P35_ copertina_R_OK C August 20-28,2004 Florence - Field Trip Guide Book - P35 Post-Congress M. Schiattarella S. ,F. Loiacono, Associate Leaders: P. Pieri,L.Sabato,M.Tropeano Leaders: SYSTEM INSOUTHERNITALY FORELAND-FOREDEEP-CHAIN TECTONIC EVOLUTIONOFTHE STRATIGRAPHIC AND PLIO-PLEISTOCENE 32 Volume N°4-fromP14toP36 GEOLOGICAL CONGRESS nd INTERNATIONAL P35 21-06-2004, 9:43:19 The scientific content of this guide is under the total responsibility of the Authors

Published by: APAT – Italian Agency for the Environmental Protection and Technical Services - Via Vitaliano Brancati, 48 - 00144 Roma - Italy

Series Editors: Luca Guerrieri, Irene Rischia and Leonello Serva (APAT, Roma)

English Desk-copy Editors: Paul Mazza (Università di Firenze), Jessica Ann Thonn (Università di Firenze), Nathalie Marléne Adams (Università di Firenze), Miriam Friedman (Università di Firenze), Kate Eadie (Freelance indipendent professional)

Field Trip Committee: Leonello Serva (APAT, Roma), Alessandro Michetti (Università dell’Insubria, Como), Giulio Pavia (Università di Torino), Raffaele Pignone (Servizio Geologico Regione Emilia-Romagna, Bologna) and Riccardo Polino (CNR, Torino)

Acknowledgments: The 32nd IGC Organizing Committee is grateful to Roberto Pompili and Elisa Brustia (APAT, Roma) for their collaboration in editing.

Graphic project: Full snc - Firenze

Layout and press: Lito Terrazzi srl - Firenze

P35_ copertina_R_OK D 9-06-2004, 10:15:47 Volume n° 4 - from P14 to P36

32nd INTERNATIONAL GEOLOGICAL CONGRESS

PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND- FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY AUTHORS: P. Pieri¹, L. Sabato¹, M. Tropeano², A. Albianelli3, A. Bertini3, V. Festa1, S. Gallicchio¹, F. Loiacono¹, C. Lombardi3, F. Masini3, M. Moretti1, G. Napoleone1, L. Pomar4, M. Schiattarella², L. Spalluto1 1Università di Bari - Italy 2Università della , - Italy 3Università di Firenze - Italy 4Universitat de les Illes Balears

Florence - Italy August 20-28, 2004

Post-Congress P35

P35_R_OK A 9-06-2004, 10:41:52 Front Cover: Nonna Carmela. (southern Apennines, Basilicata).

P35_R_OK B 9-06-2004, 10:41:54 PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35

Leaders: P. Pieri, L. Sabato, M. Tropeano Associate Leaders: S. Gallicchio, F. Loiacono, M. Schiattarella

1. Introduction Oligo-Miocene deposits are today tectonized and P. Pieri, L. Sabato, M. Tropeano added in the accretionary wedge. Younger (Plio-Pleis- The aim of this fi eld trip is to illustrate the three main tocene) foredeep deposits are less deformed and, in depositional areas of the Plio-Pleistocene Apennines southern Italy, they are well exposed as a consequence foredeep system (foreland, foredeep s.s., and satellite of a severe Quaternary uplift which affected and af- basins) in southern Italy and to discuss its evolution fects the whole south-Apennines orogenic system showing stratigraphic and sedimentologic features of (chain, foredeep and foreland settings). This allows tectonized to practically undeformed Plio-Pleistocene us to observe, during our fi eld trip, stratigraphic, sedi- successions. mentologic, and tectonic features of Plio-Pleistocene The Apennines foredeep (Italy) is the Upper Oli- successions of the whole south-Apennines foredeep gocene to present-day developed on system. the fl exured Adria Plate. Up to Pliocene time, the The fi eld trip will develop between (evening Apennines foredeep was a deep basin characterized of day 1) and Basilicata (days 2 to 5) regions (back cover and Figs. 7, 9, 28) and crosses a complete geological section of the Plio-Pleistocene foredeep system (Figure 2), beginning from the outer foreland ramp (Apulian Foreland - late evening of day 1 and day 2) as far as the younger thrusts of the Apennines (inner foredeep sector - day 3), through the foredeep s.s. (Bradanic Trough) (day 4) and the coeval satellite Sant’Arcangelo Basin (day 5) (Figure 3). As regards fi eld map references, we will refer to some geological maps of the Italian Geological Survey (Servizio Geologico d’Italia, sheets n°: 176 “Barletta”; 188 “Gravina”; 189 “”; 200 “Tricarico”; 201 “”; 211 “Sant’Arcangelo”), and to other geological maps (“Carta Tettonica d’Italia” by Funiciello et al., 1975; “Carta geologica dell’Appennino meridionale” by Bonardi et al., 1988a; “Carta geologica delle Murge e del Salento” by Ciaranfi et al., 1988). As regards road map references, we will refer to the “Grande carta stradale d’Italia 1: 200.000” made by the TCI (Touring Club Italiano – sheets: “Campania e Basilicata”, and “Puglia”).

Figure 1 - Schematic structural map of Italy showing the 2. Regional geological setting present-day location of the Apennines foredeep. P. Pieri, L. Sabato, M. Tropeano The growth of the Apennines chain (Italy) started

mainly by turbidite sedimentation (Pescatore, 1978; during Late Oligocene times (Boccaletti et al., 1990), P14 to P36 olume n° 4 - from Ricci Lucchi, 1986; Casnedi, 1988; 1991; Ori et al., when the Adria Plate, characterized by both oceanic 1991), while the Quaternary Apennines foredeep is a (Ionian sector) and continental (Apulia sector) litho- V basin characterized by: i) a subsiding overfi lled sector sphere (Finetti, 1982; Catalano et al., 2001), began (Po Plain); ii) a subsiding nearly fi lled sector (north- to subduct back to the Alpine-Betic thrust belt; the central Adriatic Sea); iii) an uplifted, exposed, and Alpine-Betic back-thrust belt and the hinterland of cannibalized sector (Bradanic Trough); iv) a deep- the same Alpine-Betic orogen (the undeformed Adria) marine basin only in the southernmost part of the were progressively involved in this westward subduc- present-day foredeep (the Taranto Gulf in the Ionian tion (Doglioni et al., 1998, and references therein). Sea) (Tropeano et al., 2002a, and references therein) The Apennines foredeep (Figure 1) is the foreland (Figure 1). basin related to the Apennines thrust belt; its subsid-

3 - P35

P35_R_OK 3 9-06-2004, 10:42:24 P35_R_OK 4

Volume n° 4 - from P14 to P36 P35 - P35 Leaders: P. Pieri,L.Sabato,M.Tropeano loading (Royden tive eastward mantelfl Plate (slabpullandsinking,and/oroppositiontorela- and isinducedbytheeastward roll-backofthe Adria ence rateishigherthan1km/Myr(Doglioni,1994) system (modifi structural elementsofthesouth-Apenninesorogenic F erences therein central andsouthern Apennines. Inthecentral Apen- ferent stylesoftectonicdeformationcharacterizethe According toPatacca andScandone(2001),two dif- caletti previous piggybackarea)(Ricci Lucchi,1986;Boc- ously characterizedbycompressionalregimes (the to theactive piggybackareaover chainsectorsprevi- tensional and/ortranstensionaltectonicregimes back of theorogenicsysteminducessuperposition 4). Moreover, theprogressive eastward migration Ori foreland (RicciLucchi,1986;Boccaletti rates graduallyinvolved moreeasternsectorsofthe e basin (apiggybackareaorawedge-topbasin)andan the foredeep,splittingitintoaninternalshallower of theorogenicsystem. Thrusting propagatedwithin foredeep recordsthisprogressive eastward migration structural andsedimentaryhistoryofthe Apennines the Apennines (Patacca andScandone,1989). The to lessthan1cm/yrmoving fromsouthtonorthalong of crustalshorteningdecreasefromabout5-6cm/yr nines and,accordingly, boththeamount andvelocity linearly decreasesmoving towards thenorthern Apen- Boccaletti ers moved towards theE-NE(RicciLucchi,1986; (Patacca order of700kminsouthernItaly( arc migration,whichhasbeencalculatedtobeinthe xternal deeperone(foredeep igure 2-Geologicalcross-sectionshowing themain et al. et al. et al. , 1991;DeCellesandGiles,1996)(Figure et al. , 1990).

ed fromSellaetal.,1988). , 1990;Gueguen ). The Apennines foredeep depocent- , 1990)following thefast Apennines et al.

, 1987;Doglioni,1991, o w) ratherthanbythrust-sheet et al. s.s. ); highsubsidence i.e. , 1997);thisvalue

Calabrian arc) et al. and ref- , 1990;

basins (ordepocenters),but recently, accordingto successions werestudiedasdepositedindifferent cally disconnected. Traditionally thesedisconnected nines foredeepsystemaretodayexposed andphysi- different sectorsofthePlio-Pleistocene south-Apen- nines chain,depositionalsuccessionsbelongingto propagation oftheduplex systeminthesouth-Apen- In consequenceofbothuplifttheforelandand subside (Doglioni w and causedtheslabtobuckle; northward andsouth- subduction hinge,whichlowered subductionrates arrival ofathicker lithosphereinthesouth-Adriatic Pleistocene times(Ciaranfi F et al. cover isunderthrustbythe“allochthon” (Ciaranfi up totheBasilicataregion), forelandsedimentary southward the Abruzzi-Molise (from ern Apennines (Patacca andScandone,2001, Merlini, 1986)andalarge-scale duplex systemform did thrustspropagateintheforeland(Mostardiniand (the Apulian Foreland). Onlyafteritsunderthrusting thon”) whichoverthrust thesouth-Apennines foreland gation mostlyproceededbylongsheets(the“alloch- al. which progressively involved theforeland(Bally imbricate fans development inpiggybacksequences, Tr nines, tothenorthofMaiellaMountainand wedge (Argnani predominantly addedtothefrontofaccretionary is directlyinvolved inthethrustpropagationandis the central Apennines, theforelandsedimentarycover characterize thecentralandsouthern Apennines. In Therefore, two different stylesofforedeepmigration (Figs. 2,4). to Doglioni oreland hasbeenupliftingsinceEarly-Middle ard of Apulia the Apennines forelandcontinuesto emiti line,thrustspropagationmostlyproceededby , 1986).Inthesouthern Apennines, thrustspropa- , 1979)(Figs2,4,5b).Moreover, the Apulian et al. et al.

et al. (1994) thisupliftisrelatedtothe , 1991);incontrast,thesouth- , 1996).

et al. and references therein , 1983). According 9-06-2004, 10:42:28 et )

PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35

nine Formation (Iannone and Pieri, 1979; Tropeano and Sabato, 2000). The in-fi ll of the Bradanic Trough began during late Early to Middle Pliocene times on a wide subsid- ing area of the Apulian platform (Ciaranfi et al., 1979); foredeep deposits lie on a carbonate bedrock mainly exposed since Late Cretaceous time (Crescenti, 1975). The buried Pliocene to Lower Pleistocene succession is mainly characterized by a turbidite complex consist- ing of slope, fan and basin plain deposits (Casnedi, 1988; 1991) (Figure 5). The inner part of the whole in-fi ll succession is characterized by the Figure 3 - Schematic geological map of southern Italy. presence, above the turbidite deposits, of the so- The Bradanic Trough (foredeep) is located between the called “allochthon”, which emplaces predominantly Apennines (chain) and the Murge (foreland) (modifi ed from Pieri et al., 1997a). pre-Pliocene deformed units (Mesozoic to Paleogene preorogenic units passing to Miocene synorogenic biostratigraphic and structural constraints, Patacca ones) over Pliocene to Lower Pleistocene foredeep and Scandone (2001) suggest a lithostratigraphic link deposits (Figure 2). The “allochthon” was considered between different successions of the whole foredeep a gravitational slide of the frontal part of the Apen- systems, while, according to lithostratigraphic and nines chain which moved towards the axis of the fore- sedimentologic constraints, Tropeano et al. (2002a) deep, but most recent data indicate that it represents suggest a schematic depositional framework for the a long thrust sheet system (as long along the dip as whole foredeep system (Figure 6). the Apennines chain is wide - Figure 2) which over- thrusts the Apulian platform units and their foredeep 2.1 The Bradanic Trough cover (Mostardini and Merlini, 1986). According to The Bradanic Trough (Migliorini, 1937; Selli, 1962) Patacca and Scandone (2001), the buried front of is the Pliocene to Pleistocene south-Apennines fore- the “allochthon” represents the tip line of the most deep sector, developed between the chain front and external frontal ramp of the duplex system, active in an exposed and fl exured karstic foreland (the Apulian earliest Pleistocene time (Santernian).

Foreland) (Ricchetti, 1980; Ricchetti and Mongelli, According to Pieri et al. (1994a; 1996a) and Tro- P14 to P36 olume n° 4 - from 1980) (Figure 3). The upper part of the in-fi ll succes- peano et al. (2002a) three representative succes- sions crops out (up to about 600 m in thickness) and is sions describe the Bradanic Trough in-fi ll. They are V mainly characterized by silty clay hemipelagites (the measured along WSW-ENE transects, perpendicular Argille subappennine Formation), which are either in to the elongation of the trough (Figure 5) and their transitional or in erosional contact with the overly- thickness depends on the inclination of the Apulian ing coarse-grained deposits (the “Regressive coastal Foreland ramp: thicker successions, associated with deposits”) (Pieri et al., 1996a) (Figs 5, 22, 26). A both the “allochthon” and turbidites, developed on carbonate unit (the Calcarenite di Gravina Formation) the inner foreland ramp, a sector of the trough with a crops out in the outer margin successions onto the highly inclined bedrock surface; thinner successions, Apulian Foreland and below the Argille subappen- not associated with the “allochthon” and turbidites,

5 - P35

P35_R_OK 5 9-06-2004, 10:42:30 P35_R_OK 6

Volume n° 4 - from P14 to P36 P35 - P35 Leaders: P. Pieri,L.Sabato,M.Tropeano grained coastalandalluvialdeposits(the“Regressive subappennine Formation), andsubsequently, coarse- the turbiditedeposits.Hemipelagites(the Argille of turbidites;the“allochthon”tectonicallyoverlies hemipelagites whichpassupward intoathickpile basin -succession A inFigure5b)arecomposedof i) innersuccessions(outerfrontofthewedge-top follows: these stratigraphicsuccessionscanbesynthesizedas the innertooutermargins oftheBradanic Trough, and aroundthehighsofexposed foreland.From foreland ramp(pre-Murge andpre-Gargano plateaux) developed ontheouter, lessinclined,sectorofthe section (a)(Tropeano etal.,2002a). basin (modifi section ofthesouthern Apennines beltanditsforeland F igure 4-a)Structuralandgeodynamicsketch ofa

ed fromDoglionietal.,1994);b)detailofthe fi lagites (the Argille subappennineFormation) and, of turbiditeswhich,inturn,areoverlain byhemipe- of hemipelagiteswhichpassupwards intoathickpile “allochthon”, areupto2kmthickandcomposed cession BinFigure5b)areadjacenttothefrontof presently exposed basinandhave avariable thickness outer forelandramp)characterizeawideareaofthe iii) middleandoutermargin successions(middleand and ontheoutermargin ofthetrough; with similardepositsformedbothonthewedgetop and coarse-graineddepositsarelaterallycontinuous (the “Regressive coastaldeposits”).Hemipelagites ii) thickdepocentersuccessions(foredeep “allochthon”, isintheorderof3-4km; The wholethicknessofthissuccession,includingthe coastal deposits”)capthesequenceonwedgetop.

nally, bycoarse-grainedcoastalandalluvialdeposits s.s. 9-06-2004, 10:42:32

- suc- PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35 logical cross-sections in which the structural logical cross-sections in which indicate the most representative successions of the indicate the most representative 2 and C 1 lling the Bradanic Trough are shown; A, B, C are shown; lling the Bradanic Trough

olume n° 4 - from P14 to P36 olume n° 4 - from ed from Pieri et al., 1994a; 1996a).

V ll (modifi

igure 5 - a) Schematic geological map of the deposits outcropping in the Bradanic Trough (for location see Figure 3); b) geo location see Figure (for geological map of the deposits outcropping in Bradanic Trough igure 5 - a) Schematic eatures of the substratum and the distribution of the deposits fi eatures of the substratum and distribution F Bradanic Trough in-fi Bradanic Trough f

7 - P35

P35_R_OK 7 9-06-2004, 10:42:35 P35_R_OK 8

Volume n° 4 - from P14 to P36 P35 - P35 Figure 6 - Paleogeographies of the south-Apennines foreland basin system from Messinian to Middle Pleistocene (Tropeano et al., 2002a). Leaders: P. Pieri,L.Sabato,M.Tropeano 9-06-2004, 10:42:37 PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35

from a few tens of metres up to 1 km. They are mainly composed of hemipelagites (the Argille subappennine Formation) passing to coarse-grained shallow-marine and alluvial deposits (the “Regressive coastal depos- its”). The relatively thicker successions (middle fore- land ramp) are located in the central part of the basin (succession C1 in Figure 5b). The thinner successions (outer foreland ramp) are located in the eastern part of the basin (succession C2 in Figure 5b) with a basal unit of transgressive shallow-marine carbonates (the Calcarenite di Gravina Formation) overlain by hemi- pelagites (the Argille subappennine Formation) and fi nally by coarse-grained deposits (the “Regressive coastal deposits”). On the foreland side of the trough, these thin successions are completely exposed from the bedrock and also characterize some depressions inside the Apulian Foreland (i.e. the Murge grabens and the Brindisi basin). It is important to underline that Lower to Middle Pleistocene shallow-marine and/or continental de- posits (the “Regressive coastal deposits”) covered the clay of the three types of succession; elevations of regressive deposits of up to more than 600 m and the Figure 7 - Field trip itinerary of the fi rst day. incision of deep valleys clearly demonstrate the Qua- ternary uplift of the region (Pieri et al., 1994a; 1996a; Mesozoic sedimentary cover overlain by relatively Tropeano et al., 2002b). thin and discontinuous Tertiary and Quaternary de- posits (Ricchetti et al., 1988). The sedimentary cover 3. Field itinerary was drilled by exploration wells and is composed of a syn-rift and passive-margin succession developed DAY 1 on metamorphic Hercynian rocks. This succession (no difficulty) is composed of: Permo-Triassic red beds about 1 km thick and correlatable to the Verrucano Fm., evapor- We will spend the morning of the fi rst day travelling ites, from about 1 to 2.5 km thick and correlatable to by bus from Florence to the area of interest. the Anidrite di Burano Fm., and well-bedded Jurassic- The evening of the fi rst day is dedicated to the Cretaceous carbonates of generally restricted platform description of stratigraphic, structural and geomor- or back-reef facies, from about 3 to 5 km thick. This phological regional features of the Apulian Foreland succession represents the Apulian carbonate platform in the Murge area (stops 1.1 and 1.2). In particular, a succession. Pleistocene forced-regressive Gilbert-type delta that Regionally the Apulian Foreland corresponds to a developed during foreland subsidence will be visited wide WNW-ESE trending antiform (Ricchetti, 1980; (stop 1.3), (Figure 7). Ricchetti and Mongelli, 1980; Royden et al., 1987)

3.1 The Apulian Foreland (Figure 2) which is obliquely oriented with regard P14 to P36 olume n° 4 - from M. Tropeano, P. Pieri, V. Festa , M. Moretti, to the south-Apennines subduction hinge (Casnedi, L. Spalluto 1988; Doglioni et al., 1994; Pieri et al., 1996a). Large V The Apulian Foreland (“Avampaese apulo” of Selli, deformation zones, striking oblique or perpendicular 1962) (Figs 2, 3, 4, 6) represents the south-Apennines to the main antiform trending, segment the outcrop- foreland and is a sector of the Adria Plate character- ping portion of the Apulian Foreland in three main ized by a relatively thick lithosphere and by a weakly blocks with different degrees of uplift, from the deformed and autochthonous sedimentary cover. It higher Gargano and Murge to the lowland Salento shows a uniform crustal structure with a Variscan towards the SE (Ricchetti et al., 1988; Funiciello et crystalline basement and an approximately 6 km thick al., 1991; Doglioni et al., 1994; Gambini and Tozzi, 1996) (Figs 3, 6).

9 - P35

P35_R_OK 9 9-06-2004, 10:42:44 P35_R_OK 10

Volume n° 4 - from P14 to P36 P35 - P35 Leaders: P. Pieri,L.Sabato,M.Tropeano Fm. (Valduga, 1965;Pieri,1980;Ciaranfi the CalcarediBariFm.from Altamura by bauxites,greenclaysand/ormarlysands,separates southern sector;amildangularunconformity, marked trichtian), about1000mthickandcroppingoutinthe Calcare di Altamura Fm.(Upper Turonian toMaas- thick andcroppingoutinthenorthernsector, andthe (Valanginian toUpperCenomanian),about2000m tions weredistinguished:theCalcarediBariFm. et al., f by monotonous,well-bedded,restrictedcarbonate to the Apulian platform,ismainlycharacterized of theMurge; they arelikely relatedtothe Quaternary tures andcausethepresent-daylow-energy seismicity The mostrecentfaults cutorreactive ancientstruc- (the CalcarenitediGravina Fm.). recorded bydepositionofshallow-marine carbonates subsidence andtransgressionontotheMurge region is del ”ofMartinis,1961). The Plio-Pleistocene plateau fromtheBradanic Trough (“faglia della Valle One oftheseyoungerfaults boundstheMurge Alte foreland subsidenceby W-WS dippingnormalfaults. cut duringtheMiddlePliocene-EarlyPleistocene the Murge area, atleastLateCretaceousinage,were ancient structures,thoselocatedinthewesternsideof es fromCretaceoustoPleistocene;amongstthemost semigrabens, E-NEdisplacedblocks.Faults agerang- E-NE dippinglistricfaults whichbound,through movement (Festa,2003). The shapeisthatofregional trending surfaces reveal dextral transtensional f cording tokinematicindicators,theNW-SE trending an archedshapewithconvexity towards theSW; ac- Pieri, 1982).Inmapview, faults andgrabensshow ally elongatedmaingrabensarepresent(Iannoneand shelf). Betweentheblocks,two narrow andregion- (the “Murge Basse” plateauandthe Apulian Adriatic placed blocksthatareupto15-20kmby60-80 sea-level, fl 15-20 kmby60-80andabout500-600mabove trending plateau(the“Murge Alte” plateau),about The latterischaracterizedbyalarge centralNW-SE ov belonging totheBradanic Trough sedimentarycycle tinuous andthinUpperPliocene-Quaternarydeposits Luperto Sinni,1996, Ricchetti (Pieri, 1980;Ricchetti,Ciaranfi sion cropsout,showing SWandSSWdipdirections during ourfi As regards theMurge area(theforelandblockcrossed acies (Ricchetti1975;1980;Pieri,Ciaranfi ault surfaces reveal dip-slipmovement whileE-W erlie theCretaceoussuccessionofMurge high.

1988; LupertoSinni,1996). Two mainforma- et al.,

anked totheNEbyfault-bounded dis- eld trip),a3-km-thickCretaceoussucces-

1988). This succession, belonging succession, 1988). This and references therein

et al., et al. ). Discon- , 1988;

1988;

3.2 The Calcarenite diGravina Fm. Euroecent coin). Middle Ages byFederickII(depictedontheItalian1 isolated structuralhighwhereacastlewas built inthe Gravina”). “CasteldelMonte”isasmallconicaland al suggest upliftratesofatleast0.5mm/yr(Doglioni the orderof0.2-0.3mm/yr, whereasstratigraphicdata Pleistocene geochronologicaldata,upliftratesarein terrazzati”) (Ciaranfi by thinmarineterraceddeposits(“Depositimarini recorded bypaleocliffs, abrasionplatforms,and/or by thepresenceof16ordersupliftedshorelines, As regards theupliftofMurge, thisistestifi peano correspond todaytoahorstandgrabensystem(Tro- (Fig 6a);asawhole,Murge andpremurge plateaux (“premurge plateau”in:Pieri al. characterized bysimilarstructuralfeatures(Sella bedrock oftheBradanic Trough fi The buried foreland ramp,whichrepresentsthe plate (Pieri uplift oftheMurge inducedbythebuckling ofthe i.e. as upto200mdeepdolinas(locallycalled“puli”, tectono-karstic structures,someofwhichevolved sions. Depressions,fi characterized byaseriesofgentlehillsanddepres- Murge Alte plateaufromtheOfanto Graben. the scarp. Another scarpboundstowards W-NW the and dippingSW. A Quaternarybajadadevelops along (“faglia della Valle delBradano”) strikingNW-SE The scarpcorrespondstoarecededmainnormalfault SW theMurge Alte plateaufromthe Bradanic Trough. A 150mhighand30kmlongscarpboundstowards The Murge Alte plateauandtheBradanic Trough Stop 1.1: rine carbonatesofFigure5band Gravina Fm.recordsthistransgression(shallow-ma- Upper PliocenetoLower Pleistocene Calcarenite di highest one(theMurge Alte plateau). The Middle- gression ontotheplateaux,except forthetopof roll-back ofthe Adria Plate,producedasevere trans- Subsidence oftheMurge, inducedbytheeastward M. Tropeano The topoftheMurge Alte plateau isnotfl “Castel delMonte” Stop 1.2: ., 1996, , 1988),mainlyintheareaadjacenttoMurge

the “Pulodi Altamura” andthe“Pulicchiodi et al. and references therein , 1997). et al. , 1997a; Tropeano

et al.

lled by , 1988). According toLate terra rossa et al. ).

lling succession,is et al. , 1994a;1996a) , 1997). , represent

at, but is 9-06-2004, 10:42:46

ed et et

PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35

6). This thin formation (no more than 70-100 m in Calcarenite di Gravina Fm. progressively onlapped thickness) derives from a mantle of bioclastic and/or the Murge paleoarchipelago by: i) aggradation against lithoclastic carbonates deposited on the faulted rocks degraded fault scarps (stops 1.3, 2.1-2.4); ii) fl ood- of the Apulian Foreland, and crops out on the outer ing of narrow shore platforms around paleoislands margin of the Bradanic Trough and on the fl anks of (horsts) or their tops (day 2); iii) drowning narrow the Murge plateaux, from the present-day sea level up straits (grabens) (Tropeano and Sabato, 2000). to more than 400 m in elevation (Iannone and Pieri 1979; Tropeano and Sabato, 2000). Stop 1.3: The lower boundary of the Calcarenite di Gravina Fm. The Minervino Gilbert-type delta is a long-term ravinement surface abraded onto the L. Sabato bedrock. Carbonates of the formation were deposited In the Minervino area, the western margin of the in shallow-marine systems which regionally onlapped Murge Alte plateau, towards the Ofanto Graben, onto the Apulian Foreland highs (with a backstepping displays one of the best examples of a steep, fault- confi guration), or covered the lower plateaux (Trope- bounded paleocoastal relief where limestones of the ano and Sabato, 2000; Pomar and Tropeano, 2001). Calcarenite di Gravina Formation, locally up to 40 Skeletal grains are the basic components of the m thick, onlap the Cretaceous substratum (Figure Calcarenite di Gravina Fm. and consist of abundant 8). Locally the Calcarenite di Gravina Fm. includes bivalves, echinoids, red algae, serpulids and benthic a conglomerate body (<12 m thick), interpreted as forams, fragments of barnacles, brachiopods, gastro- a terraced Gilbert-type delta (Sabato, 1996a). The pods, bryozoans and rare planktonic foraminifera. delta, exclusively composed of rounded clasts of This carbonate assemblage can be interpreted as a Cretaceous limestones, is situated adjacent to an up temperate-water deposit and is comparable to the to 150-m-high major degraded N-S trending fault molechfor facies of Carannante et al. (1988), typical scarp, which represents the Pliocene to present-day of a temperate-water open shelf or ramp carbonate structural boundary between the Murge Alte plateau factory. A particular feature characterizes the lithology (≈500-600 m in height) and the lower terraced surface of the formation: the presence of terrigenous carbon- (≈325 m in height). The modern relief is cut by steep ate grains. The latter are mixed within bio-lithoclastic karstic canyons (locally termed gravine). facies or may form either isolated bodies (stop 1.3), The Minervino delta has a length of approximately or, locally, may comprise the whole Plio-Pleis- 200 m, and its most proximal part sits unconform- tocene succession (stop 2.2). Terrigenous carbonate ably on the Cretaceous bedrock and is comprised facies are commonly composed of coarse sand- and of Lithophaga-bored boulders (<0.7 m). Relief of gravel-sized lithoclasts (calclithites and calcrudites) the west-dipping delta foresets increases basinwards eroded from the Cretaceous bedrock of the Murge from a few tens of centimetres to 10 m, a thickening islands during transgression. Sedimentary structures that is accompanied by a decrease of foreset dips from are mainly indicative of deposition in wave- and/or an angle of 30° to a few degrees. Beds are exclu- storm-dominated environments. sively comprised of pebble-boulder grade limestone From NW to SE and from W to E carbonate systems lithoclasts with large oysters (<0.2 m) colonizing bed- were diachronously covered by hemipelagites of the ding surfaces. Bottomsets beds are composed of ma- Argille subappennine Formation at progressively trix-rich coarse sands and interbedded conglomerates. higher levels on the fl anks of the foreland-highs (Pieri A 2 m thick tabular gravelly unit rests with erosional et al., 1996a). A drowning unconformity bounds the unconformity on the truncated delta foresets and Cre- top of the Calcarenite di Gravina Formation (Trope- taceous bedrock. This unit fi nes upward, and is com- P14 to P36 olume n° 4 - from ano and Sabato, 2000).

prised of conglomerates and coarse sands with a fi ne V As faulting of the Murge high mostly occurred prior sand-grade matrix; it displays very low-angle (1°-2°) to Plio-Pleistocene transgression (Figure 6a), the clinostratifi ed beds, with bioturbations (echinoids), antecedent topography of the Murge area was an occasional faunas of small molluscs and imbricated important control factor on the development of the clasts dipping both land- and seaward. Calcarenite di Gravina Fm. and, during drowning, The Gilbert-type delta (Gilbert, 1885) at Minervino, the Murge region became an island archipelago (Figs. was wave cut, terraced and overlain by a package that 6a, 6b). Horst-and-graben structures in the foreland records upward deepening from shoreface to offshore controlled the distribution of emerged land, basins, environments. The supply of clastic sediment to the islands and straits and, consequently, deposits of the

11 - P35

P35_R_OK 11 9-06-2004, 10:42:47 P35_R_OK 12

Volume n° 4 - from P14 to P36 P35 - P35 Leaders: P. Pieri,L.Sabato,M.Tropeano deformation structures(seismites)thatdeveloped in descriptions ofgrowth structuresand soft-sediment In theafternoon,attentionwillbefocusedon will beobserved (stops 2.1-2.4)(Figure9). bodies, whichbacksteppedonthefl In themorning,coarse-grained,clinobeddedcoastal era area,willbediscussed. Calcarenite diGravina Fm.,outcroppingintheMat- During theseconddaysomeparticularfeaturesof (low tomiddlediffi within akarsticcanyon, similartothe delta was probablyviaanephemeralstreamlocated conglomeratic matrix,fi in thedeltaapex wherelarge boulderssetinasandy- Indeed, aremnantofthisfeedercanyon ispreserved yons) observed todayintheMurge Alte karsticarea. (Sabato, 1996a, Tropeano andSabato,2000). supply was unlikely relatedtoautocyclic processes have beenimpossible,sothatthecessationofclastic ently confi relief. Sincethestreamthatfeddeltawas appar- feature thatcutsthroughtheoriginal,steep,coastal (photo). ov Fi gure 8-Geologicalsectionshowing thestratigraphicrelationshipbetween theCretaceoussubstratumand erlying Plio-QuaternarydepositsclosetoMinervino. A terracedGilbert-typedeltaisvisiblealongthewall ofaquarry

ned withinthecanyon, avulsion would

culties) DAY 2 DAY 2

ll andfossilizeanerosional

e xuring foreland, gravine (can- 3.3 The Plio-Pleistocene transgression ontothesmall, the CalcarenitediGravina Fm.(stop2.5)(Figure9). and upto500minelevation, standsoutfromclaysof tem. Today, theMateraHorst,afew tensofkm e graben systemandtheMateraHorst,todaypartially the Bradanic Trough arecharacterizedbyahorstand Region). Boththe Murge areaand the substrateof the Bradanic Trough totheS-SE(inBasilicata Murge areatotheN-NE(in Apulia Region) and middle-outer forelandramp,betweenthewider Structurally, theMateraHorst islocatedwithinthe ranean (IonianSea)withthe Adriatic Sea. ennines highlandsandconnectedtheopenMediter- Tr southwest, aseaway about50kmwide(theBradanic 6- to7-km-widegraben(Viglione Graben). To the separated fromthemainMurge archipelagobya ence-driven transgression. Towards thenorth,itwas which fi island duringLatePliocene-EarlyPleistocenetimes, The MateraHorst(Murge diMatera)was asmall M. Tropeano, P. Pieri,L.Pomar drowning, Matera paleoisland xposed, isoneofthemostelevated horstsofthesys- ough) separatedthissmallpaleoislandfromthe Ap-

nally drowned duringtheregional subsid- 9-06-2004, 10:42:49 2

wide PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35

Figure 9 - Field trip itinerary of the second, third, and fourth days.

the Argille subappennine Fm., which fi lled both the Along the southern fl ank of the paleoisland these car- Viglione Graben and the Bradanic Trough (Figure bonates are mainly lithoclastic in origin with compo- 10). A spectacular deep canyon, the “Gravina di Mat- nents derived from erosion of Cretaceous limestone. era” (Figure 11), cuts the horst and widely exposes The spectacular coastal onlap onto the bedrock of the both the Cretaceous substrate of the foreland and the paleoisland is exposed near the town. Plio-Pleistocene covers. We will spend several nights in Matera. The old town Stop 2.2: was excavated in the Calcarenite di Gravina Fm. and Backstepping of accretional units is called “Sassi di Matera” (Figure 11), (“sassi” is at Lamaquacchiola the Italian word for stones). Since 1993 the Sassi di The southern margin of the Matera paleoisland Matera have been on the World Heritage List with the was a moderately-inclined (up to 5°) rocky slope surface. Here the Calcarenite di Gravina Formation following justifi cation: “This is the most outstand- P14 to P36 olume n° 4 - from ing, intact example of a troglodyte settlement in the is composed of accretional units bounded by erosion

Mediterranean region, perfectly adapted to its terrain surfaces. The accretional units are prism shaped, V and ecosystem. The fi rst inhabited zone dates from the elongated in strike section and parallel to the Paleolithic, while later settlements illustrate a number paleocoast line. They provide continuous exposure of signifi cant stages in human history”. of coarse-grained, gravel-dominated coastal systems and are composed of several lithofacies which are Stop 2.1: conglomeratic at the proximal end (rocky coast) and The Gravina di Matera canyon become progressively sandier basinward. Lithofacies The Gravina di Matera canyon offers some of the best range from shoreline to offshore, and are basically exposed sections of the Calcarenite di Gravina Fm. dominated by limestone gravel comprised of pebbles

13 - P35

P35_R_OK 13 9-06-2004, 10:42:51 P35_R_OK 14

Volume n° 4 - from P14 to P36 P35 - P35 Leaders: P. Pieri,L.Sabato,M.Tropeano the paleoshorelineandprogradeseaward. (Figure 12). These arelaterallyextensive, parallelto large-scale, high-angle,cross-beddedlithosomes important arethetransition-slopedepositswhichform f systems onthesmallcalcareouspaleoisland. Among bedrock, andbythelackofsignifi e abundance oferosionterraces(shoreplatforms) coastal system;thissettingissuggestedbythe Gravelly depositsdeveloped inawave-abraded bioclastic, isonlysignifi and granules.Carbonatesand,eitherlithoclasticor F acies, themostconspicuousandvolumetrically xcavated intotheintenselyfracturedlimestone igure 10-GeologicalmapandgeologicalsectionoftheMateraarea(afterTropeano, 1992;Beneduceetal.,2004).

cant inoffshore settings.

cant alluvial/fl

uvial frequency cycles andstillstandsof relative sealevel. induced transgressionthatwas punctuatedbyhigh- confi Accretional unitsarestacked inabackstepping der wedgesreplacebeachface oncliffed coastlines; breaking waves andwave-swash processes;(a’)boul- - (a)thebeachface: indicatesthezoneaffected by accretional bodies(Figure13): F accretional units Depositional systemsrecorded inthe Stop 2.3: our maindepositionalzonesaredifferentiated inthe

guration whichresultedfromasubsidence 9-06-2004, 10:42:53 PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35

- (b) the shoreface: indicates the gently inclined zone dominated by wave traction and where, during large wave activity, sediments were swept seaward; - (c) the transition slope: in- dicates the steep zone locat- ed seaward of the shoreface, just below the major wave- base level. Tractive fl ows, triggered by storm waves and wind-induced currents, swept the shoreface. At the storm wave base, the fl ows changed from tractive to gravity-driven, and deposi- tional slopes developed as a result of sediment avalanche processes. The transition slope represents one sector of the coastal-equilibrium profi le and migrates accord- ing to the evolution of the depositional system. The extensive lateral continuity of these lithosomes excludes an interpretation as wave-re- worked, Gilbert-type deltas. Migration of large bedforms (i.e. sand ribbons or sand waves) are likewise excluded after considering the three- dimensional characteristics of the prograding lithosomes Figure 11 - Panoramic view of “Sassi” di Matera. The at Matera. Additionally, their basinward progradation contact between the Cretaceous substratum and the Plio- also excludes other possible interpretations such as Pleistocene Calcarenite di Gravina Fm. is located at the spits or other shore-parallel prograding bodies; base of the city. - (d) the offshore: indicates the area dominated by low olume n° 4 - from P14 to P36 olume n° 4 - from V

Figure 12 - Spectacular clinoforms of the transition slope (Lamaquacchiola).

15 - P35

P35_R_OK 15 9-06-2004, 10:42:58 P35_R_OK 16

Volume n° 4 - from P14 to P36 P35 - P35 Leaders: P. Pieri,L.Sabato,M.Tropeano with structuresrangingfromkilometrictometric characterized byacomplex horstandgrabensystem, the premurge plateauoutcrops,theforelandrampis Fm. Basically, wheretheCretaceoussubstratumof limestones belongingtotheCalcarenitediGravina of tensionalandtranstensionalgrowth faults in “Gravina diPicciano”canyons show theoccurrence Spectacular outcropsalongthe“Bradano”and M. Tropeano, V. Festa ,M.Moretti,P. Pieri in theCalcarenite diGravina Fm. 3.4 Growth andsoft-sedimentdeformationstructures paleoisland. the inclinednorthernfl bioclastic bodiesformed. These fan bodiescover to 20°)existed andasetofsuccessive fan-shaped northern fl large westwardly-prograding fan-like bodies.Onthe shaped accretionalunitsterminateandpassinto At thewesternendofpaleoisland,prism- The “ChieseRupestri”panorama Stop 2.4: iment starving,inwhichbioturbationwas signifi w T F ropeano, 2001). igure 13-Schematic depositionalsystemofthecoastalbodiesdeveloping ontheMaterapaleoisland(Pomar and ater-energy conditionsandprogressive seaward sed-

ank ofthispaleo-capeasteeperslope(up

ank ofthecorner

cant. during thesedimentation,thisalternationconstituted of grainstonesandpackstones.Ontheseabottom, decimetres thickandaremadeupofanalternation form, uptoafew kmwideandlong. Bedsarefew Pliocene timesbecameanisolatedcarbonateplat- developed ontopofasmallhorstwhichduringLate movements. Moreover, thelimestonesuccessionwas folds indicatemainlyvertical ratherthanhorizontal ential vergence (typicalofslumps)hasbeenfound; and distortedbedswithdecimetricfolds.Noprefer- sediment deformationstructuresshow convoluted deformation. Regarding thegeometry, thesesoft- formed bedsallow ustoreferthemasoft-sediment beds andtheirconfi occurs (Figure14). The geometryofthecontorted Fm., anupto2-3-m-thickhorizonofcontortedbeds Locally, inthelower partoftheCalcarenitediGravina ano at leastaMiddlePleistocenetectonicactivity (Trope- others completelycutthesevery deposits,recording sedimentation oftheCalcarenitediGravina Fm.,but formations. Someofthestructuresgrew duringthe the UpperPliocene-Lower Pleistoceneoutcropping a pre-,syn-andpost-depositionalactivity referredto scale (Tropeano et al. , 1994;1997). et al.

nement inahorizonwithinunde- , 1994). These structuresshow 9-06-2004, 10:43:05 PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35

a multilayer unstable system with reverse density gra- dients (a potential driving force system for the origin of soft-sediment deformation structures) (i.e. Anketell et al., 1970). The occurrence of synsedimentary faults and the lateral extension of the deformed horizon (which may be followed for more than 1 km) allow us tentatively to refer the trigger of the deformation to a seismic shock. Stop 2.5: “Gravina di Picciano” canyon at Mandolalena The small graben at Mandolalena is one of the best examples of tectonic structures which grew during the sedimentation of the Calcarenite di Gravina Fm. At the base of the formation, a 2-m-thick horizon charac- terized by soft sediment deformation structures may be observed (Figure 14). DAY 3 (low to medium diffi culties) Figure 14 - Detail of the soft-sediment deformation The morning of the third day is dedicated to the de- structures displayed in the Calcarenite di Gravina Fm. scriptions of the main tectonic units and structures of (Mandolalena). the Apennines frontal imbricate fan (stops 3.1-3.6); (Figure 3). Two sedimentary cycles, bounded by an the evening is dedicated to the description of the unconformity surface and both showing syntectonic satellite deposits in the Tricarico area (stops 3.7-3.9) sedimentary features, have been distinguished within (Figure 9). the Ariano Unit successions (Maggiore and Walsh, We will discuss the relationship between 1975; Caldara et al., 1993; Sabato and Marino, 1994; and sedimentation in a thrust-top basin context (Fig- Ciarcia et al., 2003, and references therein). ure 4). Near the chain front these successions were succes- sively cut by several tight thrust planes, the youngest 3.5 Satellite successions near the front of the Apen- of which (the Stigliano ramp) developed around the nines (the Tricarico example) Early-Middle Pleistocene boundary (according to L. Sabato, S. Gallicchio, P. Pieri, M. Tropeano Patacca and Scandone, 2001). Within the south-Apennines chain, from the Abruz- zo-Molise regions to the Basilicata region, Upper Before observing the satellite succession of the Ari- Tortonian to Lower Pleistocene siliciclastic and, ano Unit, we will discuss some features of the chain, subordinately, carbonate deposits unconformably rest mainly in the “Dolomiti lucane” relief. on older and previously deformed chain units. These deposits developed onto the moving “allochthon” 3.6 Regional tectonics of the south-Apennines chain (thrust-top basin) and, according to their age, fall M. Schiattarella within the Villamaina, Altavilla or Ariano units (Ip- The southern Apennines are a NE-verging orogenic polito et al., 1975; Bonardi et al., 1988). They crop

wedge accreted from Late Oligocene-Early Miocene P14 to P36 n° 4 - from Volume out discontinuously and, despite their age correlations, to Pleistocene. The chain is composed of a Mesozoic- they were considered as having been deposited within Cenozoic sedimentary cover derived from the defor- different satellite sub-basins (i.e. Ofanto, Benevento, mation of several paleogeographic domains (i.e. the Potenza, basins). The Ariano Unit represents Ligurian oceanic crust and the western passive margin the most recent (Early Pliocene to Pleistocene) and of the Adriatic plate) and of the Neogene-Pleistocene the most external of these units, and forms a dis- piggyback basin and foredeep deposits of the active continuous belt of some tens of kilometres in width margin. Recent shortening occurred at the belt front near the outer margin of the south-Apennines chain deforming Pleistocene sediments and volcanics (Pieri

17 - P35

P35_R_OK 17 21-06-2004, 9:44:58 P35_R_OK 18

Volume n° 4 - from P14 to P36 P35 - P35 Leaders: P. Pieri,L.Sabato,M.Tropeano Ty still active alongthesouth-Apenninesaxialzoneand et al. the “DolomitiLucane”. w shallow-water anddeep-seasuccessionsoftheLagonegro,NumidianIrpinianbasins;6.Meso-Cenozoicshallow- 4. Meso-Cenozoicshallow-water carbonatesoftheCampania-Lucaniaplatform; 5.Lower-Middle Triassic toMiocene v F tectonic unitsareobserved (Prosser the bottomofaccretionarywedge,following to the Adriatic (Apulian)foreland,andfromthetopto In aregional cross-section,fromthe Tyrrhenian Sea tarella, 1998, according toN120°±10°andN50-60°trends(Schiat- Plio-Quaternary strike-slip faults, mainlyoriented coaxial normalfaults. The beltislargely affected by corresponding tothestrike ofthemainthrustsand The average trendofthechainaxisisaboutN150°, al. in age(Ligurianunits,Bonardi ably covered bysyntectonicdeposits,EarlyMiocene rella, 1988;Monacoand Tortorici, 1995),unconform- ophiolitic units(Knott,1987,MauroandSchiatta- Figure 15:(1)JurassictoOligocenepolydeformed ing fromEarly Triassic toLower-Middle Miocene units mainlycomposedofdeep-seasediments,rang- Early Miocene(D’Argenio form), theageofwhichrangesfromLate Triassic to carbonate platformunit(Campania-Lucaniaplat- olcanics; 2.Miocenesyntectonicdeposits;3.CretaceoustoOligoceneophiolite-bearing internalunits(Ligurianunits); igure 15-Geologicalsketch mapofsouthern Apennines. Legend:1.Plio-QuaternaryclasticsandQuaternary ater carbonatesofthe Apulian platform; 7.Thrustfrontofthechain; 8. Volcanoes. Black frameindicatestheareaof , 1992; Amato andMontone,1997). rrhenian side(Brancaccio , 1997b)whilstwidelydocumentedextension is and references therein et al. et al. et al. , 1975);(3)several , 1991;Ortolani ). et al. , 1988b);(2)a , 1996)in et Stratigraphic andtectonicrelationships between Stop 3.1: and sandstones(Pescatore Cretaceous toLower Miocenedeep-seamarls,shales Mazzoli, 1992);(4)afrontalimbricatefan madeupof ( units,Scandone,1967;Miconnet,1988; Middle toUpperMiocenefl al. times canbeestimatedat1mm/yr(Schiattarella age upliftrateoftheentirechainduringQuaternary strain ratecanbeinferred(about1cm/yr). The aver- south-Apennines (about20Ma),avery high to therelevant shorteningandthetimespanof of theLigurianunits(Schiattarella orogenic wedge,excluding theinternaldeformation ing toabout200km)hasbeencalculatedforthe A conservative shorteningupto100%(correspond- (Mostardini andMerlini,1986). towards theeastlessdeformedforelandarea the baseofaccretionarywedgeandwhichforms ate platform,whichhasbeenpartlyincorporatedat deposits (Pieri 1988); (5)PliocenetoPleistoceneforedeepclastic , 2003). et al. , 1996a);(6)the Apulian carbon-

et al. ysch deposits(Pescatore, , 1999)covered by et al. , 1997).Due 9-06-2004, 10:43:09 et PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35

fl ysches and pre-orogenic units. At this stop-site trend and channel facies (Pescatore et al., 1980). the general structure of the whole area can be easily These rocks are part of the Gorgoglione Flysch, an observed (Figure 16). The beds of the Gorgoglione Upper Miocene synorogenic succession of the Irpin- Flysch unconformably lie on Cretaceous to Oligocene ian realm (Pescatore, 1978). Specifi cally, the Irpinian shales (Pescatore and Tramutoli, 1980), representing trough represented the entire Miocene foredeep of the pre-orogenic succession severely deformed by the the southern Apennines, in which several silici- and older tectonic stages. This fl ysch, towards the east, calcareous-clastic successions deposited (i.e. Serra thrusts on the Numidian sandstone (Patacca et al., Palazzo Formation, Faeto Flysch, Castelvetere For- 1992; Pescatore et al., 1992), a well-known Lower mation), whilst the Gorgoglione Flysch (Ogniben, to Middle Miocene quartzarenite turbidite formation 1969) is currently interpreted as a piggyback basin largely outcropping from Maghreb to southern Spain succession (Pescatore, 1988; Pescatore et al., 1999).

Figure 16 - Schematic cross-section of the “Dolomiti Lucane” area (not in scale). FG = Gorgoglione Flysch From a geomorphological standpoint, one can observe (Upper Miocene); FN = Numidian Sandstone (Lower- in the “Dolomiti lucane” area, besides the above-men- Middle Miocene); AV = “Argille varicolori” (Upper tioned strongly morpho-selected landscape, the effects Cretaceous – Oligocene). of the superimposition phenomenon of the Caperrino River, a tributary of the Basento River, which deeply and Italy (Flysch Numidico Fm. in Ogniben, 1963). cuts the Gorgoglione Flysch carving major gorges and narrow minor channels that are responsible for 3.7 The “Dolomiti lucane” relief the beautiful exposition of most of the succession. M. Schiattarella Rock pinnacles and needles - generated by fracturing The “Dolomiti lucane” relief is a sharp NW-SE-trend- coupled with erosion processes, sometimes promoting ing ridge located in the external belt of the Lucanian rock falls by seismic triggering - complete the spec- Apennine, a segment of the Neogene chain forming tacular landscape of the “Dolomiti lucane”. the geological backbone of southern Italy (Figure 15). The “Dolomiti lucane” area is included in the unit Stop 3.2: 4 (frontal imbricate fan). Accordingly, its structural The “Dolomiti lucane” relief. style has been mainly imposed by thrust tectonics This stop shows the stratigraphic and tectonic features of the external sector of the chain. The “Dolomiti lu- of the Gorgoglione Flysch succession, forming a SW-

cane” ridge emerges from the surrounding landscape dipping monocline affected by both growth strata P14 to P36 n° 4 - from Volume in a marked and startling way, due to the clear con- structures and thrusts (Figure 17). trast between the less erodible rocks of the ridge and We will walk to the unique panoramic view towards the other outcropping formations, basically made of the village, surprisingly rooted on the marly-clayey or arenaceous-pelitic successions. The sharply dipping conglomerate and sandstone beds. ridge is in fact mainly constituted by an alternation of well-cemented and thick-bedded conglomerates and sandstones with subordinate pelitic layers, forming a 1500 m thick succession characterized by regressive

19 - P35

P35_R_OK 19 21-06-2004, 9:45:27 P35_R_OK 20

Volume n° 4 - from P14 to P36 P35 - P35 Leaders: P. Pieri,L.Sabato,M.Tropeano and Bradanic Trough, (Lagonegro Basin;NumidianBasin,IrpinianBasin developed onthewesternmargin ofthe Adria Plate different anddiachronoussedimentarybasinswhich to Pliocenelithostratigraphicunits,belonging In thisareathechainconsistsofseveral Cretaceous tocene foredeepinitsinnersector. paleogeography andtheevolution ofthePlio-Pleis- Basento river; thesefeaturesmostlyconstrainedthe be observed alongthedeepandwidevalley ofthe frontal imbricatefan oftheLucanian Apennine can The mainstratigraphicandstructuralcharactersofthe S. Gallicchio thrust belt 3.8 The frontal imbricatefanofthesouth-Apennines is representedbythreemainsuperimposedtectonic Along theBasentovalley, thefrontal imbricatefan by breachingthrustsandextensive strike-slip faults. the Plio-Pleistocenefrontofchainwas affected glomerato diSerradelCedro”Fms.).Furthermore,in Bradanic Trough (“Argille subappennine”and“Con- Pleistocene, overthrust theforedeepdepositsof Early MiocenetothePliocene,and,during different thrustsystemsfromtheLateOligocene- and references therein ). These unitsweresplitinto i.e. Pescatore Figure 17-Panoramic viewofthe“Dolomitilucane”. et al ., 1999, Miocene volcanoclastic turbidite succession( Tufi Cretaceous toOligocenepelagicdeposits,andbythe substratum, representedbytheargille varicolori unit, Gorgoglione Flysch,andbyitsseverely deformed The Pietrapertosatectonicunitisrepresentedbythe press Figure 18),(Gallicchio San Chiricotectonicunits(PTU, VBTU, SCTUin called: thePietrapertosa, Vaglio diBasilicata,and units. Fromthetoptobottomthey areinformally Cretaceous); b)the“calcarenitieargilliti diFontana e radiolaritidiCampomaggiore”unit(Early–Middle Lagonegro basin,andismadeupof:a)the“argilliti Lower-Middle Miocenesuccession,belongingtothe by acontinuousandconformableCretaceousto The Vaglio diBasilicatatectonicunitisrepresented tion oftheGorgoglione Flysch. unit intheEarly–MiddleMiocene,duringdeposi- superimposed ontothe Vaglio diBasilicatatectonic Ogniben, 1969). The Pietraperosatectonicunitwas and istectonicallysuperimposedontheSanChirico ing thrustsequenceofEarly-MiddleMioceneage This tectonicunitismainlyarrangedinaneast-verg- the FlyschNumidicoFm,(Early-MiddleMiocene). Valloneto” unit(LateCretaceous-EarlyMiocene); c) ti di Tusa Formation, anUpperOligocene-Lower a). et al ., 1996;Sabato et al.,in 21-06-2004, 9:45:30 i.e.

PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35

Figure 18 - Geological map showing the main stratigraphic and structural features of the frontal imbricate fan of the south-Apennines thrust belt, between the villages of and Tricarico.

tectonic unit by a breaching thrust which was active structures. during the Middle-Late Pliocene. This structure, the The San Chirico tectonic unit tectonically overlies the Stigliano ramp in Patacca and Scandone (2001), Plio-Pleistocene foredeep s.s. deposits of the Bradanic outcrops in the Basilicata region from Mt. Vulture to Trough either along a wide east-verging subsurface Stigliano village. thrust (i.e. Patacca and Scandone 2001, and refer- The San Chirico tectonic unit is made up of a con- ences therein) or along an outcropping breaching tinuous Cretaceous to Miocene succession, on which Quaternary thrust (-Tricarico ramp) Pliocene wedge-top deposits unconformably lie. The which has NW-SE strike and NE vergence. pre-Pliocene succession is represented by: a) the

“argilliti e radiolariti di Campomaggiore” unit; b) the Stop 3.3: P14 to P36 olume n° 4 - from “calcareniti e argilliti di Fontana Valloneto” unit; c) The Stigliano ramp

the Flysch Numidico Fm; d) the Serra Palazzo Fm, In this stop the breaching thrust that superimposed the V an arenaceous turbidite succession deposited in the Vaglio di Basilicata tectonic unit on the San Chirico Miocene south-Apennines foredeep (i.e. Gallicchio tectonic unit can be clearly observed (Figure 19). and Maiorano, 1999, and references therein); e) the This structure can be correlated to the Stigliano ramp Marne Argillose del Toppo Capuana Fm. (Crostella which was considered, by Patacca and Scandone and Vezzani, 1964), an Upper Miocene muddy unit. (2001), active until the Early-Middle Pleistocene The Pliocene covers rest unconformably on these pre- boundary. In this area the Stigliano ramp affects a Pliocene units and show a depositional arrangement Middle-Upper Pliocene wedge top succession. characterized by angular unconformities and growth

21 - P35

P35_R_OK 21 9-06-2004, 10:43:16 P35_R_OK 22

Volume n° 4 - from P14 to P36 P35 - P35 Leaders: P. Pieri,L.Sabato,M.Tropeano 3.9 The Quaternary front ofthechain side thatfelldown). it aroundtheothersideofsummit(away fromthe pomaggiore village)onitsoriginalsitebyextending cided tobuild CampomaggioreNuovo (thenew Cam- the Duke’s castle, wereinruins. Village people de- tral-southern Italy. All thestructures,whichincluded The landslidefollowed anearthquake whichhitcen- part. The activity oftheemerged thrustrampduring v sively decreaseseastward. However, drillingdatare- outcrops forabout500manditsthicknessprogres- an upperalluvialone,separatedbyaclayey lens.It grained bodyiscomposedofalower deltaic partand Sabato, 1987),isenclosed(Figure5b). This coarse- del Cedro”Fm.(Gambassini,1967;Loiaconoand thick conglomeratebody, the“ConglomeratodiSerra adjacent tothemostexternal outcroppingramp,a clays ofthe Argille subappennine Fm.Inthelatter, Lower Pleistoceneforedeepdepositsrepresentedby chain, theSanChiricotectonicunitoverthrusts the In themostexternal partoftheLucanian Apennine P. part ofthevillagesliddown thefl of whichoccurredduringthespring1885,when (the oldCampomaggiorevillage),theabandonment We ternary NW-SE trendingtranstensional faults. tectonic unit).Here,theStiglianorampiscutbyQua- radiolariti diCampomaggiore”(Vaglio diBasilicata this tectonicunitisunderthrustbythe“argilliti e Chirico tectonicunit). Through theStiglianoramp the Marneargillose del Toppo CapuanaFms.(San cession unconformabyoverlies theSerraPalazzo and In thisareaaMiddle-UpperPliocenewedgetopsuc- (close-up viewoftheStiglianoramp) Campomaggiore Vecchio Stop 3.4: Pliocene sandstones;Plag:clays;Plcg-s:conglomeratesandsandstones. San Chiricotectonicunit;MTC:MarneargillosedelToppo CapuanaFormation; PAA: SerraPalazzo Formation; Pls: F eal atotalthicknessofabout1500minitsproximal igure 19-Overview oftheStiglianorampalongBasentovalley. VBTU: Vaglio diBasilicatatectonicunit;SCTU: Pieri,S.Gallicchio, L.Sabato,M.Tropeano

will crosstheruinsofCampomaggiore Vecchio

ank ofthemountain. (Pieri induced byayoungerandmoreexternal blindthrust sively affected byMiddlePleistocenebackthrusting, s.s. boundary betweenemerged landsandtheforedeep this thick,coarse-grainedbody. The rampwas the the EarlyPleistoceneistestifi peano ley, areclearlyvisible(Figure20). the Pleistoceneforedeepunit,alongBasentoval- relationship betweentheSanChiricotectonicunitand From thisview-point thestructuralandstratigraphic P Stop 3.5: cemented andlocallycross-stratifi of clast-ormatrix-supportedconglomerates,well association isreferredtoadeltaslope. Thick beds taining marinefossilsandbioturbations;thisfacies conglomerates withclays,thatareinterbedded,con- front. Itisenclosedindisorganized matrix-supported several tensofmetresthick,isinterpretedasadelta sorted sandstones(C2,C4). This facies association, bedded conglomeratesbodiesthatincludewell lenticular sandstones(S1),passingupward tocross- conglomerates (C3)and,locallyinterbedded,thin depositional systemiscomposedofwellstratifi The proximalpart(westernsector)ofthelowest - Lowerunit(subaqueousfandeltasystem) distal sectorarerecognizedinsideeachsystem. (Loiacono andSabato,1987). A proximalsectoranda longing totheConglomeratodiSerradelCedroFm. bottom tothetopinoutcroppingsuccessionbe- depositional system,canbedistinguishedfromthe Three mainstratigraphicunits,eachrepresentinga F. Serra delCedro” Formation 3.10 Sedimentaryevolution ofthe“Conglomerato di anoramic viewfrom Calcianovillage Loiacono

area whenawedge-topbasindidnotexist (Tro- et al et al ., 1997b). ., 2002). The gravelly bodywas succes-

ed bythepresenceof

ed (C4),overlie, 9-06-2004, 10:43:19

ed PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35

through a sharp contact, the slope deposits. Thick- tem. Eastward, well-stratifi ed conglomerate facies are ness of these tabular-shaped beds decreases towards arranged into decimetric beds (C2 and C3), associated the east. These features suggest reworking in shallow to thinly bedded, lenticular-shaped, and fi ne-grained water during low stand episodes. In association with facies. These features suggest a lateral evolution of slope deposits (C1), concave-upward conglomerate the alluvial fan to a braid plain, characterized by beds (C2) and heterolithic facies (S2) are observed; stream and sheet fl ows. these deposits are probably referable to the channelled Three sedimentary stages characterize the evolution part of the slope. of the Conglomerato di Serra del Cedro Fm: In the distal part (eastern sector), the conglomerate i) the infi lling of a structural depression. Sedimenta- facies are less thick than in the proximal one; peb- tion was controlled by strong subsidence, as suggest- bly mudstones (A2) are interbedded to fi ne grained ed by the remarkable thickness of the conglomerate prodelta facies. The delta front facies overlie well body. The architecture of the fan delta system in its stratifi ed thin beds organized in broad-shallow chan- outcropping part shows that the delta front and delta nelled bodies or lenticular convex-up coarse grained slope facies are assembled in a complex vertical and bodies (C2, C3, S2). These deposits are probably ref- lateral architecture, probably related to either reces- erable to the interdistributary bays of a delta plain. sional or progradational trends. Both fi ning and shal- - Middle unit (shelf system) lowing upward evolution of the system is indicated With a sharp contact, clay facies overlie the delta by the delta or coastal plain facies at the top of the plain deposits. These clayey sediments, whose thick- lowest unit; ness increases towards the east, contain marine fossils ii) a transgressive phase (marine fl ooding), indicated and are interpreted as shelf deposits (Argille subap- by the shelf facies overlying the delta system; pennine Fm.). iii) the activation of a terrigenous system, represented - Upper unit (alluvial plain system) by alluvial coarse facies unconformably overlying the Conglomerate facies, up to 150 m thick, unconforma- marine sediments. bly overlie the shelf sediments; they are well visible in the western sector, where they are mainly composed Facies of disorganized bodies (C1) with interbedded massive C1= disorganized conglomerates; debris fl ow. C2= clays. These facies are referable to an alluvial fan sys- lenticular bedded conglomerates; stream fl ow. C3= olume n° 4 - from P14 to P36 olume n° 4 - from V

Figure 20 - Panoramic view showing Cretaceous to Miocene deposits belonging to the San Chirico tectonic unit which overthrust the Pleistocene deposits of the Bradanic Trough: the Argille subappennine Fm. below, and the Conglomerato di Serra del Cedro Fm. above.

23 - P35

P35_R_OK 23 9-06-2004, 10:43:21 P35_R_OK 24

Volume n° 4 - from P14 to P36 P35 - P35 Leaders: P. Pieri,L.Sabato,M.Tropeano horizontal well-stratifi T linked tothegrowth oftwo eastverging anticlines(the and FPSinFigure21).Bothsynclinesaregenetically axis (the Tricarico andFrontePizzutasynclines- TS ve The two sequencesaremainlypreserved intwo east sitional) tensionalandtranstensionalfaults. structures, andareaffected byQuaternary(post-depo- Pliocene sequencesshow unconformitiesandgrowth ity (SabatoandMarino,1994)(stop3.8).Boththe tional sequencesboundedbyanangularunconform- of the Ariano Unitandiscomposedoftwo deposi- units (stop3.9).Itbelongstothrust-topbasindeposits cession liesontectonizedCretaceoustoMiocene Pliocene successioncropsout(stop3.7). The suc- In the Tricarico areaaLower PliocenetoUpper L. Sabato,S.Gallicchio, P. Pieri,M.Tropeano in the Tricarico area 3.11 The Pliocene sequencesandtectonicstructures surface, boththeshelfandtransitionalsediments. f deposits withasharpcontact;fi shelf clays(middleunit)overlie theshallow marine sandstones andtabular conglomerates; transgressive coastal plainfacies includinghorizontallylaminated Along theroadsomeoutcropsshow well-bedded, A Stop 3.6: normally graded;reworking andtraction. with interbeddedwell-sortedsandstones,reversely to C4 logic, sedimentologicandgeometricfeaturesof some tensofmetresupto150m.Sincethelitho- a variable residualthicknesswhich rangesbetween The fi also observed. structures, witheitherNW-SE orSW-NE strikes, are structure (Figure21);otherminortranstensional bounded byamajorSW-NE strikingtranstensional in Figure21). The Pliocenedepositsaresouthward scattered pebbles. A2 bated andrichinorganic materialandmarinefossils. and tractive structures. locally bioturbatedandshowing load-deformation thinly beddedsandstoneswhichalternatewithclays, or lenticulargravels, associatedtoC3andC4. to laminatedsandstones,includingscatteredpebbles acies oftheupperunitoverlap, withanerosional ricarico andFrontePizzutaanticlines– TA andFPA ppia road (km512-513),near Tricarico village r = disorganized clayscontainingcoarsesandand = thickorvery thickcross-beddedconglomerates ging asymmetricsynclineswithNW-SE trending

rst sequenceisEarlyPlioceneinageandhas

ed conglomerates;sheetfl A1 = massive clays,biotur-

nally, braidplain S1 = graded

S2 ow. = and show boringsbyLithophagaandattachedoysters ate clastsarealsopresent.Carbonateoften ceous incomposition;siliceous,graniticandcarbon- and wellroundedpebblestoboulders,mainlyarena- of thinlayersclayisrare.Clastsconsistrounded of sandstonesarevery frequent,whilsttheoccurrence and withwell-sortedsandymatrix.Lenseslayers mally ornormally-toinverse graded,clast-supported, of conglomerates,sometimeschannelledandnor- to coastalmarinefacies; itbegins withsomemetres conglomerates, sandstonesandclaystonesbelonging not-adjacent sections. The sequenceismadeupof physically connected,itisvery diffi the sequencearevery variable andtheoutcropsnot throughout thearenaceoussuccession. The facies The bioturbation,whichisvery intense,ispresent tularia, Rotalia,Cibicides,Elphidium,Lenticulina). echinoids, or fragmented(redalgae,lamellibranchs,bryozoans, The latterarerichinmacrofossils,eitherunbroken iciclastic (quartzandfeldspar)carbonatelayers. clinobeds arecharacterizedbythealternationofsil- is representedbyS-SW30°dippingclinoforms. The cross laminations. The upper partofthesedeposits and show parallel,trough-cross,orhummocky- calcarenites areorganized inupto2–m-thickbeds, bored cobblesandboulders. The hybridarenitesand conglomerates madeupofwell-rounded,Lithophaga- The sequencebegins withsomedecimetres-thick 60 mthick)whichpasstoclaystones(30thick). hybrid arenitesandsecondlybycalcarenites(about Apenninic units(stop3.9).Itisrepresentedmainlyby the depositsoffi The secondsequenceliesdisconformablyeitheron marine (prodelta-shelfdeposits)environments. The facies characteristicssuggestcoastal(deltaic)to and microfossils(foraminifersnannoplancton). layers ofgravels, containingmacro(lamellibranchs) thick beddedclaystonesandsiltywithrare Rapidly thesandstonespasstosometensofmetres and areparallel-orlow anglecross-laminated. nus ers. They bearpectinids,oysters, Vermetus, tains uptosomedecimetresthickconglomerateslay- an erosionalbaseandinverse gradation,andcon- sometimes amalgamated;normally, eachbankshows in amonotonousseriesofseveral-metres-thick banks, out forsometensofmetres. They areoftenarranged Upward thesandstonesbecameprevalent, andcrop of soft-sedimentdeformationstructures(loadcasts).

are alsovisible. Very frequentistheoccurrence Balanus Balanus ; scatteredpectinids,oysters and

), andbenthicforaminifers(Tex- rst sequence(stop3.8)oronolder

cult tocorrelate 9-06-2004, 10:43:23 Ditrupa Bala-

PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35

analysis allows us to refer this part of the sequence to the NW. The western limb of the asymmetric and high-energy shallow-marine environments. east-verging Fronte Pizzuta syncline may also be observed; it is represented by sands and conglomer- Stop 3.7: ates. The out of sequence thrust (Figure 21), which Panoramic view from the Saracen tower in superimposed the San Chirico tectonic unit on the Tricarico village Pleistocene deposits of the Bradanic Trough (Argille The Saracen tower is located on the eastern limb of subappennine and Conglomerato di Serra del Cedro the Tricarico syncline. Looking east, in front of you, Fms.), crops out in the middle of the hill. you can observe several main structures of the more Moving to the north (on the left) we can observe the external part of the frontal imbricate Apennines fan. upper part of the second succession, characterized by The core of the Fronte Pizzuta anticline, represented the occurrence of up to 1-2 m thick sets of clinoforms, by the lower part of the succession of the San Chirico which are often separated from each other by ero- tectonic unit, crops out; the fold plunges towards sional surfaces. Each set of clinoforms shows either olume n° 4 - from P14 to P36 olume n° 4 - from V

Figure 21 - Schematic geological map of the Tricarico area; VBTU: Vaglio di Basilicata tectonic unit; SCTU: San Chirico tectonic unit; MTC: Marne argillose del Toppo Capuana Formation; PAA: Serra Palazzo Formation; Pls: Pliocene sandstones; Plag: Pliocene clays; Plcg-s: Pliocene conglomerates and sandstones.

25 - P35

P35_R_OK 25 9-06-2004, 10:43:24 P35_R_OK 26

Volume n° 4 - from P14 to P36 P35 - P35 Leaders: P. Pieri,L.Sabato,M.Tropeano ping intheneighbourhoodofIrsinavillage,anarea In themorningwewillvisitdepositsoutcrop- deposits”. and sedimentaryfeaturesofthe“Regressive coastal cated totheobservation ofthedifferent geometries The fourthdayoftheexcursion (Figure9)isdedi- (low tomedium diffi towards NE. N whiletheonlappingPliocenesequencedips20° unconformity. The Miocenedepositsdip35°towards on theMioceneSerraPalazzo Fm.throughanangular In Tricarico village, thesecondPliocenesequencelies Pliocene succession Relationship betweenthesubstratumand Stop 3.9: depositional tectonics the secondsequence,demonstratingPliocenesyn- structure (aprogressive unconformity?)characterizes lag depositduringatrangression.Locally, agrowth Lythophaga-bored pebblestocobbles,representinga centimetres thickconglomerateswithwell–rounded, The overlying hybridarenitesshow atthebasesome NE) sandstonebankswiththinconglomeratelayers. fi the fi At Tricarico village,thesecondsequenceoverlies Relationships betweenthetwo Pliocenesequences Stop 3.8: their sedimentation. structures whichaffected thedepositsduringandafter the outcropwecanalsoobserve diverse tectonic type passestothesecondoneinsameset. Along an angularoratangentialbase;sometimesthefi rst sequenceisrepresentedbysubvertical (upto80° rst onethroughanangularunconformity. The Figure 22-Depositionalscheme ofthe“Regressive coastaldeposits”outcroppingintheIrsinaarea. culties) . DAY 4 DAY 4 rst the Miglionicoarea(stops4.6and4.7). deposit welloutcroppinginGrassanovillageand In theafternoonwewillvisitRegressive coastal transitionally orerosionally. hemipelagites ofthe Argille subappennineFm.either Trough (stops4.1-4.5).Here,thedepositsoverlie the located inthecentral-westernsectorofBradanic Fm., fromoffshore environments ( upward trendcharacterizes the Argille subappennine from NWtoSEand W toE. A shallowing Pliocene toMiddlePleistocene)becomesyounger it isuptoafew hundredsofmetres,andtheage(Late wards theNE;croppingthicknessisvariable, but nalic arrangement,withadipoffew degrees to- out extensively eitherinsubhorizontalormonocli- The latterisrepresentedbyhemipelagitescropping on the Argille subappennineFm.(Figs.5,6,22,26). part oftheBradanic Trough in-fi The Regressive coastaldepositsrepresenttheupper L. Sabato,P. Pieri,M.Tropeano the Bradanic Trough 3.12 The Regressive coastaldepositsof 2002). al. ronments (MassariandParea, 1988;1990;Pieri facies belongto paralic,deltaicand/oralluvialenvi- vary fromafew metresuptoover 100metres,and origin (Miglionicoexample, stop4.7). Thicknesses examples, stops4.1-4.4,4.6),secondlycontinentalin mainly shallow-marine inorigin(IrsinaandGrassano represent thetopofforedeepsuccessionsandare (Figs. 22,26). These coarse-grained coastaldeposits tionally (stops4.1,4.6,4.7)orerosionally(stop4.3) lagites ofthe Argille subappennineFm.eithertransi- The Regressive coastaldepositsoverlie thehemipe- shoreface environments ( 1996) passingupward toshallow shelfandtolower , 1994a;1996a;Sabato,1996b;LazzariandPieri, Modifi i.e. Sabato,1996b). ed fromSabato(1996a). ll successionandlie i.e. Ciaranfi 21-06-2004, 9:46:42

et al et ., PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35

The highest and oldest Regressive coastal deposits offshore-transition environments. The middle portion are Sicilian in age and prograde towards the E-NE of the sequences, 25-30 m in thickness, is formed by (Pieri et al., 1994a; 1996a) whilst the younger Mid- parallel- swaley- and ripple-laminated fi ne-grained dle and Upper Pleistocene deposits prograde either to sandstones commonly displaying hummocky-cross the N (towards the central Adriatic coast), to the E bedding, and characterized by the occurrence of fre- (towards the Manfredonia Gulf) or to the SE (towards quent erosional surfaces draped by thin layers consist- the Taranto Gulf) (Tropeano et al., 2002b) (Figure ing of unbroken or fragmented fossils (lamellibranchs, 6). These deposits are mainly siliciclastic in origin gastropods, oysters, Ditrupa) and discontinuous clays and of Apenninic provenance, but locally, near the and marls intensely bioturbated (echinoids), and often foreland highs, they may be carbonate or mixed in subjected to fragmentation into mud clasts and clay origin. According to Pieri et al. (1996a), these coarse- chips. This portion of the sequences can be related grained deposits are arranged into prograding wedges, to lower shoreface environments. The upper portion often characterized by wave-dominated Gilbert-type of the sequences, up to 15 m thick, is characterized bodies, whose top depositional surface progressively by remarkable variability in the lithologic features. falls in elevation along the progradation dip. The It can be represented either by conglomerates with erosionally based wedges, commonly characterized sandstones interlayered (stop 4.1), or by sandstones by gravelly delta deposits (i.e. Massari and Parea, deposits with rare conglomerates layers (stop 4.2). 1990; Sabato, 1996b), alternate with transitionally based ones, characterized mainly by aggrading de- The southern zone posits which from bottom to top pass from offshore- In the southern zone of the Irsina area a mainly con- transition facies of the Argille subappennine Fm. up glomerate erosionally-based body outcrops (Figure to shoreface, beach and, in some places, to alluvial 23). It is represented by a wave-dominated Gilbert- facies (Sabato, 1996b). type delta in which bottomset, foreset and topset are distinguished. The foreset unit mainly consists 3.13 The Pleistocene Regressive coastal of clinostratifi ed conglomerates with sandy interlay- deposits in Irsina village ers (stop 4.4). The thickness ranges between some L.Sabato metres in the proximal area, where the sequence is In the Irsina area we have the opportunity to compare incomplete because of lack of bottomset beds, and 40 the different types of relationships with the Argille m in the distal one, where sandy interlayers increase, subappennine Fm. that the Regressive coastal depos- and bottomset beds gradually appear. Furthermore, its offer (Figure 22). In fact, in the northern zone, in the proximal area the foreset beds lie at a high sandy and sandy-conglomeratic offshore-transition to angle (up to 30°) over the underlying unconformity foreshore sequences form transitionally based wedg- surface (Argille subappennine Fm.), while distally es, whilst in the southern zone, conglomerate deltaic they become tangential. Foreset beds occur often ar- sequences erosively overlie the underlying Argille ranged into groups of beds with different dipping, subappennine Fm. (Sabato, 1996b). Both examples separated by erosional surfaces. Foreset beds are are represented by a group of sandy-conglomeratic sigmoidal-shaped, some decimetres thick, reverse or deposits, 60 m in thickness, having lithostratigraphic reverse-normal graded. They are mainly clast-sup- and facies characteristics laterally and vertically vari- ported, with sandy-matrix; locally, matrix-supported able. Internally, this group of sediments shows a pro- beds are present. The rare interlayered sands are lami- gradational geometry, with NW-SE trending, low-and nated and contain gravel layers. Clasts (up to 30 cm

high angle foreset beds. in size) are well rounded and often the smaller ones P14 to P36 olume n° 4 - from show imbrication indicating paleofl ows from N-NW. The northern zone Upwards, 1-m-high, channelled, sandy-conglomerate V The base of the offshore-transition to foreshore se- bodies occur. Bottomset beds are mainly represented quences, some metres in thickness, is composed of by sandy layers bearing microfossils (foraminifers). thinly-stratifi ed, intensely-bioturbated, and parallel The topset unit has a maximum thickness of 10 m; laminated clays and silty clays; erosive-based sand- it lies with an erosional contact on the foreset beds stones, parallel- and planar-cross laminated, are in- (Figure 24) (oblique geometry) in the proximal area terlayered. Macro and microfossils and plant remains and gradually passes into the foreset unit in the distal are abundant. This portion of the sequences represents one (sigmoid geometry). Topset beds are made up of

27 - P35

P35_R_OK 27 9-06-2004, 10:43:29 P35_R_OK 28

Volume n° 4 - from P14 to P36 P35 - P35 Leaders: P. Pieri,L.Sabato,M.Tropeano to 15cm;they are wellroundedandthesmallerare sand. Clastsizesrangebetweensomecentimetresup f are clast-supported,andsomelayersshow openwork decimetres thickandoftencoarser-graded beds;they are dominatedbyconglomeratesorganized intosome layers dip10°.Upward, thesequences(beachface) dipping planarcross-lamination;theconglomerate couplets; thesandstonesshow onshoreandoffshore sequences wecanobserve sandstone/conglomerate Here, inthelower part(uppershoreface) ofthe the Irsinaarea. fo Upper portionoftheoffshore-transition to Stop 4.1: indicate paleofl crusts. The imbricated clasts,upto10cminsize, matrix, andorganic-rich layersandmanganesifer trix-supported conglomerates,withabundant clayey stratifi alluvial environments andarerepresentedbycrudely palustrine). The betterexposed facies arerelatedto deposit showing different facies (lagoonal,alluvial, f deposit unconformablyliesthroughanerosionalsur- deltaic sequences,areddishsandy-conglomeratic Either ontheoffshore-transition toforeshoreoron well-developed seaward imbrication. are smallerthanthoseoftheforesetunitandshow a conglomerates withfrequentsandyinterlayers;clasts Fi abric; thematrixisrepresentedbywellsortedcoarse ace (Figure25).Itisanupto10mthickcontinental re gure 23-Sandy-conglomeraticdeltaicdepositserosively overlie theclaydepositsof Argille subappennineFormation. shore sequences inthenorthern zoneof

ed, sometimeslow-angle clinostratifi

ow s fromN.

ed, ma- and carbonate. are frequent.Clastscompositionismostlyarenitic dipping imbrication. Attached orscatteredoysters mostly disc-shaped,andshow adominantseaward Ditrupa hummocky-cross bedding.Scatteredoralongsurfaces cm upto10insize.Frequentistheoccurrenceof lens-shaped conglomeratesarefound;clasts2-3 show planar-cross-laminations. Upwards, layersor coarse grained,well-sorted,bioturbatedandrarely sandstones occurin1-2mthickbeds,aremedium- are indicative ofuppershorefaces environments. The quences arerepresentedbysandstoneswhosefacies Here, thedepositsofupperportionse- the Irsinaarea. To The baseofthedelta. Stop 4.3: w ates beds,inversely graded,withwelldeveloped sea- foreshore facies withsomemetresthickconglomer- found. The sequencesaresometimesrepresentedby fo Upper portionoftheoffshore-transition to Stop 4.2: (Figure 23) the hemipelagitesof Argille subappennineFm. Gilbert-type deltasequenceserosionallyoverlying ard imbrication,andwithinterlayeredsandstones. re

the southofIrsinavillage,wecanobserve the shore sequences inthenorthern zoneof , lamellibranchs,gastropodsandoysters are 9-06-2004, 10:43:31 PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35

Stop 4.4: The sequences begin with about 15-m-thick, fi ne and Conglomerates of the Gilbert-type delta sequences well-sorted sandstones arranged into some decime- in the southern zone of the Irsina area. tres-thick bioturbated (echinoids) packages which al- Here, it is possible to observe the conglomerates ternate with low-angle, cross- and parallel laminated topset unit erosively overlying the conglomerates sandstones beds; lamination is often underlined by foreset beds (Figure 24) fragmented silty layers. Seldom thin conglomerates

Figure 24 - Oblique geometry of the foreset beds at their upper boundary. Irsina village.

layers and hummocky-cross stratifi cation occur; Stop 4.5: high-angle cross-lamination is also observable. At Continental deposits erosionally overlying the Re- different heights some lenses of laterally continuous gressive coastal deposits in Irsina village. claystones are visible. This portion of the sequences Here, the continental deposits, erosively overlying the can be related to offshore-transition to lower shore- Gilbert-type delta sequence, outcrop on the foreset face environments. beds, for a thickness of about 6 m (Figure 25). The sequences follow for about 10 m with sandstones, generally medium-coarse grained and bioturbated, P14 to P36 olume n° 4 - from

3.14 Regressive coastal deposits in Grassano area showing longshore-directed (N-S) trough-cross bed- V L. Sabato M. Tropeano ded sandstones and pebbly sandstones, grouped In the afternoon we will arrive at Grassano village, in sets of about 10-20 cm thick. Upwards, wedge- where at Cinti, the good exposure of a vertical section shaped conglomerates alternate with wedge-shaped allows Regressive coastal deposits to be investigated. sandstones; both wedge out seawards and are offshore Here, the regressive succession is formed by 30-35- dipping (5°-6°); planar cross-stratifi cation occur in m-thick sandstones and sandy-conglomerates off- sandy wedges. Conglomerate wedges sometimes shore- transition to deltaic sequences, transitionally pass distally to sandstone ones. This portion of the se- lying on the Argille subappennine Fm. (Figure 26). quences can be referable to lower shoreface-transition

29 - P35

P35_R_OK 29 9-06-2004, 10:43:32 P35_R_OK 30

Volume n° 4 - from P14 to P36 P35 - P35 Leaders: P. Pieri,L.Sabato,M.Tropeano o eter of7-8cm;frequentistheoccurrenceattached and subangularsiliceousclastswithanaverage diam- well-rounded arenitic,granitoidandcarbonateclasts from somecmupto60cm. The foresetbedsshow grain-size (mainlywheretheforesetsheightisless), it ispossibletoobserve adownslope increaseinclast scarce, coarse-grainedsandymatrix;inmany cases beds areclast-supportedandnormallygraded,with tion dippingonshore.Commonlythecoarse-grained The sandyforesetsdisplayahighanglecross-lamina- sandy beds,whichdisappearupwards (Figure27). more, they alternatewithafew-decimetres-thick or tangentialbaseanddisplayawedge-shape;further- some decimetresupto1mthick,have anangularand/ decrease basinward from17°to5°.Foreset bedsare w and itsthicknessdecreasesfrom5mto2.5basin- and atopsetone. The foresetunithasawedge-shape and internallyitispossibletodistinguishaforesetunit the previous deposit.Ithasathicknessofabout6m, w Through anerosionalandvery gentlyinclinedsea- to offshore environments. w nitic clastsarealsodisc-shapedandshow dippingsea- ysters, mainlyatthebaseofforesetunit. The are- ards. The northeast-dipping coarse-grainedforesets ards surface, amainlyconglomeraticbodylieson ard andlandward imbrications.Someforesetbeds Fi gure 25- Alluvial depositserosively overlie theGilbert-type deltasequenceinIrsinaarea. ove as themoreclearlyobservable continental deposits not wellvisiblehere,they have thesamesignifi its, matrix-supportedandalluvialinorigin. Though Finally, thesuccessioniscappedbyfi lower shoreface-transition tooffshore deposits. alluvial one.Distallythedeltagradesintosandstones fl etry, suggestingaseriesofhigh-frequency sealevel the upperboundaryacomplex oblique/sigmoidgeom- diameter of3-4cm. The topset unitisformedfi by adropintheclastsize,whichhave anaverage ing aneastward paleofl are very wellsorted,withdisc-shapedpebblesshow- fl part ofthesuccessioncanbeinterpretedasawave-in- conglomerate liesontheunderlyingtopsetunit. This imbrication. An upto2-m-thickmatrix-supported (average diameterof6-7cm)show aseaward dipping better sortedconglomerates;thedisc-shapedpebbles towards theNE. The following 2marecomposedof sand, andtheclastimbricationindicatesapaleofl gle crosslamination;thematrixiscomposedofcoarse cm-thick horizontalbedsshowing aseaward low-an- by 1.4-m-thickconglomeratesarrangedintoabout20- f

ace andbeachface environments andfi uctuations. The foreset/topset boundaryisevidenced uenced Gilbert-typedeltapassingupward toshore- rlying theRegressive coastaldepositsin theIrsina

ow . The foresetbeds show at

ne-gravel depos-

nally toan 9-06-2004, 10:43:34

cance

rstly

ow ow PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35

Figure 26 - Depositional scheme of the “Regressive coastal deposits” outcropping in the Grassano area. From Tropeano et al., 2002.

continental one. Such deposits can be seen along the road from Grassano to Miglionico. The road cuts into deltaic conglomerates passing to lagoonal-palustrine clays (50-60 m in all).

In the evening, we will travel towards east, crossing well developed badlands (called “calanchi”). DAY 5 (low to middle diffi culties)

During the fi fth day we will visit the northern (in the morning, stops 5.1-5.4) and the southern (in the after- noon, stops 5.5 and 5.6) part of the Sant’Arcangelo piggyback Basin (Figure 28). It will be possible to discuss tectonics and sedimenta- tion relationships in a piggyback context. Particular attention will be turned to the progressive unconform- ities characterizing the piggyback sequences and to Figure 27 - Detail of the conglomerate foresets of the the description of lacustrine deposits that developed Regressive coastal deposits outcropping at Cinti, in a tectonically controlled sub-basin. Furthermore, near Grassano. the relationships between the substratum and the in- fi ll deposits of the basin will be observed. area, which we observed during stop 4.5. 3.14 The wide Sant’Arcangelo Basin P14 to P36 olume n° 4 - from Stop 4.6:

P. Pieri, L. Sabato V Regressive coastal deposits at Cinti, near Grassano The Pliocene to Pleistocene Sant’Arcangelo Basin village (Figure 29) is a satellite basin, located back to the front of the south-Apennines thrust belt. The Stop 4.7: Sant’Arcangelo Basin in-fi ll, up to 5 km in thickness Transitionel fecies pessing upward to continental (Mostardini and Merlini, 1986; Merlini and Cippitelli, ones. 2001), is basically marine in origin, although in the In other areas, the “Regressive coastal deposits” are upper part of the succession Lower and Middle Pleis- made up of transitional facies passing upward to a tocene continental deposits occur (Vezzani, 1967;

31 - P35

P35_R_OK 31 9-06-2004, 10:43:37 P35_R_OK 32

Volume n° 4 - from P14 to P36 P35 - P35 Leaders: P. Pieri,L.Sabato,M.Tropeano ridge (ridge2inFigure29B),leadingtothephysical Apulian unitscausedthecompleteemergence ofa 29C). DuringtheMiddlePleistocene,thrustingin and Sani,2000;Patacca andScandone,2001)(Figure (Roure previously hadbeenoverthrust bythelarge sheet transpression thatoccurredinthe Apulian unitswhich stage). The upliftwas causedbythrustingand the thrustfrontbegan touplift(closedpiggyback stage), whilecontinentaldepositsaccumulatedwhen the PlioceneandEarlyPleistocene(openpiggyback accumulated ontoalarge moving thrustsheetduring According toPieri passively folded,byPatacca andScandone(2001). - partofthethrust-topbasinsuccessionwhichwas Merlini andCippitelli(2001); sion ormantlebulging atthefrontofchain,by - adepressionassociatedwithbasicmagmaticintru- - apull-apartbasin,by Turco (1994); - apiggybackbasin,byCaldara The Sant’ArcangeloBasinwas interpretedas: Caldara et al . (1988),Roure et al. et al. , 1988). , 1991;Hippolyte et al. et al

. (1991),Hippolyte (1996b), marinedeposits et al et al et al. F . (1990); igure 28-Field tripitineraryofthefi . (1988),Casero , 1994;Bonini et al .

fl of deltaictoshelfsystemsintheeasternsectorand ferent andadjacentsectorsofthebasinconsists systems; thethirdsequencedeveloped intwo dif- sequences aremainlycomposedofdeltaictoshelf of whichareprogressive inorigin. The lower two Each sequenceisboundedbyunconformities,some sediments. ove Lorenzo Cycle);thefourthsequenceunconformably f according tostructuraldata,normalandtranscurrent the endofdepositionwithinbasin.Present-day, deep separation oftheSant’ArcangeloBasinfromfore- depositional sequences( iciclastic, UpperPliocenetoMiddlePleistocene, The Sant’ArcangeloBasinin-fi et al. while thrustfaults stillaffect thechainfront(Doglioni structures (Caldara mentation assuggestedbythepresenceofgrowing oriented foldsandfaults thatwereactive duringsedi- These sequencesweremainlyaffected by NW-SE

aults occurinthebasinarea(Pieri uvio-lacustrine systemsinthewesternsector(San rlies theolderonesandiscomposedofalluvial , 1996)(Figure29C). s.s . (theBradanic Trough, Figs.29B,29C)and

fth day. et al. A , 1988;Pieri - D

in: Pieri

ll containsfoursil- et al. et al. et al. , 1997b), , 1996b). , 1994b; 9-06-2004, 10:43:39

PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35

Figure 29 - (A) Schematic structural sketch of southern Italy; (B) location of the Sant’Arcangelo Basin and its main structural and stratigraphic elements; (C) schematic cross-section through the area from SW to NE. Modifi ed from Sabato (2000).

Vitale, 1996; Zavala, 2000) and by paleogeographic 1000 m thick and prograding north-eastwards. change through time. Sequence C lies unconformably on sequence A and The fi rst sequence (A; Caliandro Cycle in Pieri et through a syntectonic unconformity on sequence al., 1994b) was deposited during the Late Pliocene. B. The development of the sequence C had been This sequence lies unconformably on the deformed controlled by the growth of a fault propagation fold pre-Pliocene units and is made up of conglomerates, (the Alianello anticline, Figure 30), NW-SE trend- sandstones, and marly claystones representing a com- ing, which divided the basin into two parts during plete sedimentary marine cycle with transgressive the Early Pleistocene (Pieri et al., 1996b). In the and regressive deposits. It has a wedge-shape with eastern part, which maintained a connection with the maximum thickness (1000 m) towards the west, in the Bradanic Trough conserving the characteristics of an proximal area. The dip angle of beds progressively open piggyback basin, marine sedimentation carried P14 to P36 olume n° 4 - from decreases from the lower part of the sequence (75°) to on until the Middle Pleistocene (Sauro Cycle in Pieri V the upper part (35°). Its sedimentologic features sug- et al., 1994b, Figs. 29B, 30), and a fan delta system, gest that the basin can be recognized in this stage as prograding east-southeastwards, was deposited. This an open piggyback (Pieri et al., 1996b). sequence is composed of silty claystones, sandstones Sequence B (Agri Cycle in Pieri et al., 1994b) lies and conglomerates, up to 1300 m thick. On the con- on sequence A with a syntectonic unconformity; it trary, the western part was separated from the sea and developed in the Late Pliocene-Early Pleistocene and assumed the characteristics of a closed piggyback is composed of silty claystones, sandstones, and con- basin; here continental sediments, composed of 500 glomerates, forming a marine fan delta system up to m thick silty claystones and conglomerates deposited

33 - P35

P35_R_OK 33 9-06-2004, 10:43:41 P35_R_OK 34

Volume n° 4 - from P14 to P36 P35 - P35 Leaders: P. Pieri,L.Sabato,M.Tropeano (San LorenzoCycleinPieri glomerati diSerraCornetainPieri The fourthsequence(sequence defi this laststagecantheentireSant’ArcangeloBasinbe Pieri to Pleistocene. According in whichsedimentationcontinuedfortheentire isolation ofthebasinfromrestforedeep, (ridge 2inFigure29B)whichcausedthephysical was broughtabout bytheemergence ofanouterthrust represents thelastevolutionary stageofthebasinand interpreted asalluvialfan deposits. This sequence stones andconglomeratesabout150mthickis the previous sequences;itismadeupofsiltysand- and MiddlePleistoceneinage,liesunconformablyon continental inorigin(Vezzani, 1967;Loiacono,1983) Alianello anticline). two sectorsasaresultofthegrowth ofarampfold (the the EarlyPleistocene,ofSant’ArcangeloBasininto Figure 30-Block diagramshowing thedissection,in ned asaclosedpiggyback basin. et al. et al. , 1994b). D ; SabbieeCon- (1996b),onlyin et al.

, 1994b), the depositsofbothsequences unconformity. Notethedecreasing ofthedippingin sequence Cycle). Onthelatter, thealluvialconglomeratesof the deltaicsandstonesbelongingtosequence B the sandstoneandconglomeratedepositsofsequence (Figure 30).Furthermore,lookingtowards thewest, west (SanLorenzoCycle)ofthe Alianello anticline of sequence ferent stratigraphicdevelopments andarrangements From thispanoramicview youcanmake outthedif- Stratigraphic andstructuralfeatures ofsequenceC Stop 5.2: (sequence the conglomeratesbelongingtoSanLorenzocycle Along theleftsideofSaurovalley, wecanobserve and sequenceC(Sauro and SanLorenzo cycles) The relationship betweensequence B(AgriCycle) Stop 5.1: L. Sabato,P. Pieri 3.15 The northernpartofthe Sant’Arcangelo Basin canbeobserved. C C (SauroCycle)overlie withasyntectonic ) faulted byanormal fault, incontactwith C totheeast(SauroCycle)and B and C . 21-06-2004, 9:48:50 B (Agri PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35

Figure 31 - The two measured lithostratigraphic logs within the lacustrine unit of the San Lorenzo Cycle in the Sant’Arcangelo Basin: log a was measured in the depocentral area, log b in a marginal area (3,5 km to the NW of log Volume n° 4 - from P14 to P36 n° 4 - from Volume a). The three recognized magnetic polarity intervals and the palynological spectra are shown. 3.16 Lacustrine deposits of sequence C ally composed of thinly bedded claystones and silty (San Lorenzo Cycle) claystones, interbedded with sandstones, calcareous L. Sabato, A. Albianelli, A. Bertini, F. Masini, M. and volcanoclastic interlayers. To the west it is pos- Moretti, G. Napoleone, P. Pieri, M. Tropeano, C. sible to observe sandstones and conglomerates that Lombardi are interlayered with claystones. Measurements of The lacustrine deposits are variable in thickness, paleocurrents indicate major paleofl ow direction with a maximum of over 200 metres, and are gener- towards the SE; transverse paleocurrent directions

35 - P35

P35_R_OK 35 21-06-2004, 9:48:54 P35_R_OK 36

Volume n° 4 - from P14 to P36 P35 - P35 Leaders: P. Pieri,L.Sabato,M.Tropeano Ephedra are characterizedbytheoccurrenceof phases containPoaceaeandChenopodiaceae, ure 31,Sabato to 47moflog steppe-dominated phasesandforesttaxafrom20m Palynological dataindividuated alternationsbetween lacustrine successionisEarlytoMiddlePleistocene. this Mammal Age. Therefore, theobtainedagefor the restricts theageofassemblagetolatestpart - brecciensis, (Figure 31,log 1992), obtainedbyK-Arradiometricmeasurements indicate anageof1.1 in composition,fromtheupperpartofsuccession, been measured. The volcanoclastic layers,phonolitic along thewesternsidetowards theeasthave also lie onasmallanticlinethatdeveloped withinthelower alluvialdeposits,belongingtothesameCsequence. Figure 32-Field view, alongthe Agri valley, ofsequenceC(theSanLorenzoCycle).Thelacustrinedeposits(ontheleft) arvalidens, Microtus 31, log some faunal elements suchas fauna totheBiharian Mammal Age; thepresenceof mammals of assemblage) was found. The occurrenceamongsmall dium sizeddeerandafairly diversifi fauna (rarereptiles,amphibians,rareremainsofame- part oflog sedimentation rate. The uppernormalpolarity(upper m inthickness,thesetimelimitssuggestaquitehigh the Brunhes(0–0.78Ma).Inaprofi Jaramillo chron(0.99–1.07Ma),andtheupperone tozone. The basalnormalpolarityisthereforethe the latestMatuyamachronassignedtothismagne- volcanoclastites, whoserangeof confi stratigraphy. The reversed polaritycontainsthedated detailed magneticmeasurementsofreversed polarity netic polarityintervals arealsoshown, asaresultof marginal partofthelacustrinedeposits)threemag- a ; scarcefi inthecentralpart,andlog b ) includesthelayersinwhichavertebrate Mimomys and et al., a a andtheupperpartoflog nds ofdeciduoustreepollencon- ). Inthesyntheticcolumns(Figure Macroneomys ( Iberomys in pressb).Steppe-dominated

± savini 0.3Ma(Caggianelli allows ustoreferthe ) Microtus

ex gr ex cf. ed smallmammal b le ofupto200 brachygnathus dence confi inthenorthern . huescarensis Artemisia ( Terricola b (Fig- et al rms and

) ,

In contrast,theforestfl tribute toattribution ofconditionstoanaridclimate. and trees, mainly (Moretti andSabato, dykes). The analysescarriedoutonthesestructures large vertical water escapestructuresandneptunian variability (deformedlamination,load-structures, mation structures. They show awidemorphological succession istheoccurrenceofsoft-sedimentdefor- are found. A very distinctive featureofthislacustrine ( eae oogonia),freshwater ostracodsandgastropods Along theentiresuccessioncharophytes (Charac- tocene glacial/interglacial phases. which arecorrelatablewiththeEarlytoMiddlePleis- arboreal pollenassemblages)andclimaticchanges plete therecordofvegetational (herbaceousvs. from themiddletoupperpartofsuccessioncom- humid climate.Palynological analyses,inprogress, ronment (Sabato,1997;2000). environment intotheoverlying distallacustrineenvi- of afan delta,at thetransitionofaproximallacustrine in theproximalareaareinterpretedasdistalpart enous-dominated freshwater lake; thefacies observed that they weredepositedinadistalzoneofterrig- Facies analysisofthedepocentersedimentsindicates lope dippingtowards theaxisofsyncline. deformation. Slumpsprovide evidence ofapaleos- during compaction)andwithdifferent mechanismsof at different times(duringoraftersedimentation,and From thisviewpoint, thelacustrinedepositsbelong- San Lorenzo Cycle The fl Stop 5.3: Planorbis Zelkova uvio-lacustrine depositsofthe sp.),aswellplantandvertebrate remains , whicharetaxaofawarm andrelatively Quercus in prep. followed by ora isdominatedbydeciduous ) show thatthey occur Carpinus, Ulmus 21-06-2004, 9:48:59 PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35

ing to the San Lorenzo Cycle (sequence C), can be conformably covered by Lower-Middle Miocene observed lying on the alluvial deposits, which belong pre-fl ysch deposits (Bifurto Formation); (2) Jurassic to the same sequence (Figure 32). In the distance, to Oligocene polydeformed ophiolitic units (Ligurian it is possible to make out the alluvial conglomerate units, Bonardi et al., 1988b; see also Knott, 1987, unit which overlaps the lacustrine deposits and closes Mauro and Schiattarella, 1988; Monaco and Tortorici, sequence C. The lower unit forms a small anticline, 1995), unconformably covered by syntectonic de- and has a thickness of about 150 m; it is composed posits, Early Miocene in age (Albidona Formation); of poorly-sorted and well-stratifi ed conglomerates, (3) Lower Pleistocene satellite basin clastic deposits which locally contain decimetre thick clayey beds (Caldara et al., 1988; Pieri et al., 1994b), correspond- and massive sandstone layers. The lacustrine deposits ing to the upper part of the thick Sant’Arcangelo suc- onlap onto the fl ank of the fold, showing a progressive cession, covered by mid-Pleistocene alluvial deposits unconformity; this, together with other sedimentary with reddish matrix (Sabbie e Conglomerati di Serra features, confi rms its sedimentation during the Al- Corneta Fm.). ianello anticline’s growth Stop 5.5: Stop 5.4: Contact zone between bedrock and Unconformity between the substratum basin succession and sequence A In this stop the tectonic setting of the entire area can Along the Agri valley we can observe conglomerates be observed. Along the frontal part of the northern and sandstones, belonging to sequence A, which dip sector of Pollino Ridge, Meso-Cenozoic limestones about 50°-55° towards E-NE. They unconformably are thrust onto the Bifurto Formation. A comparison overlie the deformed Miocene Gorgoglione Flysch, between the attitude of the NW-dipping carbonates in which dips about 70° towards NE. the northern sector and the attitude of the NE-dipping limestones outcropping in the central area suggests 3.17 The southern border of the that the frontal thrust developed by anticlockwise Sant’Arcangelo Basin rotation of blocks bordered by left-lateral strike-slip M. Schiattarella N120° trending faults and right-lateral strike-slip N-S The southern border of the Sant’Arcangelo Basin is trending faults, since the basic orientation of the ridge located to the north of the Pollino Massif, a mountain- is NW-SE. Owing to the transversal streams cutting ous area with elevations up to 2200 m a.s.l. represent- the hanging wall, it has been possible to estimate a ing the junction between the southern Apennines and thrust motion of at least 1.5 km (Schiattarella, 1996; the Calabrian arc and which is constituted by Meso- 1998). However, it is likely that the moderate thrust- Cenozoic platform carbonates overthrust by Ligurian ing due to block rotation re-activated an inherited (i.e. internal ophiolite-bearing) units. The carbonate out-of-sequence thrust related to the earlier Pliocene ridge is sharply interrupted toward the NW by the contractional tectonics. The propagation of a deeper Mercure River structural depression, a lacustrine ba- thrust under the Pollino structure may be responsible sin fi lled by mid-Pleistocene sediments (Schiattarella for the growth strata and general architecture of the et al., 1994). southern zone of the Sant’Arcangelo Basin. As a The average trend of the carbonate Pollino Ridge matter of fact, growth structure expanding towards axis is about N120°, corresponding to the strike of the NE in the southern fl ank of the basin and NW-SE the main transcurrent and normal faults. The ridge is trending transpressional structures have both been

in fact bordered by Plio-Pleistocene strike-slip faults observed in the Plio-Pleistocene clastics. P14 to P36 olume n° 4 - from re-activated as normal faults starting from Middle In this site we can also observe the contact zone be- Pleistocene times (Schiattarella, 1998). tween Pleistocene clastics and the pre-Pliocene bed- V In a schematic cross-section from SW to NE (i.e. from rock. Conglomerate and sand beds are visibly tilted the bottom to the top of the tectonic stack), the follow- and affected by eye-catching faults. The panorama ing units can be observed: (1) a carbonate platform also allows us to view both the growth structures in unit (Alburno-Cervati-Pollino Unit, corresponding the Sant’Arcangelo Basin strata and its Quaternary to the back-reef bulk of the Campania-Lucania plat- stratigraphic setting. form), the age of which ranges from Late Triassic to Early Miocene (D’Argenio et al., 1975), para- 3.18 The southern part of the Sant’Arcangelo Basin

37 - P35

P35_R_OK 37 9-06-2004, 10:43:53 P35_R_OK 38

Volume n° 4 - from P14 to P36 P35 - P35 Leaders: P. Pieri,L.Sabato,M.Tropeano which, throughasharpcontact(marinefl composed ofanupto900-m-thickpeliticsuccession Pliocene substratumatthesoutheasternmargin; itis (Upper Pliocene),unconformablyliesonthepre- The lower unit,theMonteCotugnoSupersynthem The MonteCotugnoSupersynthem Serrapotamo). bounded, supersynthems(MonteCotugno,Sinniand and hasbeensubdivided intothree,unconformity and Serrapotamorivers), isupto2500mthick, the Sinnivalley anditsmaintributaries (Sarmento southern partoftheSant’ArcangeloBasin,along The stratigraphicsuccessionoutcroppinginthe F. Synthem. F The following unit,theSinniSupersynthem, iscom- The SinniSupersynthem higher order). be identifi small-scale cyclicity, probablyofeustasticorigin,can supply increasedintheplain. Thus, inthisunit,a of eustaticorigin,whichoccurredbeforethesandy upper part,two small-scale T-R pulses,probably alluvial ordeltaicinorigin. This unitshows, inthe ov igure 33-SandstonelobesinthedeltafrontofSenise Loiacono erlies a-few-metres-thick, coarse-graineddeposits,

ed (inthecontext ofaregressive phaseofa

ooding) thick, interbeddedtothickfi composed ofseveral sandstonebodies,10to100m i) theS.Giorgio delta system,about450mthick,is (Figure 33),organized intotwo mainsystems: m-thick successionofmarinedeltasandstonebodies The SeniseSynthemisrepresentedbyanupto1000- ent regime. tems, feddeltaicmarinesystemsinastronglysubsid- transversal supply, duetovery active alluvialsys- roughly N-Selongatedtopbasin.Longitudinaland migration ofthe Apenninic frontalthrustformeda mobility ofthesouthernandeasternmargins. The the basinevolution linked totheuprisingand and )whichcorrelatetoimportantstagesin posed oftwo alluvialanddeltaicsynthems( The NoepoliSynthem,upto400mthick,corresponds center. source) aswellaN-Selongatedsubsidingdepo- reveals westernprovenance (linearandtransverse alluvial conglomeratesfacies. Itsstackingpattern posed ofdeltafrontsandstonelobeswithoverlying ii) theRoccanova system,upto350mthick,iscom- to EarlyPleistoceneeustaticoscillations; related tostructuralbarriersinthesourceareasand/or east. The causes ofthecyclicity maymostlikely be supply. This systemhadapointsourcefromthesouth- origin isreferabletoasharpcyclic decreaseinalluvial

ne-grained facies whose 9-06-2004, 10:43:55 PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35

to the most important paleogeographic change in the panorama: to the E and NE, the Valsinni Structure, basin. This sedimentary stage was controlled by the composed of pre-Pliocene units, is observable (north- uplifting of the Valsinni ridge that separated to the eastern margin of Sant’Arcangelo Basin); to the SW, east the Sant’Arcangelo Basin from the foredeep. In the highest mountains of the southern Apennines the Sant’Arcangelo Basin the sedimentary succession (Pollino, Alpi, and Raparo) are visible. Furthermore, is represented by prograding coarse grained facies of to the west, marine prodelta and shelf mudstones of a marine fan delta underlying fi ne grained facies of the Monte Cotugno Supersynthem (Upper Pliocene), shallow marine systems (nearshore or lagoon). The delta front sandstone lobes of the San Giorgio system overlying alluvial and lacustrine facies record the (Early Pleistocene), fan delta and lacustrine systems overall evolution to continental depositional environ- of the Noepoli synthem (Lower Pleistocene), lacus- ments. trine mudstones and alluvial sheetlike conglomer- In the foredeep depocenter, the development of ma- ates of the Francavilla and Chiaromonte synthems rine delta systems (Lower-Pleistocene Tursi Sand- (Lower Pleistocene), are visible. Finally, at the top stones) is the result of the eastward migration of the of the westernmost outcrops, alluvial facies including alluvial deposition through the superimposition of paleosols (Sabbie e Conglomerati di Serra Corneta, hydrological channels on the rising outer thrust. Middle Pleistocene) may be observed. The Serrapotamo Supersynthem The Serrapotamo Supersynthem, composed of lacus- In the evening we will cross an important archeologi- trine and alluvial systems up to 300 m thick, follows cal area, along the Ionian coast, where it is possible the last compressional phases which restricted the to visit remains of Magna Graecia. During the 7th sedimentation area along the western margin. On a century BC, Greek settlers began to disembark on gentle syncline, lacustrine and alluvial systems (the the shores of southern Italy, establishing primitive Francavilla Synthem) developed. Most of the supply outposts. Successively, traders, farmers and craftsmen came from the internal areas (western sides); fi ning founded Sybaris, Poseidonia (Paestum), Crotone and, upward sequences attest to periods of increase in maybe, Naples. The artefacts they have left behind are subsidence that confi ned the coarse detritus in the clearly Hellenic, yet marked with their own “provin- proximal areas of the basin, in accordance with mod- cial” themes and shapes. Locally it is possible to ob- els proposed by Blair and Bilodeau (1988), Heller et serve remains of Heracleia and Metapontum Hellenic al. (1988), Paola (1988), and Hartley (1993). villages, represented by temples - as the 6th century The Chiaromonte Synthem records the extension BC Tavole Palatine temple - walls and columns; near of the braided plain towards the N-NW, on the area the villages of Policoro and Metaponto two rich ar- previously dominated by lacustrine sedimentation cheological museums are present. (the Francavilla Synthem), and is indicative both of The fi eld trip will end in Bari, where we will arrive in an increase in erosion, transport and sedimentation as the night, after dinner. well as of a decrease in subsidence. The overlying paleosol and the following cutting Acknowledgments and alluvial phases recorded in the uppermost unit Our research was supported by MIUR (grants 60% (Sabbie e Conglomerati di Serra Corneta), represent 2000 and 2001 and PRIN 2003 to L. Sabato; grants successive events in which the climatic variations, the PRIN 2000 and 2002 to L. Simone and A. Laviano) regional rising, and the various phases of cutting and terracing in the hydrographic networks marked the References

subsequent history of this region (Giannandrea and Amato, A. and Montone, P. (1997). Present-day fi eld P14 to P36 olume n° 4 - from Loiacono, 2003). and active tectonics in southern peninsular Italy. Geoph. Journ. Int. 130, 519-534. V Stop 5.6: Anketell, J.M., Cegla, J. and Dzulynski S. (1970). On the Sarmento valley and San Giorgio village the deformational structures in systems with reversed The Sarmento valley offers a panoramic view and a density gradients. Annales de la Société Géologique noticeable cross section of the southern sector of the de Polonie (1), XL, 3-30. Sant’Arcangelo Basin. San Giorgio village is located Bally, A.W., Burbi, L., Cooper, C. and Ghelardoni, R. on extensive outcrops of the San Giorgio delta system (1986). Balanced sections and seismic reflection pro- (the Sinni Supersynthem) and offers an almost 360° fi les across the Central Apennines. Mem. Soc. Geol.

39 - P35

P35_R_OK 39 9-06-2004, 10:43:57 P35_R_OK 40

Volume n° 4 - from P14 to P36 P35 - P35 Leaders: P. Pieri,L.Sabato,M.Tropeano M. and Tropeano, M.( Beneduce, P., Festa, V., Francioso,R.,Schiattarella, It Soc. Geol.It lucano): caratterigeologiciepaleoambientali. parte NorddelBacinodiS. Arcangelo (Appennino Sabato L.(1988).Idepositipliopleistocenicidella Caldara M.,LoiaconoF., MorlottiE.,PieriP. and 908. Neogene. reconstruction ofthepery-Tyrrenian areaduringthe (1990). Palinspastic restorationandpaleogeographic Pescatore, T., RicciLucchi,F. and Tortorici, L. G., Gelati,R.,Lentini,F., Massari,F., Moratti,G., Boccaletti, M.,Ciaranfi ba sins:sedimentaryresponsetoepisodictectonism. of tectoniccyclothems inrift,pull-apartandforeland Blair T.CC and W.C. Bilodeau(1988).Development Physics andChemistryoftheEarth P Garaguso (Basilicata). dell’Appennino meridionalefraOliveto lucanoe I depositiplio-pleistocenicidiavanfossa albordo Caldara, M.,Ciaranfi Il Quaternario vulcanoclastiche (BacinodiS. Arcangelo, Basilicata). Depositi lacustriinfrapleistoceniciconintercalazioni Caggianelli, A., Dellino,P. andSabato,L.(1992). 82, 47-58. (Region ofNaples,Italy). tor ofthe Tyrrhenian fl Geomorphology andneotectonicevolution ofasec- C., Russo,F., Santangelo,N.andSanto, A. (1991). Brancaccio, L.,Cinque, A., Romano,P., Rosskopf, 17, 909-927. f Apennines, Italy)asaconsequenceofdeep-seated Northern S.Arcangelobasins(Basilicata,Southern transpressional evolution ofthe Anzi-Calvello and Bonini, M.andSani,F. (2000).Pliocene-Quaternary Mem. Soc.Geol.It (1988a). GeologicalmapofSouthern Apennines. Bonardi, G.,D’Argenio, B.andPerrone, V. (eds) 17-35. rapporti conl’ArcoCalabro. aperti sullasuaevoluzione pre-appenninicaedisuoi Liguride Auct: statodelleconoscenzeeproblemi Miconnet, P. andPerrone, V. (1988b).IlComplesso Bonardi, G., Amore, F.O., Ciampo,G.,deCapoa,P., aeoecology ault reactivation. atterns intheMateraHorstarea,SouthernItaly. . 35(I),257-310. 16,517-520. Pa 77,41-50. . 41,391-410. laeogeography, Palaeoclimatology, Pal- 5,123-132. . 41. Marine andPetroleum Geology

, N.andMarino,M.(1993). ank ofthesouthern Apennines Boll. Soc.Geol.It

, N.,Cosentino,D.,Deiana, 2004 Z. Geomorph.,Suppl-Bd ). Confl Mem. Soc.Geol.It. , 29(10),717-724

icting Drainage . 112,893- Mem.

41, .

Structural patternoftheCampania-Lucania Apen- D’Argenio, B.,Pescatore, T. andScandone,P. (1975). 121-141. Italy.foredeep, southern Adriatic f Casnedi, R.(1988).Subsurface basinanalysisof Mem. Soc.Geol.It geodinamic evolution oftheSouhern Apennines. Muller, C.,Sage,L.and Vially, R.(1988).Neogene Casero, P., Roure,F., Endignoux,L.,Moretti,I., Geol latitude indicators:problemsandlimitations. Simone, L.(1988).Carbonatelithofacies aspaleo- Carannante, G.,EstebanM.,MillimanJ.D.and the MesozoicIonianBasin. Catalano, R.,Doglioni,C.andMerlini,S.(2001).On Carter, Eds.),219-233. dell’Appennino Foggiano. Crostella, A. and Vezzani, L.(1964).LaGeologia Boll. Soc.Geol.It dell’Avanfossa appenninica dalleMarchealloJonio. Crescenti, U.(1975).Sulsubstratopre-pliocenico Boll. Soc.Geol.It dell’Appennino meridionale(settoreIrpino-Dauno). nell’ambito del“forelandbasinsystem”pliocenico e paleogeografi M. (2003).Evoluzione tettono-sedimentaria Ciarcia, S.,DiNocera,Matano,F. and Torre, It Salento (Pugliacentromeridionale). illustrative allacartageologicadelleMurge edel Ciaranfi Ionico, Basilicata). sudoccidentale dellaFossa bradanica(Montalbano una successioneinfraemesopleistocenicanellaparte A. andDeRosa,R.(1996).Studiostratigrafi Ciaranfi Fi sulla neotettonicadellaFossa bradanica. Ricchetti, G.and Walsh, N.(1979).Considerazioni Ciaranfi Fi Carta Neotettonicadell’Italiameridionale. G., Torre, M., Tortorici, L.and Vezzani, L.(1983). Lambiase, S.,Pieri,P., Rapisardi,L.,Ricchetti, Ciaranfi 49-64. atic foredeep(Italy). turbidites inmigratingbasinsofthesouthern Adri- Casnedi, R.(1991).Hydrocarbonaccumulationin 1370-1380. ault-controlled turbiditesysteminBradano Trough, . 41,449-460. nalizzato GeodinamicaCNR nalizzato GeodinamicaCNR, . 60,333-336.

, N.,Pieri,P. andRicchetti,G.(1988.)Note , N.,Marino,M.,Sabato,L.,D’Alessandro, , N.,Maggiore,M.,Pieri,P., Rapisardi,L. , N.,Ghisetti,F., Guida,M.,Iaccarino,G.,

a deidepositi“wedgetop” . 94,583-634. . 122,117-137. ., 41,109-120. Boll. Soc.Geol.It In

“Facies models”(Boumaand Boll. Soc.Geol.It Geoph. Journ. Int , 251,73-95. 515, 62pp. AAPG Bull Mem. Soc.Geol. . 115,379-391. Progetto Progetto 9-06-2004, 10:43:58 . 83(1), . 72/11,

. 144, co di Sed. PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35

nines. Quaderni “La Ricerca Scientifi ca”, 90, 313- successioni alluvionali e lacustri quaternarie affi oranti 327. nella media valle del fi ume Sinni (Appennino DeCelles, P.G. and Giles, K.A. (1996). Foreland basin meridionale, Basilicata). Il Quaternario, 16 (2), 257- systems. Basin research 8, 105-123. 267. Doglioni, C. (1991). A proposal for the kinematic Gilbert, G.K. (1885). The topographic features of lake modelling of W-dipping subduction - possible appli- shores. U.S. Geol. Surv. 5th Annual Rep., 69-123. cation to the Tyrrenian-Apennines system. Terranova Gueguen, E., Doglioni, C. and Fernandez, M. (1997). 3, 423 -434. Lithospheric boudinage in the Western Mediterranean Doglioni, C. (1994). Foredeeps vs. subduction zones. back-arc basin. Terranova 9, 184-187. Geology 22, 271-274. Hartley, A.J. (1993). Sedimentological response of an Doglioni, C., Mongelli, F. and Pialli, G. (1998). alluvial system to source area tectonism: The Seilao Boudinage of the Alpine Belt in the Apenninic back- Member of the Late Cretaceous to Eocene Purilactis arc. Mem. Soc. Geol. It. 52, 457-468. Formation of Northern Chile. In “Alluvial sedimen- Doglioni, C., Mongelli, F. and Pieri, P. (1994). The tation” (M. Marzo and C. Puigdefabregas, Eds), pp. Puglia uplift (SE-Italy): an anomaly in the foreland of 489-500. IAS Sp. Publ. 17. Blackwell, Oxford. the Apenninic subduction due to buckling of a thick Heller P.L., Agevine C.L., Winslow L.S. and Paola C. continental litosphere. Tectonics 13 (5), 1309-1321. (1988). Two-phase stratigraphic model of foreland- Doglioni, C., Tropeano M., Mongelli, F. and Pieri, basin sequences. Geology 16, 501-504. P. (1996). Middle-Late Pleistocene uplift of Puglia: Hippolyte, J.C., Angelier, J., Roure, F. and Casero, an “anomaly” in the Apenninic foreland. Mem. Soc. P. (1994). Piggyback basin development and thrust Geol. It. 51, 101-117. belt evolution: structural and palaeostress analyses Festa, V. (2003). Cretaceous structural features of of Plio-Quaternary basins in the Southern Apennines. the Murge area (Apulian Foreland, Southern Italy). Journ. Struct. Geol. 16, 159-173. Eclogae geol. Helv. 96, 11-22. Iannone, A. and Pieri, P. (1979). Considerazioni Finetti, I. (1982). Structure, stratigraphy and evolu- critiche sui “Tufi calcarei” delle Murge. Nuovi dati tion of central Mediterranean. Bollettino di Geofi sica litostratigrafi ci e paleoambientali. Geografi a Fisica e Teorica ed Applicata XXIV (96), 247-312. Dinamica Quaternaria 2, 173-186. Funiciello, R., Montone, P., Parotto, M., Salvini, F. Iannone, A. and Pieri, P. (1982). Caratteri neotettonici and Tozzi, M. (1991). Geodynamical evolution of delle Murge. Geologia Applicata e Idrogeologia, an intra-orogenic foreland: the Apulia case history XVIII (II), 147-159. (Italy). Boll. Soc. Geol. It. 110, 419-425. Ippolito, F., D’Argenio, B., Pescatore, T. and Funiciello, R., Parotto M., Praturlon A. (eds) Scandone, P. (1975). Structural-stratigraphic units (1975). Carta tettonica d’Italia. Progetto Finalizzato and tectonic framework of Southern Apennines. In Geodinamica CNR, 269. “Geology of Italy” (Squyres, Ed.) pp. 317-328. Gallicchio, S. and Maiorano, P. (1999). Revised Knott, S.D. (1987). The Liguride Complex of South- stratigraphy of the Serra Palazzo Formation, a Mi- ern Italy - a Cretaceous to Paleogene accretionary ocene foredeep turbidite succession of the Southern wedge. Tectonophysics 142, 217-226. Apennines. Riv. It. Pal. e Strat. 105 (2), 287-302. Lazzari, M. and Pieri, P. (2002). Modello stratigrafi co- Gallicchio, S., Marcucci, M., Pieri, P., Premoli Silva, deposizionale della successione regressiva I., Sabato, L. and Salvini, G. (1996). Stratigraphical infrapleistocenica della Fossa Bradanica nell’area data from a Cretaceous claystones sequence of the compresa tra , Genzano e Spinazzola. Mem.

“Argille Varicolori” in the Southern Apennines (Ba- Soc. Geol. It. 57, 231-237. P14 to P36 olume n° 4 - from silicata, Italy). Palaeopelagos 6, 517-526. Loiacono, F. (1983). Facies di conoide alluvionale nei Gambassini, P. (1967). Il Conglomerato Calabriano depositi pleistocenici del Bacino di Sant’Arcangelo V della Serra del Cedro presso Tricarico (Matera). (alta valle del F. Sinni). Geografi a Fisica e Dinamica Accademia Gioenia Scienze Naturali s VI, XVIII, Quaternaria 6, 31-38. 153-157. Loiacono, F. and Sabato, L. (1987). Stratigrafi a e Gambini, R. and Tozzi, M. (1996). Tertiary geo- sedimentologia di depositi pleistocenici di fan-delta dynamic evolution of Southern Adria microplate. sul margine appenninico della Fossa bradanica Terranova 8, 593-602. (Tricarico, Basilicata). Mem. Soc. Geol. It. 38, 275- Giannandrea, P. and Loiacono, F. (2003). Le 296.

41 - P35

P35_R_OK 41 9-06-2004, 10:43:59 P35_R_OK 42

Volume n° 4 - from P14 to P36 P35 - P35 Leaders: P. Pieri,L.Sabato,M.Tropeano occidentali. Martinis, B.(1961).SullatettonicadelleMurge nord- It pleistocenici di (Potenza). Maggiore, M.and Walsh N.(1975).Idepositiplio- of Taranto (Pleistocene,southernItaly). Gilbert-type gravel deltasintheinterlandofGulf Massari, F. andParea, G.C.(1990). Wave-dominated 35, 881-913. Murge. biostratigrafi Luperto Sinni,E.(1996).Sintesidelleconoscenze e signifi Silentina diBase:assettostrutturale,metamorfi Mauro, A. andSchiattarella,M.(1988).L’Unità 311-331. IASSp.Publ.10.Blackwell,Oxford. grained deltas”(A.ColellaandD.B.Prior, Eds),pp. ergy, microtidalmarineenvironment. gravel beachsequencesinamoderate-tohigh-en- Massari, F. andParea, G.C.(1988).Progradational dell’Appennino meridionale. meridionale. prospezione petroliferadiunazonadell’Italia Migliorini, C.(1937).Cennosullostudioesulla inferred byseismicprofi Merlini, S.andCippitelli,G.(2001).Structuralstyles Apennines). ic Lagonegro UnitsinSWLucania(SouthernItalian Mazzoli, S.(1992).StructuralanalysisoftheMesozo- 1201-1213. de Lagonegro. Miconnet, P. (1988).Evolution mesozoiquedusecteur Kluwer Academic Publishers,GreatBritain. sins” (G.B. Vai andI.P. Martini,Eds.),pp.441-454. gen: the Apennines and Adjacent MediterraneanBa- modello strutturale. centro meridionale.Sezionigeologicheepropostadi Mostardini, F. andMerlini,S.(1986). Appennino 153-160. the Southern Apennines orogenicbelt. of ophiolite-bearingterranesinthedevelopment of Monaco, C.and Tortorici, L.(1995). Tectonic role 1-11. delle Madonie(Siciliacentro-settentrionale). Ogniben L.(1963).Leformazionitipo Wildfl F. Ori, G.G.,Serafi It geologia delconfi Ogniben L.(1969)-Schemaintroduttivo alla Ist. Geol.Min.Univ. Padova . 94,93-109. . 8,453-763. , Casnedi,R.,Colalongo,M.L.,andMosna,S. Mem. Soc.Geol.It

cato tettoniconelquadrogeologico

Rend. Acc. Naz. Lincei Naz. Rend. Acc. Studi Geol.Camerti che delCretaceoGargano edelle 2nd Petroleum worldCongress Mem. Soc.Geol.It

ni, G., Visentin, C.,RicciLucchi, ne calabro-lucano. Mem. Soc.Geol.It

les. . 51/2,995-996. 24, 1-56. In Mem. Soc.Geol.It

“A 12,117-146. . 41,321-330. S.8,31pp. natomy ofanoro- Mem. Soc.Geol. Boll. Soc.Geol. Sedimentology . 35,177-202. Terr In

anova “Coarse- , Paris, Mem.

ysch . 41, smo

7,

a geodynamicmodel. geometries andbasementstructure. A hypothesisfor Southern Apennines: Relationshipsbetweencover and Toccaceli, R.M.(1992). Active tectonicsinthe Ortolani, F., Pagliuca, S.,Pepe,E.,Schiattarella,M. Zeist, 1991,1-85. Adriatic Foredeep Field Trip GuideBook Association ofPetroleum Geologists Conference, to surface andsubsurface geology. In: (Marche and Abruzzo, Italy): An integrated approach Pliocene-Pleistocene (1991). The Foredeep Adriatic since late Tortonian times. rhenian basinand Apenninic arcs:kinematicrelations P 231-243. Springer Verlag, New York. Analysis” (K.KleinspehnK. And C.Paola Eds),pp. in alluvialbasins. P 413- 419. (Pliocene-Pleistocene). belt-foredeep SystemoftheSouthern Apennines propagation andSedimentaryResponseinthe Thrust- P pp. 157-176. Atti deiConvegni deiLincei80,Rome. Boriani, M.Bonafede,G.B.PiccardoandG.B.,Eds), phere inItaly. Advances inearthscienceresearch”(A. sive sinkingofareliclithosphericslab. mountain building inthe Apennines. The roleofpas- P 425-451. in thesouthern Apennines. and Santini,U.(1992). The Numidian-sandevent P Academic Publishers,GreatBritain. (G.B. Vai andI.P. Martini,Eds.),pp.401-440.Kluwer Basins” Mediterranean and Adjacent the Apennines Pescatore, T., Renda,P. and Tramutoli, M.(1992). ennines, Italy. basin andcoeval carbonateplatformsinsouthern Ap- relationships betweenMeso-CenozoicLagonegro Tr Pescatore, T., Renda,P., Schiattarella, M.and It nell’Appennino campanolucano. Pescatore, T. (1988).Lasedimentazionemiocenica K rine canyons, fans, andtrenches”(D.J.Stanley andG. tation inSouthernItaly. tonically controlledFan andbase-of-SlopeSedimen- Pescatore, T. (1978). The Irpinids: A Modelof Tec- XLIII, 297-337. atacca, E.,SartoriR.andScandoneP. (1990). Tyr- aola C.(1988).Subsidenceandgravel trasport atacca, E.andScandone,P. (2001).Late Thrust atacca, E.andScandone,P. (1989).Post-Tortonian atacca, E.,Scandone,P., Bellatalla,M.,Perilli,N. . 41,37-46. elling, Eds),pp.325-339. amutoli, M.(1999).Stratigraphicandstructural Te ctonophysics In

“ New Perspectives inBasin IGCP In In

“Sedimentation insubma- “A Mem. Sci.Geol.Padova Mem. Soc.Geol.It.

315,269-286. Nº 276,Newsletter, 5, natomy ofanorogen: Mem. Soc.Geol. In 3rd European

“The lithos- . EAPG, 9-06-2004, 10:44:01 45,

PLIO-PLEISTOCENE STRATIGRAPHIC AND TECTONIC EVOLUTION OF THE FORELAND-FOREDEEP-CHAIN SYSTEM IN SOUTHERN ITALY P35

“Tufi ti di Tusa” e Flysch Numidico nella Lucania 661-689. centrale (Appennino meridionale). Rend. Acc. Sc. Fis. Prosser, G., Schiattarella, M., Tramutoli, M., Mat. Soc. Naz. Sc. Lett. e Arti Napoli 59, 57-72. Doglioni, C., Harabaglia, P. and Bigozzi, A. (1996). Pescatore, T., Salvati, G. and Tramutoli, M. (1980). Una sezione rappresentativa dell’Appennino Regressive depositional cycles in the Gorgoglione meridionale. Conferenza sulla Ricerca Scientifi ca Flysch, Irpinids, (Southern Italy). Geologica Romana. in Basilicata, Università della Basilicata - Regione 19, 51-61. Basilicata, Febbraio 1996. Pescatore, T. and Tramutoli, M. (1980). I rapporti tra Ricchetti, G. (1975). Nuovi dati stratigrafi ci sul i depositi del bacino di Lagonegro e del bacino irpino Cretaceo delle Murge emersi da indagini del nella media valle del Basento (Lucania). Rend. Acc. sottosuolo. Boll. Soc. Geol. It. 94, 1083-1108. Sc. Fis. Mat. Soc. Naz. Sc., Lett. e Arti Napoli 47, Ricchetti, G. (1980). Contributo alla conoscenza 19-41. strutturale della Fossa bradanica e delle Murge. Boll. Pieri, P. (1980). Principali caratteri geologici e Soc. Geol. It. 49, 421-430. morfologici delle Murge. Murgia sotterranea, Ricchetti, G., Ciaranfi , N., Luperto Sinni, E., Bollettino Gruppo Speleo Martinense 2, 13-19. Mongelli, F. and Pieri, P. (1988). Geodinamica ed Pieri, P., Festa, V., Moretti, M. and Tropeano, M. evoluzione sedimentaria e tettonica dell’avampaese (1997a). Quaternary tectonic activity of the Murge apulo. Mem. Soc. Geol. It. 41, 57-82. area (Apulian Foreland - southern Italy). Annali di Ricchetti, G. and Mongelli, F. (1980). Flessione e Geofi sica XL (5), 1395-1404. campo gravimetrico della micropiastra apula. Boll. Pieri, P., Sabato, L. and Loiacono, F. (1993). Carta Soc. Geol. It. 99, 431-436. geologica del Bacino di Sant’Arcangelo (tra il Ricci Lucchi, F. (1986). The Oligocene to Recent Torrente Sauro e il Fiume Agri). Scala 1:50.000. Ed. foreland basins of the northern Apennines. In “Fore- Paternoster, Matera. land basins” (P.A. Allen and P. Homewood, Eds.), pp. Pieri, P., Sabato, L., Loiacono, F. and Marino, M. 105-139. IAS Sp. Publ. 8. Blackwell, Oxford (1994b). Il bacino di piggy-back di Sant’Arcangelo: Roure, F., Casero, P.and Vially, R. (1991) Growth evoluzione tettonico-sedimentaria. Boll. Soc. Geol. It. processes and melanges formation in the southern 113, 465-481. Apennines accretionary wedge. Earth and Planetary Pieri, P., Sabato, L. and Marino, M. (1996b). The Plio- Science letters 102, 395-412. Pleistocene piggyback Sant’Arcangelo Basin: tecton- Royden, L., Patacca, E. and Scandone, P. (1987). Seg- ic and sedimentary evolution. Notes et Mémoires du mentation and confi guration of subducted lithosphere Service géologique du Maroc 387, 195-208. in Italy: an important control on thrust-belt and fore- Pieri, P., Sabato, L. and Tropeano, M. (1994a). deep-basin evolution. Geology 15, 714-717. Evoluzione tettonico-sedimentaria della Fossa Sabato, L. (1996a) - Delta calcareo terrazzato nella bradanica a sud dell’Ofanto nel Pleistocene. In: Guida Calcarenite di Gravina (Pleistocene)-Minervino, alle escursioni, 77° Congresso Soc. Geol. It., Bari, Murge nord-occidentali. Mem. Soc. Geol. It. 51, Italy, 23 September-1 October 1994, Quaderni della 517-526. Biblioteca Provinciale di Matera, 15, 35-54. Sabato, L. (1996b). Quadro stratigrafi co-deposizionale Pieri, P., Sabato, L. and Tropeano, M. (1996a). dei depositi regressivi nell’area di Irsina (Fossa Signifi cato geodinamico dei caratteri deposizionali bradanica). Geologica Romana 32, 219-230. e strutturali della Fossa bradanica nel Pleistocene. Sabato, L. (1997). Sedimentary and tectonic evolution Mem. Soc. Geol. It. 51, 501-515. of a lower-middle Pleistocene lacustrine system in the

Pieri, P., Vitale, G., Beneduce, P., Doglioni, C., Sant’Arcangelo piggyback basin (Southern Italy). P14 to P36 olume n° 4 - from Gallicchio, S., Giano, S.I., Loizzo, R., Moretti, M., Geologica Romana 33, 137-145. Prosser, G., Sabato, L., Schiattarella, M., Tramutoli, Sabato, L. (2000) - A lower-middle Pleistocene V M., Tropeano, M. (1997b). Tettonica quaternaria lacustrine system in late evolutionary stages of the nell’area bradanico-ionica. Il Quaternario 10, 535- Sant’Arcangelo Basin (southern Italy). In “Lake 542. basins through space and time” (E.H. Gierlowski- Pomar, L. and Tropeano, M. (2001). The Calcarenite Kordesch and K.R. Kelts, Eds.), pp. 543-551. AAPG di Gravina Formation in Matera (southern Italy): new Studies in Geology 46. AAPG, Tulsa. insights for coarse-grained, large-scale, cross-bedded Sabato, L., Bertini, A., Masini, F., Albianelli, A., bodies encased in offshore deposits. AAPG Bull. 85, Napoleone, G. and Pieri, P. (in press, b). The lower

43 - P35

P35_R_OK 43 9-06-2004, 10:44:02 P35_R_OK 44

Volume n° 4 - from P14 to P36 P35 - P35 Leaders: P. Pieri,L.Sabato,M.Tropeano catena appenninicameridionale). geopetrolifera dellaFossa bradanica(avanfossa della Sella, M., Turci, C.andRiva, A. (1988).Sintesi Quaternario nel bacinodelMercure(Confi Analisi strutturaleedosservazioni morfostratigrafi Schiattarella, M., Torrente, M.M.andRusso,F. (1994). Abstract Supplement1. T Schiattarella, M.,Doglioni,C.,Prosser, G.and geomorfologici dellaGravina diMatera“Parco T 3, 737-789. geologia dell’Italiameridionale. Selli, R.(1962).IlPaleogene nelquadrodella 41, 87-107. ematics oftheSouthern Apennines. Italy. case-study fromtheLucanian Apennine, southern S.I. (2003).Quaternaryupliftvstectonicloading:a Schiattarella M.,DiLeoP., BeneduceP. andGiano Soc. LondonSp.Publ.135,London. Strachan andJ.F. Dewey, Eds.),pp.341-354.Geol. T southern Italy. the PollinoRidge,Calabria-Lucaniaboundary, Schiattarella, M.(1998).Quaternarytectonicsof It l’Appennino calcareo. serie calcareo-silico-marnosaeisuoirapporticon Scandone, P. (1967).Studidigeologialucana:la della BibliotecaProvinciale diMatera,15,87-104. Bari, Italy, 23September-1 October1994,Quaderni It Apennines, Italy).Inpresson: gilliti eradiolaritidiCampomaggiore”unit,(Southern ( P. Sabato L.,GallicchioS.,PieriP., SalviniG.andScotti tional. Apennines, Italy).Inpresson: custrine sequenceinSant’ArcangeloBasin(Southern and middlePleistocenerecordoftheSanLorenzola- Pollino (Confi Schiattarella, M,(1996). Tettonica dellaCatenadel 1-175. Guida alleescursioni, 77°Congresso Soc.Geol.It del margine appenninicodi Tricarico (Basilicata).In: Sabato, L.andMarino,M.(1994).Idepositipliocenici ramutoli, M.(1997).Large-scale geometryandkin- ropeano, M.(1992). Aspetti geologicie ranstensional Tectonics” (R.E.Holdsworth, R.A. . 51,543-566. “Profi in press Quaternary International

lo CROP 04”. , a).Cretaceousanoxicevents inthe“Ar- 7,613-626.

ne Calabro-Lucano). In

“Continental Transpressionaland Boll. Soc.Natur. Napoli

ne Calabro-Lucano). , 101-102,239-21. Spec. Boll.Soc.Geol. Quaternary Interna- Mem. Soc.Geol.It Mem. Soc.Geol.It Terr Mem. Soc.Geol. anova

9, 109,

che 76, Il ., . . Tr del Materano”. Archeologico StoricoNaturaledelleChieseRupestri In Calcarenite diGravina Formation, Puglia,SEItaly. ate-water carbonatesystemtoforcedregression: the Plio-Pleistocene mixed bioclastic-lithoclastictemper- Tr Quaternario nell’area delleMurge (Avampaese apulo). Te Calcagnile, G.,DelGaudio, V. andPierri,P. (1997). Tr Zagarella. margine orientaledellaFossa bradanica:L’Horst di Evidenze ditettonicadistensiva plio-pleistocenicaal Tr Soc. London,Sp.Publ.172,London. Hunt andR.L.Gawthorpe, Eds.),pp.217-243.Geol. Tr ing andcannibalizationofaforedeep:theBradanic 399-416. southern Apennines, Italy.southern Apennines, tory ofthePlio-PleistoceneSant’Arcangelobasin, Zavala, C.(2000).Stratigraphyand sedimentary his- ionico. sistema catena-avanfossa lungoilfrontebradanico- dal passaggioMiocene-Plioceneall’attualedel V Naturali S.Arcangelo (Lucania V re Murge baresi. V 519-529. lucano: modellocinematico. La tettonicaplio-pleistocenicadelconfi Tu 449-454. - SouthernItaly). the South-Apenninesforedeep(Bradanic Trough The Quaternary“post-turbidite”sedimentationin Tr Spec. Publ.191,London. L.E. Frostick,Eds.),pp.55-79.Geol.Soc.London, Causes, ControlsandConsequences”(S.J.Jones ezzani, L.(1967).Ilbacinoplio-pleistocenicodi alduga, A. (1965).Contributo allaconoscenzadelle itale, G.(1996).Evoluzione tettonicaestratigrafi gione pugliese : “Sedimentaryresponsestoforcedregression” (D. opeano, M.,Marino,M.andPieri,P. (1994). opeano, M.andSabato,L.(2000).Responseof opeano, M.,Pieri,P., Moretti,M.,Festa, V., opeano M.,Sabato,L.andPieri,P. (2002a).Fill- ough (SouthernItaly). opeano, M.,Sabato,L.andPieri,P. (2002b). ttonica quaternariaedalementidisismotettonica rco E.,MarescaR.andCappadonaP. (1990). PhD thesis s6,18,207-227. Il Quaternario 10 (2),543-548. Itinerari Speleologici Studi Geologici emorfologici sulla I,15pp. Boll. Soc.Geol.It , University ofBari,Italy, 159pp. ). Accademia Gioenia Scienze Gioenia ). Accademia In 7(2),597-606.

“Sediment FluxtoBasins: Riv. It.Pal. Strat Mem. Soc.Geol.It . 121,vol. Sp.1, 2,19-33.

ne calabro- 9-06-2004, 10:44:04 . 106,

45,

ca Il

Back Cover: fi eld trip itinerary with location of the stops

P35_ copertina_R_OK E 9-06-2004, 10:16:40 FIELD TRIP MAP INTERNATIONAL GEOLOGICAL CONGRESS

nd 32

Edited by APAT

P35_ copertina_R_OK B 9-06-2004, 10:17:00