Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ◦ erences 0 to 20

Open Access ff ∼ , 1 Discussions one ffi Solid Earth Solid , M. Ma 1 2 938 937 , C. G. Langereis 1 , and L. Sabato 2 counterclockwise vertical axis rotation of Adria. This result , M. Mensink 1 ◦ 8.7 ± , M. Tropeano 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, Utrecht University, Budapestlaan 4, 3584Dipartimento CD di Utrecht, Scienze the della Terra e Geoambientali, Universitá degli Studi “Aldo Moro” di provides no support forbetween the models Early invoking Cretaceous and significantkinematic Eocene. Africa–Adria The models Alpine rotation are and di Ionian bothmutually Basin exclusive. permitted end-member This apparent within enigmalowing the can conditions documented be (requiring solved rotation only futurethe range, if research) western one yet are or Alps are more satisfied: hasNeogene of (i) been the extension Neogene significantly fol- in shortening underestimated themuch in (by Ionian as as 420 Basin km); much has and/or as (iii) beenSouth a Adria 150 significantly major km); in underestimated sinistral Neogene (ii) strike-slip (by time. zone Here as has we decoupled present North five and alternative reconstructions of Adria counterclockwise. Here, we providefrom six new the paleomagnetic Lower poles Cretaceoussula from to Adria, (southern Upper derived Italy). Miocene(Italy), carbonatic These, units the in of Istria combination the peninsulaa with Apulian (Croatia), post-Eocene published penin- and 9.5 poles the from Gargano the promontory Po (Italy), Plain document orogens, and forms theHellenides. It is foreland connected of to the theMesozoic African plate oceanic Apennines, through lithosphere. the If Alps, Ionian the Basin, Dinarides,sition relative likely with motion relative and lower of to Adria Albanides- Eurasia vs. canary Africa be is conditions constrained known, through for its the the po- ranean plate reconstruction circuit, are of and obtained. the hard Kinematic bound- complexAfrica reconstructions kinematic interpreted for from history the the of Alps,lead Neogene the and to motion Mediter- from Ionian scenarios of Basin Adria involving and vs. vertical its surroundings, axis however, rotation predictions ranging from The first and foremost boundaryranean condition for region kinematic is reconstructions the ofreconstructions relative the motion Mediter- of between the Africa Atlanticplate and Ocean. position Eurasia, relative The constrained to Adria through the continental strongly curved block Central is Mediterranean in subduction-related a downgoing Abstract Solid Earth Discuss., 6, 937–983,www.solid-earth-discuss.net/6/937/2014/ 2014 doi:10.5194/sed-6-937-2014 © Author(s) 2014. CC Attribution 3.0 License. L. Spalluto 1 Netherlands 2 Bari, Via E. Orabona 4, 70125, Bari, Italy Received: 17 March 2014 – Accepted: 18Correspondence March to: 2014 D. – J. Published: J. 28 van Hinsbergen MarchPublished ([email protected]) 2014 by Copernicus Publications on behalf of the European Geosciences Union. Did Adria rotate relative toD. Africa? J. J. van Hinsbergen 5 25 15 20 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | er- ff of which can be accounted for ◦ 2 ∼ counterclockwise (ccw) rotation of Adria ◦ 20 940 939 ∼ There is no zone of intense compression between Adria and Africa, and Adria has Detailed kinematic reconstructions constitute a fundamental tool for advancing our Africa during the Neogene. GPS measurements suggest that at present, Adria moves it is crucial toent reconstruct approaches any to past this relativesea motions end, floor between is however, lead widely Adriaotte regarded to and et as Africa. contrasting al., Mesozoic 2011; Di results. Gallais (e.g., et Theimplying Catalano al., a Ionian et 2011; semi-rigid Schettino connection al., Basin’s and between 2001; Turco, Adria 2011;creasing Frizon and Speranza Neogene Africa de et shortening since al., in Lam- that 2012), the time. Alpsever, Eastward has (Schmid in- et been al., used 2013; to Schönborn,relative infer 1999), a to how- Neogene Eurasia (Ustaszewski etby al., African–Europe 2008), plate only motion. That would suggest that Adria was decoupled from been paleolatitudinally stable relative toically Africa several within hundreds paleomagnetic of error2004). bars kilometres) Because (of (e.g., the typ- motion Channell of et Adriadition relative al., to to Europe 1979; reconstruct would Rosenbaum be the the et central best al., boundary Mediterranean con- kinematic history since the Mesozoic, overthrust by these sinceare currently Neogene exposed time. in Tectonic2009; all Faccenna slices et circum-Adriatic al., of 2001; mountain Gaina the rangesStampfli et al., Adriatic (Bernoulli and 2013; Hochard, and Handy upper et 2009; Jenkyns, crust al.,and Stampfli 2010; and Martini, Schmid et Mosar, 2001; al., 1999; 2008; van Ustaszewskiseparated Hinsbergen et from and the al., Schmid, North 2008; 2012) African Vai the (Fig. passive Ionian 1). continental Basin margin To the by (Catalano oceanic2011; south, et lithosphere Speranza Adria al., et of is 2001; al., Frizon 2012). de Lamotte et al., 2011; Gallais et al., ates currently exposed onItaly, the the Apulia Istria peninsula peninsula andAdria Gargano of promontory is Croatia, of and in southern the aoverthrust Adige downgoing by Embayment the plate Apennines of position in theeast, relative the and southern west to although and Alps. all it the was surrounding Dinarides-Albanides-Hellenides originally in mountain in the an belts: overriding it plate position is in the Alps, it became European and African plates composed of essentially undeformed platform carbon- break-up of Pangea. Anental critical domain element of in Adria (Fig. Mediterranean 1). reconstructions Adria is is the a fragment conti- of continental crust intervening the understanding of the complexboundary geodynamics condition of adopted the by Mediterraneantions all summarized region. reconstructions in A is the common magnetic represented Eurasia–North by anomalies America–Africa the plate of relative circuitand the mo- based Sengör, Atlantic on 1979; Ocean marine DeweySavostin (e.g., et et Capitanio al., al., and 1989; 1986; Goes,which Gaina defined Seton 2006; et the area et al., Dewey generated 2013; al., and consumed Rosenbaum 2012; between et Africa Torsvik and et al., Europe 2002; al., since the 2012; Vissers et al., 2013), evolution that has made thefundamental concepts Mediterranean that region link instrumental surface innati deformation the et to development deep al., of mantle 2012; processesGovers and (Carmi- Cavazza Wortel, et 2005; al., JolivetSpakman, 2004; et 2000). al., Doglioni, 2009; 1991; Malinverno and Faccenna Ryan, and 1986; Becker, Wortel 2010; and The complex geodynamic evolution of theinated central Mediterranean by region convergent has been motionbeing dom- between accommodated the along African aof and discrete the European plate region plates. boundary, led Ratherzones, the to and than complex convergence to paleogeography being distributed accommodated overridingsince the plate along late shortening. segmented Eocene In subduction hascurved addition, formed subduction a subduction series roll-back zones of extensionalDoglioni and back-arc et basins associated al., and mountain strongly 1997;ter, Gueguen belts 2004; et Stampfli (e.g., al., and Dewey Hochard, 1998; et 2009; Jolivet Wortel et al., and al., 1989; Spakman, 2009; 2000). Rosenbaum It and is this Lis- complex or previously proposed kinematic reconstructions from the surrounding. 1 Introduction at 20 Ma that highlight the enigma: they fit the inferred rotation pattern from this study 5 5 25 15 20 10 25 15 20 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ccw ◦ clockwise ◦ 5 km thick sequence > cw rotation since 30 Ma ccw rotation of Adria rel- ◦ ◦ ccw early-late Cretaceous rotation ◦ cw rotation and a post-Eocene 30 ◦ 942 941 -scraped sediments now exposed in Calabria ff ccw rotation since the late Cretaceous (Márton and Nardi, ◦ Before the Calabrian subduction zone retreated away from Sardinia in the late Greater Adria was separated from Eurasia in the northeast by the Triassic Vardar, or Paleomagnetic data can provide useful quantitative constraints on the vertical axis In this paper, we present a new paleomagnetic study of the Lower Cretaceous to (Speranza et al., 2012). The Ionian abyssal plainforeland is of the the only central relativelyet Mediterranean undeformed subduction al., systems portion 2006; (Gallais that SperanzaRooke et serves et and al., as al., 2011; Rangin, the 2012). Hieke 2005)floor Given is and the likely very crustal oceanic in low thickness2012). nature, of The heatflow and age 7–9 (Pasquale very km of old et the (Chamot- (e.g.,Cretaceous Ionian al., Gallais (Dercourt Basin et 2005) has et al., been al., this 2011; estimated 1986;Golonka, Speranza ocean to 2004; Frizon et range Robertson de al., from et Lamotte late al., et PaleozoicStampfli 1991; al., to Schettino and 2011; and Borel, Gallais Turco, 2011; et 2002), Sengör al., et with al., 2011; the 1984; most recent suggestion giving a late Triassic age (Bonardi et al., 1988). Theof modern sediments, Ionian Basin which isCalabria in floored (the the by a Calabrian west accretionarytion have below prism), been the and thrust Aegean inet in region the al., response (the 2011; east to “Mediterranean Minelli in ridge”) subduction and response (e.g., Faccenna, below to 2010; Finetti, Reston subduc- 1985; et Gallais al., 2002; Speranza et al., 2012). 2013). To the south thejugate Ionian margin Basin across separated the Ionian Adria Basinthe from is east Africa likely by (Fig. the Hyblean the 1). Plateau Malta Adria’s2005; of con- Speranza escarpment Sicily et bounded (Catalano al., to et 2012). al., 2001; Chamot-Rooke and Rangin, Miocene (Cifelli et al.,the 2007; Ionian Faccenna Basin et extendedleast al., farther Jurassic 2001, in to age, 2004; the as Rosenbaum north-west. evidenced et by This o al., oceanic 2008), lithosphere was at (or Neotethys) and the Ionian Basin. Neo-Tethys Ocean (Gaina et al.,by 2013; the Schmid et Jurassic al., Piemonte 2008)1992; Ligurian, and Frisch, or in 1979; Alpine the Handy Tethys north Ocean et and (e.g., west al., Favre 2010; and Rosenbaum Stampfli, and Lister, 2005; Vissers et al., porated in the surrounding fold-thrust belts and that existed between the Vardar ocean including many Mesozoic intracontinental rift basins and platforms that are now incor- range of paleomagnetically permissible rotations valuessequences in for terms Central of Mediterranean their region kinematic con- reconstructions. 2 Geological setting Before the onset of Africa–Europelarger convergence than in today the and mid-Mesozoic, stretchedGaina Adria from was et the much al. Italian Alps (2013) to introduced Turkey the (Vlahoviæ et term al., “Greater 2005). Adria” for all continental lithosphere was followed by a late Cretaceous–Eocenerotation 20 (Márton et al., 2010). Upper Miocene stratigraphycompare of our the results to, Apulian and carbonate integrate these platform with (southern published data Italy). sets We and evaluate the ative to Africa between 130Basin. and 80 Ma, assuming a Cretaceous opening ofrotation the history Ionian of Adria. Contrastinging results Adria’s sedimentary from cover, the however, have above-mentioned beenrotation regions reported, expos- (Channell, interpreted 1977; to reflect Channell (i)(Tozzi and no et Tarling, al., 1975), 1988), (ii) (iii) 20 1994), 20 or (iv) more complex models where a 20 matics are consistent with a4 NE-ward Myr motion inferred from of kinematic Adria reconstructionSchmid, vs. of 2012). the Africa Conversely, Aegean Wortmann of region et 40 (van al. km Hinsbergen(cw) (2007) over and rotation argued the for of past a Adria Cenozoic vs. 8 reconstructions, Africa and to avoid Dercourt overlaps et of al. Adria with (1986) Eurasia postulated in a pre-Cenozoic 30 NE-ward motion relative to Africa (D’Agostino et al., 2008). These present-day kine- 5 5 25 15 20 10 25 15 20 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 944 943 140 km wide Sicily Channel rift zone (Argnani, 2009) ∼ To the north of Apulia, in the central Adriatic Sea, the fronts of the external Dinarides The northern margin of the platform is exposed on the Gargano promontory that Our study area, the Apulian carbonate platform, herafter called “Apulia” (Fig. 2), Despite the uncertainties on the opening age and direction (NE–SW according to 40 % crustal thinning and contains active rift-related volcanoes (Civile et al., 2008). first one is the Pescara–Dubrovnik line, whose presence was hypotesized by Gambini Adriatic Basin is cut byzoic Neogene extensional structures NW–SE (Fantoni striking and thrusts,et Franciosi, some 2010; al., of Grandic 2013; which et Scisciani al., invertRidge, 2002; and Meso- it Kastelic Calamita, is 2009; believed Scrocca,dissect that 2006). the several Adriatic South strike-slip Basin; of structures, unlikely, Authorsor the about disagree the Mid-Adriatic W–E with each or movement other of SW–NE aboutwhose striking, these the presence location structures is (although mainly primarily inferredmic considered from lines, dextral the or in analysis GPS origin), ofeach velocities. seismicity, As other, low-resolution were a seis- called result, three into main consideration deformation to zones, decouple alternative North to and South Adria: (i) the Apulian zone of westernrated Greece, from exposed on Apulia the alongPapanikolaou, Ionian the 2011; Islands Kefallonia Underhill, Fault which 1989; Zone became van (Kokkalas sepa- Hinsbergen et et al., al., 2013; 2006). Roydenand Apennines and antithetically meet, producing the Mid-Adriatic Ridge (Fig. 1). There, the Adriatic Basin, from which thewas present-day a Adriatic Jurassic Sea deep water roughlyUmbria-Marche continental inherited basin, rift the basin location, now that incorporatedeastward continued into in northwestward the Ionian into the Zone the Apennine whichnot is fold-thrust be now part confused belt, with of the the and previously Hellenides-Albanidesposite south- mentioned and oceanic should side Ionian of Basin, Apulia located on2002; (Fantoni the and Mattavelli op- Franciosi, et 2010; al.,units Flores 1991; of et Picha, Apulia al., 1991; have 2002; in Grandic Zappaterra, et Pliocene 1990, al., and 1994). younger Basin-transition times become incorporated in the Pre- the Mesozoic has(Channell compensated et the al., 1979; thermal Ricchetti subsidence et al., of 1998). thewas oceanic located lithosphere close toBasin the (Bosellini northestern et transition of al., Apulia 1999b; toward Graziano the et adjacent al., Adriatic 2013; Santantonio et al., 2013). The along the Apulian Escarpment (Finetti, 1985), where accumulation of sediment since Basin in a narrow segment between the Calabrian prism and the Mediterranean ridge is part ofbelt Adria to and the liesevident in west from the (D’Argenio Apulia Plio-Pleistocene et (Fig. forelandgoing 2) al., is of Adriatic 1973). interpreted the lithosphere Recent to ApennineDoglioni into NE–SW, result fold-thrust et low-magnitude the from al., flexural extension Apennine bending 1994).resents subduction of the To zone the Late-Miocene-Quaternary the down- (Argnani foredeep northeast, ofbelt et Apulia the (Argnani, al., Dinarides-Albanides-Hellenides borders 2013; 2001; the Argnanisouthwestern Adriatic et margin al., Sea, of 1996; which Bertotti Apulia rep- et appears al., to 2001; constitute de a Alteriis, passive 1995). margin The of the Ionian of kilometers of extension. Thisbasins system of connects to Lybia the (CapitanioMiocene SE to and et the younger al., Sirte NE–SW 2011)Africa, and extension likely Tripolitana and caused between was by Adria slab-pull interpretedBelguith (and forces et of to the al., the reflect Ionian 2013; subducting Capitanio African Basin), renewed et plate and late al., (Argnani, 2011; 1990; Civile et al., 2010; Goes et al., 2004). after the Mesozoic, andwhere gently the margin dips is towardsaccommodating reactivated the in Calabrian basin Pliocene trench floor, and retreat younger exceptand (Argnani times, to younger and likely the Bonazzi, NE–SW as northwest 2005). apassive extension, STEP Late margin, however, fault Miocene has forming been the between Sicily documented and within the Tunisian the∼ coast (Fig. African 1). This riftThe system dimension is of associated with the up rifted to zone and the crustal attenuation may indicate some tens Chamot-Rooke and Rangin (2005)to and Frizon Speranza de et Lamottement al. et that (2012) al. the or Ionian (2011) NW–SEMesozoic. abyssal and according Minor plane Gallais late has Miocene et notshortening inversion al. been (Gallais was (2011), strongly et associated there deformed al., with 2011). since is only Also the a general the middle few agree- Malta kilometers escarpment of has not been reactivated 5 5 25 15 20 10 25 15 20 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | erent GPS- ff 200 nT). Sam- < (Mullender et al., 1993). Ap- 2 Am erential slab retreat, and, according ff 9 − 10 × of primary non-tectonic dip (Bosellini, 2006; 946 945 ◦ C. ◦ au, 2010; Spalluto et al., 2005), the succession forms a mon- ff ) located in a magnetically shielded room (residual field 2 Am 12 − 10 For each locality, eight to ten samples were selected as pilot samples, and of each The samples were measured at the Paleomagnetic Laboratory Fort Hoofddijk of Apulia was considered an isolated carbonate platform that developed away from × performed in a magnetically shielded oven using variable temperature increments up sample two specimens weredemagnetization. retrieved for AF both demagnetization thermal and (TH)ried measurement and of out alternating the using remanence fieldzontal were (AF) an pass-through car- in-house 2G Enterprises developed1 DC robotized SQUID sample cryogenic handler magnetometerples (noise were coupled demagnetized level to by stepwise a AF20, treatment 25, hori- (alternating 30, field steps: 35, 5, 40, 8, 12, 45, 15, 50, 60, 70, 80 and 100 mT). Thermal demagnetizations were Utrecht University, the Netherlands.gated The for nature representative of samples thetype using magnetic Curie an carriers balance, in-house wasproximately with developed investi- 60 horizontal a mg translation of sensitivityheating-cooling powder of cycles obtained 5 up from to 700 each sample was subjected to stepwise 3 Paleomagnetic sampling, analysis and results 3.1 Sampling and laboratory treatment We collected 456 samples fromcarbonate nine stratigraphy localities of covering Apulia. theered Cores Cretaceous motor samples and drill were Cenozoic and collected their with orientation was a measured gasoline with pow- a magnetic compass. Salento margin show well-preserved tensthat of meters formed thick along clinoforms, and i.eThese slope rework slope deposits rocks deposits of reach theTropeano up old et to al., Apulia 2004). 25/30 margin (Bosellini et al., 1999b). Apulia (Del Ben et al., 2010). Post Cretaceous carbonate rocks cropping out along this a southern intraplatform pelagic basin, recognized in the subsurface of the submerged val is widely exposed,1975). In consists the mainly Murge of2011; area Spalluto (Fig. dolomitic and 2), and where Ca calcareousocline its age rocks dipping has (Ricchetti, gently beenSSW best towards (Ciaranfi constrained the et (Spalluto, al., SSW, 1988)undulations thus (Fig. and 2). exposing steep This younger normal monoclinaltation succession and rocks is transtensional (Festa, from deformed faults 2003). by NNE with The gentle the an to southernmost overall Salento NW–SE part Peninsula orien- facing ofthe the the Mesozoic Otranto platform exposed Channel, margin Apulia Fig. (Bosellini (i.e. 2) et the represents al., edge the 1999b). of position It of probably sharply passed to that suggested the presence of someeval continental exposed bridges regions between in Apulia and LateDuring other Jurassic co- the to Early Mesozoic, Cretaceousthe shallow time regional water (e.g. subsidence, Bosellini, carbonate 2002). up and deposition to led was 6000 m to able thick the to (Ricchetti accumulation compensate et of al., a 1998). The stratigraphic succession, succession whose Cretaceous inter- ture segments Adria in order toto accommodate Festa a et di al.finally, (2014), also its the subsurface Mid-Adriatic evidences Ridgeferent were was sectors interpreted enhanced of to by Adria be salthighs (Scisciani a of and tectonics; boundary the Calamita, (iii) external between 2009), Dinaridessent two assuming the (i.e. dif- that southward the some prosecution Palagruza structural of High the of same Grandic ridge et in al.,emerged the 2002) estern continents repre- Adriatic (D’Argenio Sea. et al., 1973) until the discovery of dinosaur footprints according to Oldow etmeasured al. velocity; (2002), (ii) the borders second twoStructure one fragments is of the of Tremiti Andre Line Adria ofseismicity and with Finetti (Favali di (1982) Doulcet et or al., (1991), the 1993,According Tremiti whose 1990) to and Doglioni presence sea-floor et is deformation al. well (1994) (Argnani and et known Scrocca al., for (2006), 1993). both this dextral its lithospheric struc- and Tozzi (1996), and that roughly corresponds to a segment of the boundary that, 5 5 20 25 15 10 25 15 20 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 140– 19.5). ∼ = ). c 2 < γ Am 12 − 15.9 ective for the sam- 10 = ff × γ C (Fig. 4a–c). The ChRMs ◦ was applied to the VGPs (Johnson ff ) and stable ChRMs were isolated for only 1 cut-o − 948 947 ◦ were rejected from further analysis. Because secular vari- ◦ C. Above this temperature intensities become too low or spu- C. This points to the presence of minor amounts of pyrite con- ◦ ◦ ; Deenen et al., 2011). The tilt corrected mean ChRM direction max A95 < A95 C. After each heating step the remanence was measured with a 2G Enterprises < ◦ C (Fig. 3). ◦ min The very low NRM intensities of these limestones also causes nearly 30 % of the Thermal demagnetization treatment demonstrated to be more e Demagnetization diagrams were plotted on orthogonal vector diagrams (Zijderveld, The distribution of theA95 ChRMs satisfies the quality criteria of representing PSV (i.e. microfossiliferous assemblage of PAgae), (mostly Luperto-Sinni and benthic Masse foraminifers (1984)136 refer and Ma; this according calcareous succession to to al- the thea Valanginian geological ( 10 time m-thick scale interval of of Gradsteinof this these et section samples al., avoiding is 2012). to very We39 low drill sampled (30–300 specimens dolomitic µAm at beds. temperature The stepsshow NRM between both intensity 220 normal and and 500 et reverse al., polarities, 2008; and McFadden and yield McElhinny, a 1990) positive (classification reversal C; test (Johnson cession in which few dm-thickthick carbonate dolomitic beds beds (Luperto-Sinni are and irregularlyup Masse, of alternated 1984). biopeloidal with wackestones/packstones Carbonate and a lithofacies microbial few aretions bindstones m- made with of rare biopeloidal intercala- and ooliticenvironments. grainstones Dolomites interpreted consists of as an formed anhedral intals, or inner which subhedral mosaic totally shelf of or peritidal dolomitic partly crys- replaced the carbonate precursor. Based on the study of the more succesful demagnetization diagrams, we usesteps eight for to the ten successive ChRM temperature directions determined by principal component3.2.1 analysis. Locality Petraro quarry (PA) The Petraro quarry (PA) isThis located section shows in the NE oldest MurgeMurge part close area of to the and the Calcare consists di town of Bari of a Formation Barletta cropping well-bedded, (Fig. out 55 2). in m-thick, the shallow-water carbonate suc- temperature steps (or AF steps)removing show this a viscous overprint, or the present-daywere characteristic overprint (Fig. remanent interpreted. 4). magnetization Most After (ChRM)approximately specimens directions 400–450 show interpretablerious results magnetizations up occur that to hamper temperatures any further of interpretation (e.g. Fig. 4g). Of the specimens show a weak but stable and measurable remanence. In general, the lowest demagnetized specimens (167) to showsamples an yielded erratic no interpretable demagnetization directions. pattern Nevertheless, and a many total of 298 demagnetized Curie balance results areates, and noisy do because no of notUpon reveal the meaningful close information very inspection about it low the can carriers intensitiesheating, be of just of seen the above that these remanence. 400 some carbon- newverted magnetic to mineral magnetite. is The created coolingthat upon curves new are higher magnetic than minerals the were700 heating created curves, that confirming were not fully removed upon heating to et al., 2008). The resultsN-dependent were reliability then envelope filtered of by (Deenenparameters the are et paleomagnetic listed al., quality in 2011). criteria Table Mean 1. of values the and statistical 3.2 Results 1967) and the characteristic remanentcipal magnetizations component (ChRMs) analysis were isolated (Kirschvink, via 1980).tion prin- Samples (MAD) with larger a maximum than angularation 15 devia- of the geomagnetictribution field gradually induces becomes scatter more in ellipsoidal1959; paleomagnetic towards Tauxe directions and equatorial whose Kent, latitudes dis- 2004), (Creerstatistics we et on calculated virtual al., site geomagnetic mean polesnen (VGPs) directions following using et procedures (Fisher, described al., 1953) in (Dee- 2011). At each locality a 45 horizontal 2G DC SQUID cryogenic magnetometer (noise level 3 pled rocks as it provided moreThe stable remaining demagnetization diagrams samples than of the each AF locality technique. were therefore thermally demagnetized. to 500 5 5 25 15 20 10 25 15 20 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ) ◦ ◦ 15, 78– erent 14.6 = ∼ 10.2 ff ± N = ( ◦ ected this ff 23.4 − 10.7 = ± I to the ChRMs dis- 16.8, A95 ∆ ff = 51.7 ± I ). Stable ChRMs were = K , 1 I ◦ − cut-o ∆ C (Fig. 4f and g) and their ◦ 32, ◦ 8.5 ± 129–121 Ma). We sampled I = ± , ∼ ◦ N ( ◦ 11.8 130.8 ± 8.0 = ± D 2.3 ∆ = ) did not allow to obtain high quality rema- ± 44.9 D 1 950 949 D = − ∆ I ± is ∆ D ff ± I , ◦ cut-o 90–83.5 Ma), overlie green shales and mark the recov- ) (Table 1 and Fig. 5). ◦ ◦ 7.1 ∼ ). ± ), but show interpretable demagnetization diagrams (Fig. 4d max 10.9 1 − = 94–90 Ma). Peritidal limestones of the Calcare di Altamura Fm, A95 333.2 ) (Table 1 and Fig. 5). Although the distribution of the ChRMs re- ∼ ◦ < = 98–94 Ma), belonging to the uppermost part of the Calcare di Bari D 9.9 ∼ ∆ A95 = 11.5, A95 ± < = D min K 29, 15.7, A95 = = N diagrams because of the lowisolated intensity at of low the temperatures NRM commonlydistribution (8–34 µAm provided not a exceeding mean 280 value of K flect a PSV-induced scatter,from the the present obtained day mean fieldCretaceous direction direction inclinations. (PDF; It is Fig. is 5) notsite, and very and statistically not likely the di consistent obtained that with results a the are recent expected not magnetic considered further. overprint a bedded pelagic chalky limestonestaining planktonic (microbioclastic foraminifers and mudstones calcispheres. to Accordingand to wackestones) Luperto-Sinni Pieri con- and and Laviano Borgomano (1989) water, distal (1989), slope these environments in deposits late69 Ma). formed Campanian to in All early relatively Maastrichtian 45 timescession. deep- ( samples Only 30 were % collected of the from analyzed the specimens lower yielded interpretable part demagnetization of the outcropping suc- tribution is (Table 1 and Fig. 5).PSV The (A95 VGP scatter for this site is consistent with3.2.4 that expected from Locality Caranna quarry (CN) The Caranna quarry (CN)ternino. is The located outcropping in section SE consists Murge of (Fig. an 2), about close 20 m-thick to succession the of town thin- of Cis- of the Calcare di Bariist Fm. beds According cropping to Laviano outmargin et in into al. a the (1998), shallow upper Ruvo intraplatformintensities Cenomanian area basin. (10–290 rud- µAm Samples record are the characterizedand progradation by e). generally of The low a mean tilt rudist-inhabited corrected direction after applying a 45 of 43 samples were collected from the lower, 15 m thick, grey-brown rudist limestones Coniacian-Santonian in age ( ery of carbonate marine sedimentation after the Turonian subaerial exposure. A total 3.2.3 Locality Cavallerizza quarry (CU) The Cavallerizza quarry (CU) is locatedtown in of Ruvo the di western Puglia. Murge The areamanian outcropping (Fig. section in 2), shows close age rudist to biogenic ( the beds,Fm late (Iannone Ceno- and Laviano, 1980).1 Rudist m beds thick, are interpreted toppedthe by as whole a a Turonian horizon ( palaeosol, of green which clays, marks a regional unconformity covering a stratigraphic thickness of 20low m intensity in of the these lowernence rocks part components (5–100 of µAm because the of outcroppingChRMs succession. is high highly The MAD scattered, failing valuestherefore all and not the considered the adopted for quality distribution further criteria of analyses. (Fig. 5). the The isolated locality is located SW of Trani.40 m-thick, The shallow-water outcropping carbonate sectionbonate succession. consists beds Similarly consist of to of a the biopeloidalshowing well-bedded, wackestones/packstones Petraro evidence and more quarry, of microbial car- than bindstones desiccationformed in features inner (mud shelf peritidal cracksthere environments. are Interbedded and few-mm with birdeyes) thick the green carbonate interpretedthe shale lithofacies study intercalations as of interpreted the as microfossiliferous palaeosols. assemblagerefer Based of this on CR, succession Luperto-Sinni and to Masse the (1984) Barremian to lower Aptian ( ( 3.2.2 Locality Casa Rossa quarry (CR) The Casa Rossa quarry (CR) is a large limestone quarry in the NE Murge area (Fig. 2), for this locality after a fixed 45 5 5 25 15 20 10 20 25 15 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | , , ◦ ◦ ◦ 17, 8.9 11.4 = 11.2 ± ± ± N ( ◦ ) (Table 1, ◦ 52.2 45.4 165.0 = 11.4 = 5.1 = I I ± = D ∆ ∆ ∆ ± ± I 46.6 I ± , ◦ , = ◦ D I ∆ 12.6 17.9, A95 10.3 ± ± I = ± , ◦ ) and only 18 samples yielded 1 K − ect of a recent overprint. Accord- 359.8 , the mean in situ ChRM direction 78–72 Ma), slightly dipping to the ; see Table 1). The distribution of ff 10.7 ff ◦ 357.7 47, = ± ∼ = = D 8.8 to the ESE is a primary, non-tectonic 8.8 ∆ D cut-o N ◦ = ( ◦ ± ∆ = ◦ 30 D ± D (Bosellini et al., 1999b). According to Par- ∼ 952 951 D ∆ 6.3 ff ± ± , a D ff 21.6, A95 44.8 = = K cut-o I ◦ ) and is probably the e ) (Table 1, Fig. 5), very close to the present-day field, and ◦ ∆ ◦ 14, ± C (Fig. 4l–n). The remanence displays both normal and re- I ◦ = 9.2 10.5 , 11.7). After a fixed 45 ◦ = N = = , erent from the present-day field direction ( ◦ 5.6 ) (Table 1 and Fig. 5). Before tilt correction, this direction is not sta- c ff ◦ 14.7) (McFadden and McElhinny, 1990). The mean normal polarity ± < γ = 16.2 9.4 c ± = 8.2 10.1, A95 12.4, A95 356.0 ) and and both normal and reversed ChRM’s that did not pass the reversal > γ 1 erent from the present-day field ( = = = = − and usually gave stable demagnetization diagrams characterized by curie ff 18.4 γ 29 K 1 − D K − = ∆ = 23, γ I ± 17, 15.2, A95 ∆ = D = = ± N 28–23 Ma) limestones belonging1992; to Parente, the 1994). This Castro unit Limestone represents Fm a (Bosellini fringing and reef complex Russo, and shows a very cation C, is Fig. 5) and the ChRMs distribution satisfies our criteria.3.2.8 Locality Castro (OC) An about 10 m-thickSalento section (Fig. was 2). The sampled outcropping close succession to consists of the Upper village Oligocene of (Chattian, Castro (OC) in E ente (1994) and Bosellini etin al. eastern (1999b), Salento this formation andorientation. is its A the current oldest total non-deformed dip of3 unit of 56 mAm samples yielded NRMtemperatures around intensities 420 ranging betweenverse 0.15 polarities and that pass the reversal test (McFadden and McElhinny, 1990) (classifi- 3.2.7 Locality Torre Specchialaguardia (TS) An about 10 m-thick successionsampled of at clinostratified the Torre breccias Specchialaguarda and localitysion bioclastic (TS) belongs in deposits E was to Salento (Fig. theLimestone 2). Upper This Fm succes- Eocene (Parente, (Priabonian,a 1994), 44–38 rocky Ma) which Cretaceous Torre formed to Specchialaguardia in Eocene paleocli a steep forereef slope onlapping ChRMs in tilt-corrected coordinates is K tistically di N ingly, this site is not considered for further analyses. interpretable demagnetization diagrams (Fig. 4). The mean direction of the isolated crofossiliferous assemblage (mostly benthic foraminifers and ostracodes).tensity The in NRM those in- samples is relatively low (0.08–6 mAm ChRM are used for further analyses. 3.2.6 Locality Massafra (MA) This locality was sampled fromMurge a (Fig. road 2). cut close We to sampledbedded the a white town 15 m-thick of to stratigraphic Massafra light-brown interval in66 Ma) the shallow-water mostly (Reina south comprising limestones of and well- with Luperto-Sinni,tidal, a 1994b). mud-supported, Maastrichtian Sampled biopeloidal limestones age mudstones mostly (72– and consist wackestones of showing peri- a benthic mi- ( likely the result ofthat a is recent statistically overprint. di TheI reverse polarity ChRMs yieldthe a reverse mean polarity value ChRMs satisfy our criteria. Accordingly, only the reversed polarity sampled in thisa study syn-sedimentary formed tectonic insoft-sediment activity, an as deformation intraplatform shown structures basin bymens, (slumps). and the 48 Out record occurrence yielded of the ofand interpretable the two i). evidence diagrams The horizons of 52 for NRM of 2000 demagnetized the µAm of speci- calculation those samples oftest is the ( characterized ChRMs by (Fig. relativelyChRM low shows, 4h after intensities a (10– fixed 45 The succession of the Porto Selvaggioconsists cove (PS) of crops out upper in Campanian westernSE, Salento. chalky It overlying mostly limestones sub-horizontal ( shallowLuperto-Sinni, marine 1994a). limestones According and to dolostones Mastrogiacomo (Reina et and al. (2012) chalky limestones 3.2.5 Locality Porto Selvaggio cove (PS) 5 5 25 15 20 10 25 15 20 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ◦ ◦ = cut- D 3.7 ◦ 20.2 ∆ ± ± ± D ESE-ward 44.2 . A total of ◦ 33.2 1 − − − 30 = = I ∼ I ∆ ∆ ± ± , indicating that PSV I I , ) (Table 1, Fig. 5). The ◦ , cw rotation of Adria by ◦ min ◦ ◦ 3.2 9.2 25 ± 13.7 = ∼ ± 180.5 222.5 = = D 19.5, A95 ) indicating a strong clockwise rotation, ◦ ∆ D = ∆ ± K ± 13.7 D 954 953 ± D is 14, ff = N ( cut-o ◦ ◦ ) (Table 1 and Fig. 5). The VGP distribution does not en- 7.9 ) (Table 1, Fig. 5). Despite the low number of specimens, ◦ ◦ ± 2.9 , site MN1 yielded a mean paleomagnetic direction of 13.0 = ff 61.1 = = C were isolated from 31 specimens (Fig. 4o and p). The mean I ◦ cut-o ∆ ◦ ± I 85.8, A95 , ◦ 19.0, A95 = ) and stable ChRM components with maximum unblocking temperatures 1 = erent sites belonging to the Lower Messinian succession of the Novaglie Fm − K ff 12.5 K ± 8, 29, = = , eight samples with a mean ChRM of The rotation of Adria and its relationship with the African plate has always been After a fixed 45 ff N N bedding dip as a(e.g., Bosellini, result 2006), of and tectonic calculated tilting, a inconsistent post-Paleogene with sedimentological studies local rotation, we consider thisrotation direction of not Adria. meaningful for the analysis of the regional a moot point (Mártonnew et constraints al., for 2003, the 2008;can Caporali rotation test et of the al., Adria 2000). robustnesscompare during Our and the the new reliability results data Cenozoic of provide ofet and, the al. the more (1988) available Oligocene importantly, from dataset. the site Interestingly, same OC we area. (Fig. These can authors 2) interpreted with the those local obtained by Tozzi of a present-day overprint. Oneyielded more an site anomalous declination (MN3), (042.5 althoughnot passing seen the in quality the criteria, restexplained considering of that the the reliable samples, collected sites.a in large The a fallen anomalous block forereef direction within breccia, the could at Messinian represent site slope MN3 deposits. Regardless may of be the cause of this 4 Discussion 4.1 Paleomagnetic constraints on the rotationReliable of paleomagnetic Adria poles werethroughout obtained Apulia (Fig. from 2). six The results localitiesdistribution from of (out three the localities of isolated were ChRMs nine) discarded did because sampled not the match the adopted quality criteria or because defined ChRM, with a dispersionwas discarded. well The beyond large our scatter quality ofo the criteria ChRMs (Fig. of 5). sub-site MN3 This yields,( sub-site after the 45 the A95 envelope passes the (Deenen et al., 2011) criteria (Table 1). VGP distribution passes our quality criteria. Only 6 specimens of MN 2 yielded a poorly- 355.1 ities, the bedding attitude1999a, in b, the 2001; sampled Vescogni, sitesa 2000). is 10 m-thick At most interval. likely each16, NRM primary sub-site 13, (Bosellini intensities 20 and et range 6 samplesrespectively al., ChRMs between were (Fig. were 9 collected successfully 4q–s). and from isolated Overall,scattered, 5000 from the µAm with sub-site direction MN1, both of MN2, normalative the and result and isolated MN3, (McFadden ChRMs reverse and is polarities.calculated McElhinny, at substantially The 1990), each reversal therefore sub-site. test separate mean yielded values a were neg- Three di were sampled within three km ofThe each outcropping other, close successions to consist the easternfied of Salento breccias in coast and (Fig. situ 2). associated coralfine-grained, bioclastic reef bioclastic and bioconstructions, base-of-slope lithoclastic clinostrati- calcarenites. prograding Similarly slope to deposits the and previous two local- ChRM direction after a fixed( 45 tirely satisfy our criteria, sinceis the underrepresented. A95 The value reverse is polaritycludes lower a of than present-day the (or A95 recent) ChRMs overprint,the and and result their the of low underrepresentation some of inclinations averaging PSV ex- PSV may within be each limestone3.2.9 sample. Locality Novaglie (MN1–3) Parente, 1994). The sampled sectioning shows to clinostratified the bioclastic(Bosellini deposits reef belong- and slope Russo, subenvironment 1992).180 Very showing µAm low no NRM evidence intensitiesbetween of characterize 220–500 these tectonic rocks deformation (15– well-preserved lateral zonation of the reef subenvironments (Bosellini and Russo, 1992; 5 5 20 25 15 10 25 15 20 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | N, ◦ 10 Ma. ) values, but ◦ ± erent numbers of ff ; Table 1). We assume that min erence at each data point. This A95 ff ccw. < ◦ ccw rotation of Adria vs. Africa. They ) and quite significant (18 ◦ ◦ 8.7 error envelope. The other approach is to ± D ∆ 956 955 erent from the expected African declinations. ff . The timing of this rotation is ill constrained, but ◦ values and a erently, since large datasets provide a better representation D ff ccw rotation. These Eocene poles are included in our analy- ◦ erent regions. We used two approaches. One approach is to cal- 30 ff cw rotation of Adria between the Cretaceous and Eocene, followed ∼ ◦ 20 ∼ E (Table 1, Fig. 7). Mean paleomagnetic directions and statistical parameters ◦ In summary, paleomagnetic data allow for a counterclockwise rotation of Adria rel- This obtained magnitude is accidentally comparable to the total rotation of Adria To calculate the magnitude of rotation of Adria with respect to Africa we combine the Figure 7a shows all declinations vs. age, from all four sectors of Adria. Approximately The updated paleomagnetic database is composed of twelve poles from Apulia (Már- To assess whether and when Adria rotated relative to Africa, we combine our results by a post-Eocene sis, but taking allsignificant available rotation data phases into between account, the early we Cretaceous see and no the solidative late to Cenozoic. ground Africa for anywhere interpreting betweenwith negligible a (1 very consistent averagecan of be 9.5 estimated from the average declination (Fig. 7) since roughly 20 calculated from the upperet Cretaceous al. (2010). of These the authors, however, Adigedistinct interpreted their phases Embayment total of and rotation cw as Istria andinterpreted the by result ccw by of Márton rotation. Márton two In et particular,suggested al. an a (2010) average to of show Eocene rocks 30 was calculate a (fourth order) polynomialBoth best-fit based approaches on show declination a values remarkablydeviation only of (Fig. coincident 7b). pattern the mean thattaceous declination display a of to systematic Adria Late ccw relative CenozoicAPWP to time of Africa Africa interval. from (Torsvik We et theing al., interpolated entire 2012) to Early the to Cre- our declination obtain theyields curve moving declination an of average, at average deviation the the and of ages determined all correspond- data the of di 9.5 significant rotations between the northern and southern sectors ofdata Adria. sets from the di culate a full-vector (six-point slidingwhich window) we moving determined average the at every data point, from counterclockwise deviations from the African APWP. The data provide no support for Vandenberg, 1983), twelve polesSouthern from Alps the (Márton Adige etof Croatia al., Embayment (Márton 2010, in et 2011), theAdige al., and Embayment 2003, foreland PSV eight 2008) of is poles (Table 1). underrepresented the this from (A95 At is the six out a Istria of result peninsula included twelve these of localities sites from within-sample in the our averaging analysis. due to low40 % sedimentation of rates the and polesThe have are remaining not poles, representing statistically the di majority of the dataset, consistently show small samples should weigh di of PSV than small data sets (see Deenen etton al., 2011). and Nardi,promontory 1994; (Channell, Scheepers, 1977; Channell 1992; and Tozzi Tarling, 1975; et Speranza and al., Kissel, 1988), 1993; five from the Gargano pare them to thefrom expected the directions Global for APWP the17.2 of European Torsvik and et African al.from plates the (2012) existing calculated database using were a re-calculatedthrough at reference parametric each location bootstrap site by sampling of averaging using 40.7 parameters VGPs the obtained (Table 1). provided This mean procedure values overcomesdata and the scatter loss statistical that of occurs information on whenity the only is original the computed mean by paleomagnetic averaging site direction averages. at In a addition, given sites local- with di preted in in situare coincident coordinates, and and indicate our no,Adria or results with a respect as minor to counterclockwise well Africa post-Oligocene (Fig. as rotation 6). of those ofwith Tozzi published et data al. from Apulia, (1988) Gargano, Istria and the Adige Embayment, and com- restoring this bedding to the horizontal. The paleomagnetic direction should be inter- 5 5 25 15 20 10 25 20 10 15 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ◦ ◦ N, ◦ 230 km of ∼ rotation of Adria would require up ◦ ◦ 400 km of E–W convergence > ccw rotation relative to Eurasia trans- ◦ 150 km NW–SE directed convergence ccw rotation of Adria relative to Africa. ∼ ◦ 17 958 957 ∼ 40 km. A similar amount of Adria–Africa relative ∼ ccw rotation of Adria relative to Africa). The other type de- ◦ erential rotation, according to Rosenbaum et al., 2004). The ff 17 ccw rotation derived from reconstructions of the Alps, this would, ∼ ◦ 40 % crustal attenuation in the 140 km wide Sicily Channel (Civile et al., 2008) ccw rotation of Adria relative to Europe around an Euler pole in the western Alps, ∼ ◦ Our discussion above identifies a paradox between the kinematic interpretations Alternatively, we may explore the maximum amount of rotation around the Euler pole Adria could rotate ccw without extension in the Ionian Basin if the Adria–Africa Eu- An Euler pole for the relative motion between Adria and Eurasia located at 45.0 20 4 E, near the city of Torino was computed by Ustaszewski et al. (2008) based on ◦ magnetic data violates both end-member scenarios. ccw rotation of Adria.the This circum-Ionian Basin, reconstruction but isbetween it consistent Adria would with require and the Europein geological contrast since record with 20 Ma, of widelytaszewski to accepted et be lower al., 2008; values accommodated Handy of in et no al., the more 2010) Western than (Fig. Alps, 8d). from some the tens geological of record of km thethe (Us- Alps scenarios and that the Ionian fulfill Basin.be the Paleomagnetic reconciled constraints data with permit from each both other. regions, Moreover, the but average these rotation scenarios suggested cannot by the paleo- would suggest a (maximum) amounttension of between NE–SW Adria latest and Miocene Africamotion to of since Plio-Quaternary the ex- Early Pliocenestruction was of inferred to the have Aegean occurredlaps from region between a by kinematic Adria van recon- and Hinsbergen the and west-Aegean Schmid fold-thrust (2012) belt. to This avoid corresponds over- to a 1.7 lenides, and the amount of westwardrequired retreat by of in this the scenario western (e.g., Alps2012) Ustaszewski is (Fig. et much 8c). smaller al., than 2008; van Hinsbergen and Schmid, constrained by Ustaszewski et al. (2008)dence that from is the permitted Sicily by the Channel available andthat structural kinematic evi- reconstructions is of comparable the Aegean with region,The the and minimum permissible rotation documented by this study. ler pole is locatedand applying in the the 17 farhowever, lead southeast to of a AdriaAdria reconstructed (Fig. and overlap the 8c). of Dinarides Assuming (i.e.in and the major Adriatic Hellenides, western Neogene rigidity, Alps. and extension Instead, predicts Adria between) continuously converged with the Dinarides and Hel- ENE–WSW extension, still much higher than what is geologically documented (Fig. 8b). westward decreasing Neogene shortening in theAdria Alps, below and the northward southern underthrusting Alps. of lates Their inferred to 20 a paleomagneticallyAssuming internal permitted rigidity of Adria,to 420 a km rotation of around ENE–WSW this extensioneasternmost pole in tip the by of Ionian stable 17 Adria Basinrequire along measured the at that Kefallonia the the Fault modern (Fig. entire south- 8a).ferred Ionian This ages scenario Basin would that is range Miocene(average from in rotation Permian age, constrained to inconsistent by Cretaceous. with our Similarly, any paleomagnetic a of analysis) 9.5 the would in- yield nate the two end-member kinematickinematic scenarios consequences for of Adria. the Accordingly, permitted wea will minimum function show and of the maximum the location rotation of of its Adria Euler as pole. 6 cw rotation (Wortmann etcan be al., accommodated 2007). within the Weccw). range of observe One rotation that documented type in two of∼ this major study scenario (i.e. types is 1–18 of putcorresponding scenarios forward to from a anrives Alpine from point an of IonianAdria view Basin and (post-20 Ma, point hence of nopaleomagnetically view permissible di (assuming rotation range near-rigidity derived between here, Africa can therefore and not discrimi- The rotation pattern ofthe Adria wider as context emergingpublished of from paleomagnetic the this data central studyCretaceous do can Mediterranean vertical not now region. axis rotations be lend Our (Dercourt interpreted support et compilation al., in to 1986; of Márton models new et al., that and 2010) infer or a either small large 4.2 Regional kinematic implications 5 5 25 15 20 10 25 15 20 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | , occurring sometime ◦ 8.7 counterclockwise) is con- ± ◦ ccw rotation). This would require as much ◦ 960 959 set sinistral strike-slip fault? ff ccw rotation), and the reconstruction of van Hinsber- ◦ Fieldwork was funded through the Netherlands research school of Inte- counterclockwise rotation of Adria relative to Africa (based on kine- ◦ 18 ∼ 10 Ma. Our revised paleomagnetic database for Adria discards significant ro- ± The discussion above indicates that, although scenarios based on kinematic inter- Since a key assumption in the above analysis is the rigidity of Adria, we explore a fi- ern edge of the Tyrrhenian subducted slab, Geol. Soc. Spec.along Publ., the 311, front 193–212, of 2009. the Albanide thrust-and-fold belt, IJG, 132, 175–185, 2013. arc basin, J. Geodyn., 12, 311–331, 1990. Petroleum Geology, Atlas of Oil andand Gas Fields, Beaumont, Stratigraphic E. Traps II, A., edited AAPG, by: Tulsa, Foster, 29–54, N. H. 1991. disagreement with both models, wesive. establish We that cannot these solve scenarios thisquestions are enigma, that mutually but may exclu- lead call to forthe a kinematic solution western studies of Alps focused the on significantly conundrum:nian three (i) underestimated? Basin key was (ii) significantly Neogene Was shortening underestimated? Neogene in (iii)a extension Was South in a Adria North block the along Adria Io- a block large-o decoupled from several studies. The permissiblesistent rotation with magnitude two (1–18 end-member modelsa for Neogene the Central Mediterranean regionmatic requiring reconstruction (i) of the Alps),reconstruction or of (ii) the negligible Ionian rotation Basin. of Although Adria paleomagnetic based data on from kinematic Adria are not in tations of Adria vs. Africa between the Early Cretaceous and the Eocene, as invoked by a counterclockwise rotation of Adriaafter relative 20 to Africa at 9.5 Mediterranean ridge? 5 Conclusions We provide six new paleomagnetic polesof from the the Lower Cretaceous Murge to Upper anddata, Miocene combined Salento with areas recalculated ofIstria published peninsula the poles of Apulian from Croatia, Platform, the and southern the Gargano Adige Italy. promontory, Embayment These the of new the southern Alps, constrain may underestimate the true amountening of in convergence: the is western the Alpstiming significantly amount and underestimated? of (ii) Neogene amount Is short- of itblock? possible potential (iii) to strike-slip Is quantify it zones the Apulian possible separating that escarpment, a there North perhaps is and hidden a South below large Adria amount the of advancing Neogene Calabrian extension prism along and the the identified structures appear likelyments (Fig. candidates 8e). to accommodate such major displace- pretations from both the Alpsrotations and that the are Ionian within basintually the infer Neogene exclusive. range Adria–Africa Paleomagnetic documented relative data in– this alone cannot study, – these solve with scenarios this theof are “Adriatic error mu- three enigma”, envelope areas but calculated centered calls here around for three a questions: reassessment (i) of since the shortening kinematics reconstructions nal scenario whereby weRidge, decouple or north and along south theet Adria, Tremiti al. e.g. fault (2008) along (Fig. for the North 2).gen Mid-Adriatic and Adria Applying Schmid (17 the (2012) for reconstruction Southas Adria of 160 (1.7 km Ustaszewski of left-lateral strike-slip between North and South Adria, and none of the Argnani, A.: The influence of Mesozoic Palaeogeography on the variations in structural style Argnani, A.: Evolution of the southern Tyrrhenian slab tear and active tectonics along the west- Argnani, A.: The strait of sicily rift zone: foreland deformation related to the evolution of a back- Acknowledgements. grated Solid Earth Sciences306810 (ISES). 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R.: Late Cenozoic deformation of the Hellenide foreland, western Greece, Geol. 5 30 25 20 15 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | E ◦ (ref) I corre- ∆ N/17.2 I ◦ ∆ max (ref) I declination; = (ref) D D ∆ DI ∆ ; and A95 ff (ref) 1.00.6 3.9 4.8 55.9 53.7 3.0 4.1 5.7 8.8 59.7 5.9 0.2 3.2 45.1 3.6 333.5311.4 7.1 8.5 44.2351.4 22.1356.2 8.1 5.5333.5 14.8 3.8315.4 57.4 3.3352.4 47.8 7.1326.8 4.0 35.3 2.9334.8 3.9 44.4 2.6335.8 4.6 45.2 5.9316.2 8.1 44.1 4.3 3.2 34.2 3.5338.9 2.9 33.5336.0 8.5 39.2 7.0351.1 6.3 4.6340.6 4.5 44.2 3.4339.9 38.3 3.0339.6 8.0 27.8 2.2335.3 6.1 22.0 2.8332.5 5.5 35.0 3.5333.6 5.2 35.9 2.1310.3 3.2 27.8 3.2307.0 3.9 29.1 5.1339.0 5.7 27.5 3.4344.5 3.3 33.7 8.1334.9 5.2 32.1 8.9342.3 7.4 47.4 6.6347.4 5.0 42.3 4.0332.6 8.4 50.1 9.7319.1 10.7 42.4 3.4317.9 6.4 56.6 6.4 4.7 35.3 4.3 7.4 36.6 4.8 41.0 8.8 5.3 355.3 11.8355.6 57.6 5.7 8.6 344.6 45.7 8.9 6.3 19.7 16.1 reference location 40.7 D D min number of interpreted cut-o = error in inclination sensu N45 i ◦ i N = 1613 14 8 355.1 12.5 42.5 61.1 13.7 7.8 33.2 20.2 31 29 0.5 3.2 44.2 3.7 5518 4715 17 356.0 15 5.7 8.8 44.8 2.3 10.6 6.4 46.6 11.7 51.7 11.4 10.7 14 14 345.0 8.9 18.4 16.3 4339 32 29 333.2 310.8 7.2 8.5 44.9 23.4 8.0 14.6 λp φp /N ). A95 / / / / / / / / / d N Ix k ) ∆ k Longitude of the site; Ages are Age 95, ∆ = α 95) ( 3.9 72.6 82.9 267.8 6.2 39.0 67.1 253.6 2.7 94.33.2 83.5 21.9 192.9 6.2 77.82.4 21.9 213.1 50.5 32.65.5 279.9 74.7 20.8 223.9 3.2 59.2 42.3 249.3 48.8 274.0 3.82.7 90.9 239.5 63.02.8 56.1 216.4 3.2 233.0 67.8 59.3 62.9 243.2 56.34.3 244.0 3.3 28.8 116.3 42.2 39.1 274.7 276.3 5.73.1 13.65.6 33.1 79.63.9 24.1 58.5 271.3 85.3 49.9 253.2 50.8 269.3 274.3 2.7 71.8 85.7 186.8 3.3 65.6 59.02.1 252.0 36.24.4 58.8 10.9 269.1 4.6 59.4 247.2 27.64.0 85.7 26.9 106.9 62.12.1 251.1 164.2 62.52.0 241.9 2.8 121.7 55.3 57.4 248.7 55.36.3 246.1 7.1 15.64.4 15.2 69.03.1 25.9 69.2 258.4 65.2 240.4 67.4 68.1 269.2 245.2 α ( K 8.0 168.0 210.2 Inclination; max = 7.1 8.0 76.2 9.8 7.6 113.7 13.8 116.8 13.8 124.5 16.3 A95 I min 974 973 3.1 9.8 11.5 9.1 9.6 38.3 266.8 2.5 E. ◦ ) and directions ( 3.1 2.73.1 8.0 3.1 54.1 2.1 9.6 1.84.1 72.7 1.8 4.0 36.2 4.1 12.6 2.1 3.1 3.1 2.67.1 7.38.1 2.9 47.5 3.1 8.7 9.8 12.8 11.8 6.42.4 3.3 1.84.4 10.5 2.8 4.1 20.9 26.7 8.2 20.8 3.4 2.9 8.9 52.3 3.3 3.9 4.0 3.1 9.6 44.3 4.8 2.8 8.2 23.4 6.03.9 3.1 3.9 9.8 13.8 20.7 85.6 4.3 3.6 12.4 57.5 6.3 4.1 14.9 37.5 8.3 3.3 2.0 4.7 20.8 4.3 2.5 7.1 23.4 2.9 4.3 3.6 3.0 9.1 50.0 2.0 2.6 3.2 2.6 7.3 43.9 3.2 2.3 6.0 32.2 2.6 2.7 3.2 3.9 6.7 2.8 8.4 13.3 5.7 2.7 7.8 16.1 7.7 K Latitude of the site; Lon N, 17.2 = ◦ number of demagnetized specimens; = d N total number of specimens that fall within the 45 = Table showing all the data of our, and published paleomagnetic results for Adria. MN3 (Novaglie Lower Messinian) This study Apulia 39.9 18.4 6.6 0.6 20 MA (Massafra Quarry)CN (Caranna Quarry) This study This study Apulia Apulia 40.6 17.1 40.8 69.1 17.4 72.1 3.1 4.0 40 45 Continued. 78 Middle Eocene9 Turonian–Senonian Turonian Van den Berg et al. Speranza (1993) and Kissel (1993) Gargano Gargano 41.9 41.8 16.0 16.1 Channel and Tarling (1975) 83.0 44.5 Gargano 10.9 3.3 41.7 15.7 90.1 3.8 123 114 326.1 352.0 13.2 3.3 46.0 46.7 212.9 39 225.7 334.0 4.2 36.3 76.7 12 Upper Plio–Pleistocene3 Pliocene–Quaternary (in4 situ) Miocene (in5 situ) Eocene/Oligocene (in6 situ) Tozzi Conamanian–Turonian et al. (1988) Scheepers Lower–Middle (1992) Cenomanian Tozzi et al. (1988) Márton and Márton Nardi and (1994) Apulia Nardi (1994) Tozzi Apulia et al. (1988) 40.0 Apulia 40.5 Apulia 18.4 Apulia 16.5 41.0 41.0 3.2 2.7 16.3 40.0 16.3 Apulia 18.4 98.9 2.2 95.1 0.9 26.8 40.0 1.6 2.1 18.4 1.3 14.2 30 8.8 40 26 0.9 30 0.9 93 314.9 333.1 2.2 356.5 3.9 2.3 2.4 64.6 1.3 55.7 20 45.3 36.2 59.7 46.9 351.6 51.8 3.0 59.7 185.7 8.9 56.6 37.3 error on declination sensu Butler (1992); CN (Caranna Quarry) This study 9.9 4.1 14.9 15.7 8.3 22.0 81.4 184.4 MN3 (Novaglie Lower Messinian) This studyMA (Massafra Quarry) This study 13.0 5.2 22.1 19.0 9.4 14.9 14.7 3.9 47.5 126.5 13.8 15.2 10.2 13.1 75.3 164.9 1011 Turonian–Coniacian Neocomian–Aptian1213 Priabonian14 Lutetian15 Ypresian16 Paleocene Channel et17 al. (1977) Maastrichtian18 Van den Campanian Berg et al.19 (1993) Upper Coniacian20 Coniacian Gargano Gargano21 Turonian–Coniacian 41.9 41.922 Cenomanian Márton 16.0 16.0 et23 al. (2011) Valanginian–Hauterivian 124.0 91.9 Berriasian24 Márton et 15.4 al. Márton (2011)25 et Márton Márton 2.0 al. Lutetian et et (2011) al. al. (2010) (2011)26 Márton et Cuisian al. Márton Adige Márton (2010) et27 Márton et al. et al. (2010) Turonian–Coniacian al. (2010) (2010)28 Turonian Adige 45.629 47 Cenomanian Márton Adige et Adige Adige al. 11.430 114 (2010) Márton Albian 315.3 et Adige al. 45.331 (2010) 35.9 335.1 Adige Valanginian–Aptian Adige 21.9 45.4 Adige 11.7 45.5 45.6 Tithonian 2.2 41.2 11.5 2.0 45.5 11.3 11.3 Márton 44.5 Márton et 45.5 et 35.7 al. 45.5 66.3 al. 51.9 45.5 (2008) 11.3 (2010) Adige 69.1 61.0 11.3 227.0 11.3 11.3 3.3 Adige 87.2 4.1 Márton 90.1 135.1 77.9 3.1 5.0 et al. 45.5 (2003) Márton 0.9 et 45.5 11.3 al. 4.3 3.8 Márton (2003) 5.8 et Istria Márton al. 37 Adige et (2008) 11.3 Márton al. 88.1 et (2008) al. (2008) 97.2 6.2 15 1.8 45.5 45.1 Istria 49 13 17 3.3 11.3 336.2 13.7 Márton 9.7 Istria et al. 332.9 40 (2008) Istria 142.2 Márton 337.1 348.1 39 et 44 7.4 90.1 Istria 64.1 29 al. 45.3 (2008) Istria 4.9 336.5 3.0 3.5 2.8 51.1 305.8 328.9 13.9 45.3 336.8 5.3 3.8 46.3 2.9 45.1 32.1 36.6 13.9 5.3 2.2 44.5 45.1 6.9 2.3 34 45.1 13.7 44.2 5.2 Istria 13.7 46.0 42.7 4.5 46 4.9 38.7 43.4 13.7 331.8 126.2 3.3 Istria 3.3 97.2 330.1 6.3 91.9 2.9 3.7 13.2 8.0 2.7 45.1 17 3.3 3.3 37.5 42 45.1 2.1 13.7 37.3 302.4 13.7 106.8 5.0 332.7 3.5 148.6 4.5 35 7.0 6.3 41.3 29 3.5 29 55.4 337.1 4.3 316.3 49 342.8 8.5 33 5.6 6.7 346.3 9.4 53.1 340.4 10.4 43.5 48.5 64 4.1 7.4 61.0 17 7.8 9.4 48.6 330.3 6.6 314.9 3.5 4.1 4.4 42.5 47.3 4.2 4.6 PA PA (Petraro Quarry) This study Apulia 41.3 16.3 138.0 2.0 48 TS TS (Torre Specchialaguardia) This study Apulia 40.0 18.5 35.9 2.0 56 PS PS (Porto Selvaggio Cove) This study Apulia 40.2 18.0 74.0 2.0 53 CU CU (Cavallarizza Quarry) This study Apulia 41.0 16.4 95.6 1.7 50 OC OC (Oligocene Castro) This study Apulia 40.0 18.4 25.6 2.6 45 MN MN1 (Novaglie Lower Messinian) This study Apulia 39.9 18.4 6.6 0.6 20 code site name source area lat lon Age = 23 Pliocene–Quaternary (in situ) Miocene (in situ) Tozzi et al. (1988) Tozzi et al. (1988) 1 Upper Plio–Pleistocene45 Eocene/Oligocene (in6 situ) Conamanian–Turonian Scheepers7 Lower–Middle (1992) Cenomanian8 Middle Eocene9 Tozzi et al. (1988) Turonian–Senonian Márton Turonian and Márton Nardi and (1994) Nardi (1994) Van den Berg et al. Speranza (1993) and Kissel (1993) Channel and Tarling (1975) 13 Lutetian Márton et al. (2011) 24 Lutetian Márton et al. (2003) 1011 Turonian–Coniacian Neocomian–Aptian12 Priabonian1415 Ypresian16 Paleocene Channel et17 al. (1977) Maastrichtian18 Van den Campanian Berg et al.19 (1993) Upper Coniacian20 Coniacian21 Turonian–Coniacian22 Cenomanian Márton et23 al. (2011) Valanginian–Hauterivian Berriasian Márton25 et Márton Márton al. et et (2011) al. al. (2010) (2011) 26 Márton et Cuisian al. Márton Márton (2010) et27 Márton et al. et al. (2010) Turonian–Coniacian al. (2010) (2010) 28 Turonian29 Cenomanian Márton et al.30 (2010) Márton Albian et al.31 (2010) Valanginian–Aptian Tithonian Márton Márton et et al. al. (2008) (2010) Márton et al. Márton (2003) et Márton al. et (2008) Márton al. et (2008) al. (2008) Márton et al. (2008) Márton et al. (2008) PA PA (Petraro Quarry) This study TS TS (Torre Specchialaguardia) This study 5.1 2.6 7.3 17.9 5.1 17.7 76.0 213.4 PS PS (Porto Selvaggio Cove) This study 8.8 4.2 15.6 11.0 11.9 12.1 56.5 225.5 CU CU (Cavallarizza Quarry) This study 6.4 3.0 9.2 16.8 7.2 13.4 63.6 261.5 OC OC (Oligocene Castro) This study 2.9 3.1 9.8 85.8 3.1 75.6 75.9 196.6 MN MN1 (Novaglie Lower Messinian) This study 9.2 4.2 15.6 19.5 6.9 34.3 85.7 255.0 code site name source A95 A95 Dx Table 1b. Table 1a. Areas are indicated in Fig. 1. Lat assigned based on theGradstein biostratigraphy et of al. the (2012); sites, and translated into numerical ages using specimens; N45 ∆ Butler (1992). Statistical parameters aretics given by on a virtual cone geomagnetic confidence using poles Fisher (A95, (1953) statis- spond to the confidenceerrors envelope at a of reference Deenen location et 40.7 al. (2011). Right-hand panel: directions and Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper |

Ionian Abyssal Otranto Channel = S T Adige Embayment; OC; 4 o MN; 2,3 Karaburun Peninsula;

= t 30°E 50°N 40°N =

es alen

t S y (published) a t y (this study, unsuccessful) Platform bon Moesian t r Aegean Sea Aegean

Carpathians y (this study, successful) t PS oic ca z Ionian Sea o Tremiti Fault. ampling locali

en II

S Albanides-Hellenides KFZ Mediterranean Ridge C - = 20°E ampling locali c ene clastics

AEs S oi c KP ampling locali z o Hyblean Plateau; IAP S t o Pannonian Basin Pannonian Tripolitania-Sirte Basin

CN IAP

= es Prism leis Adria M

Apulia P - Calabrian Ionian Basin Figure 2 Figure A ge o

Dinarides r li M

P

976 975 ME Bari Ga TF Mu Calabria Kefallonia Fault Zone; KP HP Is = MAR Figure 1 Figure Adriatic Sea Sicily

Sicily Channel 1 Eurasia Apennines rift zone AE e 2 Gargano; HP CU r gano CR

Po Plain r = pulia Africa a Malta Escarpment; TF Tyrrhenian Sea Tyrrhenian A igu G = A Istria; KFZ F P 5,6 Alps = 7 t 10°E on Fr 50 km 9 8, 10, 11 Maghrebides penninic A Ionian Islands; Is Regional tectonic map of the Mediterranean region. AE = A simplified geological map of the exposed Apulian Foreland (Apulia, southern Italy) Mid-Adriatic Ridge; ME Apulian Escarpment; Ga = = indicating our new, and previously publishedet paleomagnetic al., sampling 1997). sites Numbers (modified and from codes Pieri correspond to sites listed in Table 1. Fig. 2. AEs Plain; II MAR Fig. 1. Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | TS46 700 600 500 400 300 Temperature (°C) 200 100

0 Total Magnetization (Am2/kg) Magnetization Total 0.00 0.01 700 PS 5.1 600 500 400 978 977 300 Temperature (°C) Figure 3 Figure 200 100

0 300 (Am2/kg) Magnetization Total 100 700 PA 6a 600 500 400 300 Temperature (°C) 200 100

0 Total Magnetization (Am2/kg) Magnetization Total 0.01 0.00 Orthogonal vector diagrams (Zijderveld, 1967), showing representative demagnetiza- Thermomagnetic curves measured on a Curie balance (Mullender et al., 1993) for rep- tion diagrams for allcoordinates. Closed sampled (open) sites. circles indicate Except the for projection OC, on the TS horizontal and (vertical) MN plane. all sites are in tilt corrected Fig. 4. Fig. 3. resentative samples. Arrows indicate heating (red) and cooling (blue). Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | In Situ (bedding tilt is primary) Tozzi et al., 1988 et al., Tozzi Tilt corrected Tilt 980 979 ) indicates the present-day geocentric axial dipole Figure 6 Figure ∗ Locality OC In Situ 95). Red (small) dots indicate the individual directions rejected α (bedding tilt is primary) . Green asterisk ( ff New data cut-o ◦ Tilt corrected Tilt Equal area projections of both in situ and tilt corrected ChRMs from our site OC (left) Equal area projections of the VGP (left) and ChRM directions (right) of all sites in both and from therotation same that locality would of resulthave Tozzi a from et primary a dip al. tilt (Fig.Fig. correction (1988) 7) 5. of and (right), should the illustrating be bedding considered the at in apparent in this situ clockwise locality. coordinates. The Symbols strata are here as in Fig. 6. after applying a 45 Fig. 5. in situ and tiltthe corrected upper coordinates. Open (lower) hemisphere. (closed)relative symbols Large cone corresponds dots of to in confidence the the projection ( ChRM on plots indicate the mean direction and (GAD) field direction at the sampledwith location. a Sites primary TS, OC, bedding and attitudes, MN and were sampled should in be sediments considered in in situ coordinates. Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ) (red D ∆ calculated at each D 30 20 10 0 -10 -20 -30 -40 -50 -60 30.0 20.0 10.0 0.0 -10.0 -20.0 -30.0 -40.0 -50.0 -60.0 ∆ 0 0 1 B A 2 MN1 3 data point data 4rth Polynomial trendline order moving 6-point average 20 20 This study (Apulia) This Apulia Gargano Promontory Embayment Adige Istria OC 4 TS 12 40 40 13 8 24

25 African APWP African

14 African APWP African 15 60 60 16 PS 17 80 982 981 5 80 Eurasian APWP Eurasian 19 Eurasian APWP Eurasian 18 9 Figure 7 Figure 26 20 27 6 10 28 7 CU 21 100 E). Numbers and site abbreviations correspond to data 100 ◦ 29 120 11 120 N, 17.2 30 ◦ 22 140 PA 23 140 31 Same data, with a polynomial 4th order trend line (purple dashed line) Reference location 40.7°N, 17.2°E location Reference Reference location 40.7°N, 17.2°E location Reference (B) Age (Ma, following the timescale of Gradstein et al., 2012) vs. declination plot for our Caption on next page. Fig. 7. (A) new, and published data fromare Adria. from The Torsvik error et envelope for al. the (2012). African Vertical and Eurasian error APWPs bars correspond to the Fig. 8. line). and the declination component of a full-vector 6-point moving average with error bars ( site (Table 1); horizontalto error a bars reference location correspondentries (40.7 to in age Table 1. uncertainty. All data are recalculated Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ◦ ccw . Re- ◦ a 1.7 decou- (D) (D) a 9.5 (E) (B) ccw rotation of Adria vs. Africa, ◦ ccw rotation of Adria vs. Africa corresponding to ◦ 983 , and South Adria following a scenario as in a 9.5 (A) (C) the rotation pole of Adria vs. Eurasia of Ustaszewski et al. (2008), (A) ccw rotation of Adria vs. Europe, corresponding to 18 ◦ Reconstructions at 20 Ma for rotation scenarios of Adria vs. Africa that are permitted by pling north and south AdriaNorth along Adria the Mid-Adriatic following a Ridge of scenario Scisciani as and in Calamita (2009), with the paleomagnetically constrained mean rotationof in Adria this and paper, around allowing a minimum pole relative located latitudinal in motion the between SE Africa and Adria; constrained from shortening reconstructionsrotation in of the Adria vs. Alps Africastrained by mean around the rotation the in same same this authors; pole paper; corresponding to the paleomagnetically con- ccw rotation of Adriato the vs. maximum Africa amount around of the Neogene pole extension documented of in Ustaszewski the et Sicily al. Channel; constructions (2008), of: (i) corresponding the Adriaticet front al. of (2008), the Alps, (ii) Carpathians thebergen and western Dinarides et Mediterranean follow region al. Ustaszewski follow (2014), Faccenna(2012). et and al. Reconstruction (iii) (2004), is the and given Aegean–Albanian van inusing Hins- region a rotation follow Europe-fixed van poles frame, Hinsbergen with ofCentral and the Gaina Atlantic Schmid position Ocean, et of respectively. al. Africa (2002) determined and Müller et al. (1999) for the North Atlantic and Fig. 8. paleomagnetic data, using and a 20