vardar/Almopia units Axios/Vardar/Almopia ZFT 68 (61.9-73.6) (youngest detrital pop.) (youngest Upper Cretaceous transgressive marine sediments Upper Cretaceous transgressive marine globotruncana 3100 3099 serpentinite/ ophicalcite marl ( )

Axios/Vardar/Ambelakia units Axios/Vardar/Ambelakia Pelagonia units Pelagonia orthogneisses amphibolites Tectono-stratigraphic column of the Pelagonian zone and schematic ﬁeld Location and age of FT samples (pooled age and the 68 % conﬁdence interval) on Pelagonia zone ( Pumonata: Art Radix auriculata) ( Pumonata:

Gilbert delta sequences leucocratic gneiss marbles erosion < 7 Ma transgressive lacustrine sediment Figure 4. the geological map (located inFor Fig. the 1) detrital of the zircons eastern of Pelagonian sample gneiss 10-130, dome the Schenker range (2014). of single-grain ages is reported. interval. The displacement of the normal fault in the AVAZ is unknown. Figure 3. relationships of the AVAZ with sample location and FT ages. FT ages shown with 2

a r 10-090 t

o i s s

e t i t a

p k a c a r t

i z A’ 09-098 09-098 09-032 b E 09-032 N Concave-up hillslopes in valleys in the footwall of 3102 3101 (b) Erosion features on the fault scarp. On the horizon the Kozani 09-055 09-055 (a) ). 00 50 0 B 59 5 ◦ 09-108 09-120 09-120 09-108

[Ma] 3

10 100 m] 100 [ 20 30 x 70 Topographic expression of the recent faulting along the Servia fault (GPS: , E021 00 AFT and ZFT ages along three transects across the eastern Pelagonia gneiss dome. S a 37 0 10 ◦ apatite FT age apatite FT zircon FT age zircon FT zircon FT ages zircon FT confidence interval

Pooled ages with 68 %

Single-grain distribution

100 m] 100 [ SW x 9 N40 Figure 6. plane (elevation ca. 280 m)at ﬁlled elevations with of Pliocene ca. to 800 recent m lacustrine in the sediments footwall. which are found the Servia normal fault, suggesting recent and fast uplift. Figure 5. For the location of the transects see Fig. 2. Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Radix

66 Ma)

number

RE [%] RE > [%] density = 6 2 40 30 20 n felsic clast, = 0.2 mm 1 cm [Ma] sedimentation Zircon age-distribution p1 ZFT age p1 ZFT (b) Late Cretaceous ( Pliocene to recent art p1 = 68 (+5.6 -6.1) Ma p2 = 179.6 (+42.8 -56) Ma observed (c) (d) Helvetoglobotruncana helvetica Metamorphic conglomerate of sample Turonian d 10-130 (b) (a) n = 27 b b) 30 60 120 240 3104 3103 vc 0.1 mm relative error in %) calculated with Binomﬁt (Brandon, 0.5 mm = chl [Ma] volcanic clast. = 92.2 (+10 -9) Ma observed fc cc population, RE = p quartz and vc in the marls incarlated with sample 10-128. = sedimentation ZFT age ZFT

afs qz n = 16

Microphotographs of thin-sections.

10-029 Zircon age-distribution of grain-supported conglomerate 10-029 belonging to the

found in the lacustrine sediments. Age density histograms for “detrital” FT ages with distribution curves ( RE [%] RE density [%] density 40 80 160 320 8 2 a c a) 40 30 20 (a) feldspar, qz = 1996). Upper Malm–Lower Cretaceous “ﬂysch” of the AVAZ (IGME, 1991). of grain measured, from unmetamorphosed, Late Cretaceous conglomerate (10-130). Figure 8. Figure 7. 10-029 withafs metamorphic chlorite (chl) in calcitic matrix. Other clasts: fc (93.5 and 90 Ma) in marls on the transgressive discordance. Globotruncana sp. Auriculata Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | E Normal fault in (c) U-concentration vs. ages; (a) W

age [Ma] c) Frequency 0.25 0.20 0.15 0.10 0.05 18 30 30 14 0.5) goodness-of-ﬁt indicate non-failure at 95 > Length [μm] Length b) track length distr. 3106 3105 20 age [Ma] 20 0 3 10 10 5 Ma) uncorformably covering the Pelagonia crystalline rocks ). < 00 sediments b) a) tectonized

0.05) and “good” (

accettable path (GOF = 0.05) path (GOF accettable = 0.5) good path (GOF (shown in (c)) (shown

] μm [ Dpar U [ppm] U > 80 60 40 20 2.1 1.9 1.7 1.5 33.5 100 0 Distribution of counted horizontal track lengths. best fit: data age = 19.5 (+3.1/-2.7) model age = 19.6 GOF = 0.96 data mean length = 12.59 ± 2.33 μm model mean length = 12.97 ± 1.91 μm GOF = 0.97 08 ◦ 21 (b) 24 18 15 12 9 6

T-t paths of sample 09-055 modeled with computer program HeFTy (Ketcham,

, E022 ZFT age 95% CI 95% age ZFT 00

t [Ma]

a) time-temperature history

°C] Plots of single apatite measurements of sample 09-055. [ T 0 40 80 49.4 120 160 200 240 0 19 ◦ Dpar vs. age. Figure 10. (a) 2005). The “acceptable” ( and 50 % conﬁdence interval,random respectively. Inverse t-T modeling paths. is based on simulation of 50 000 deltaic-lacustrine sediments ( (N40 Figure 9. (b) Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 3108 3107 ZFT and AFT thermal history of the Pelagonia from the Late Cretaceous with Figure 11. restored proﬁles. ZHearea. and Unit AHe patterns ages identicalLock neglected to and since Fig. Willett 1. nottectonic (2008). contacts. Conceptual homogenously Until cooling distributed ca. patterns 32 in Ma, along the cooling thrust homogeneous sheets and from parallel to the NW–SE Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 00 ); 00 ) in 31.2 0 26.7 0 27 ◦ bi-layered 12 ◦ (b) 1 cm 1 cm 022 ) 00 00 Plagioptychid 13.8 45.1 0 0 outer valve layer 13 27 ◦ ◦ cavity? 022 00 laminae 40.7 0 inner valve layer 27 ◦ inner valve layer inner valve ) (40 d b . 3109 1 cm (c) Durania 1 cm cellular structure showing an external layer with polygonal ornaments (40 inner valve layer Multi-layer architecture of a Rudist shell fragment ( (c) composite shell of a rudist ( ). Radiolitidae 00 c a 07.7 0 13 ◦ Sketch of the Rudist fragment shown in (d) Figure A1. (a) shell of the 022 a conglomerate, showing radial laminae in the outer-valve layer (40