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3 2 1 Article type : ArticleOriginal 22-Jan-2014 : Date Accepted Date Revised :07-Jan-2014 04-Jan-2013 : Date Received This article is protected by copyright. All rights reserved. reserved. rights All byprotected copyright. is article This 10.1111/bre.12061 doi: between version to differences and Versionlead of this Please the this Record. as cite article may which process, proofreading and pagination typesetting, copyediting, the through been not has but review peer full undergone and publication for been accepted has article This Cretaceous synsedimentary deformation was dominated by positive inversion of Jurassic Jurassic of by dominated inversion was positive Cretaceous synsedimentary deformation place. took Cerro Toro of channels conglomerate and turbidites of where deposition the wedge-top depozone domain of was belt an Coniacian-Campanian fold-thrust active internal present the that showing deposition syntectonic of evidence present multiple We deposited in depocenter. bodies deep-water an axial foredeep conglomerate-filled channel of example a world-class includes Formation that Cerro Toro Cretaceous Upper turbiditic mainly belong tothe sequences studied Andes. The Patagonian southern in the and sedimentation deformation of understanding the for withimplications Basin, Magallanes sequences the Austral of or basin foreland angular within syntectonic basal unconformities Coniacian-Campanian of evidence present the and seismic We existence for field Abstract Parque Martín Mendoza,San s/n, 5500 Argentina [email protected]. Consultor, Rivero Gaucho 635 (9000), Comodoro Chubut. Rivadavia, y Científicas CONICET-IANIGLA Investigaciones Tecnológicas, Centro Regional de Instituto Andinos de de "DonEstudios PabloGroeber". AiresBuenos – Universidad Geodynamic context for the deposition of coarse-grained deep- ofcoarse-grained for the deposition context Geodynamic water axial channel systemsAndes channel in axial the water Patagonian Laura Beatriz Giambiagi BeatrizLaura Matías C. Ghiglione C. Matías 1 ; Jeremías; Likerman 2 ; Beatriz Aguirre-Urreta Beatriz ; 1 ; VanesaBarberón ; 1 ; Fabián; Suarez 1 ; 3

brought toyouby provided byCONICETDigital CORE Accepted Article of the Austrian molasse basin (Hubbard (Hubbard basin molasse theAustrian of deep-water wedge-topthe are depozone. such tilting sequences withinas examples There to and uplift in response an abrupttectonic develop sedimentary systems typically multiple in patterns dispersal sediment axial 2004), 1996;Ford, &Giles, (DeCelles front the topographic transport Although basin systems a to directedforeland may perpendicular show sediment INTRODUCTION plate a global-scale reorganization event. due accelerated forces and to Basin opening, during itspush during ridge closure, Atlantic its Verdes Rocas of western margin the of the collision both of combination the generated by south Patagonian event stages. This orogenic can berelated to compressional stresses Andean wedge deformation subsequent thanwideningof in orogenic the significant all terms deformation was thatLate throughoutimplying domain, Cretaceous more front internal the orogenic theof advance km a ~50-80 indicates unconformities Coniacian-Campanian of The position axial highs and distributionchannels. of structural controlling the development by separated trenches submarine elongatedaxial thatproduced structures extensional This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This hundred a few from thesouth, towards basement andto depth sedimentary thickness al., 2005;1990; &Lowe, Crane Fildani & Hessler, 2008; Hubbard &Ramos, 1981;1979; Dott Aguirre-Urreta direction in (Scott, theDott, the & 1966; accommodation deepening of space same Winn dispersal with pattern a north sediment a is Magallanes strong to Basin, axial south of the A peculiar feature northern thealso knownAustral system, as foreland basin interpretations. difficult to lead andmay models, conventional by predicted that when with compared accommodation produce space a completely distribution different of et al., Argentina (Carrapa in NW deposits and fluvial 2012), Robertson, & Mediterranean (McCay 2009, 2010; Jobe 2010;Jobe 2009, 2012). This kind of interaction between sedimentary and tectonic processes can processes ofcan and tectonic 2012).kind between interaction sedimentary This et al., 2010; Bernhardt Bernhardt 2010; et al., et al., et al., 2009), turbidite deposits inthe easternmost 2009), turbidite deposits 1982;Macellari 2011) expressed in an increase in total in anincrease 2011)expressed

et al., et al., et 2008, 2010; Romans 2008,2010; Romans 1989; Aguirre-Urreta, 1989; Aguirre-Urreta, et Accepted Article geodynamic models for the region (Wilson, 1991; Fildani Fildani 1991; (Wilson, theregion for models geodynamic There is a conceptual understanding that an inherited tectonic relief and structural is geometryand structural relief a conceptual There understanding that aninheritedtectonic Bernhardt and further south (Fig. & 3;Arbe 1984; Hechem, Lowe, 2008;Hubbard Crane & Laguna 3 extending Surof LagoArgentino Esperanza in Brazo de Abril Última from to Seno Santonian-Campanian (Fig. transport trough ofthe southwardwith along the axis 2) the until active were west tothe located channels andsecondary system axial channel Toro 1984;Jobe Hechem, Dott Dott, 1979; & (Winn platform abyssal the trough,incising marine occurred inception coarse-grainedof strata deep-water thick upto400 pelitic along the m Hubbard theturbidites of Cerro Formation Toro 2 (Figs and 3; 1989, Scott, 1966; Arbe, 2002; a watertowards deep N-S trough developed by marine abyssal to the and south filled Argentinoprograded Lago north of system depositional and deltaic slope submarine where a depozone in within zone, scenario - Campanian occurred foredeep the Coniacian the study remarkable A (Fig.1). and 54°SL between 51° km to 8 up (47°) Posadas atLago meters This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This &Aydin,Gonzales 2008;Bernhardt have (Crane Lowe,the western 2008; beendiscovered & systems secondary axial channel of and uplift structural tectonic confinement sedimentaryfor indications and synsedimentary pattern important dispersal (Fig.controlled their northto sediment Recently, 3). south axial additional and which may have systems, aspects channel deep-water conglomerate triggered the as which such abrupt factors poorlyscenario remain inception of constrained, 2011; Likerman (Wilson, 1991; phase 1989, Arbe 2002; Kraemer, 1998; Romans foreland the during evolution and structural patterns distribution thesedimentary influenced the Middlefrom to rift depth, Late Jurassic troughphase created this relict ~2000 N-S m that et al., et al., 2008). In early Coniacian time (ca. time 2008).Inearly 87Ma, Bernhardt Coniacian 2012). et al., et al., 2013). However, important aspects of this singular foreland basin basin foreland this singular of aspects important However, 2013). 2010). A 4 to 8 km wide by >100 km long deep-water 2010). towide by >100 del km Sierra A 4 8 km et al., 2011), although the proposed regional although theproposed 2011),

et al., 2008; Kraemer, 1998; 2008; Kraemer, et al., et al., et al., 2009; Fosdick Fosdick 2009; 2012)the abrupt Arbe& 1982; et al., 2008; 2008; et al.,

Accepted Article Ghiglione This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This Patagonian Batholith (Ramos granitoidsthe intrudedof byMesozoic-Cenozoic complexes latesubduction Paleozoic low-grade interpretedarchipelago (Fig.of as composed 1),is mainly metasedimentary rocks The structural thePacific of theregion,metamorphic basement along outcropping SETTING GEOLOGICAL presented data. the of implications geodynamic theglobal of discussion thoughtful and a thrusting, of and distribution dating outstanding an for allows processes sedimentary and deformational other linkingthat case between foreland systems. for may The be a paradigmatic basin highs bystructural trenches submarine elongated of separated bathymetry axial consisting a the geometry inversion produced Thestructural depocenter. of basin geometry of the peculiar thatshaped extensional structures oriented Jurassic N-S of inversion positive by dominated wedge-top depozone in a triggered tectonically probably was conglomerates thatthe in the platform. channels conclude Toro deposition the abyssal Cerro of We submarine of with abruptthe development conglomerate in inception coinciding and time angular withinunconformities the syntectonic Coniacian-Santonian Toro Formation, Cerro of existence the for evidence seismic and field and independent present new,direct We during its deposition. the channel area in the systems generalized uplift of synsedimentary depocenters (Biddle depocenters synrift oriented N-S several produced event extensional Jurassic Late 1999). The (Pankhurst lavas and intermediated mafic withminor ignimbrites (Uliana Gondwana of rifting continental Triassic-Jurassic the inPatagonia during began subsidence Initial extensional et al., 2009; Romans Romans 2009; et al., 1986, Diraison Diraison 1986, et al., et al., et al., 1989), characterized by a bimodal rhyolitic association characterized of 1989), by a bimodal 1982; Hervé Hervé 1982; 2009; Fosdick Fosdick 2009; et al., 2000), filled up by a heterogeneous suite of of suite heterogeneous a up by filled 2000), et al., et al., 2007). 2007).

2011) do not account for for account not do 2011) et al., 2000; Féraud Féraud 2000; et al., et

Accepted Article during the rest of the Cretaceous and Cenozoic (Thomson, 2002), while maintaining the the while maintaining 2002), (Thomson, and Cenozoic Cretaceous the of rest the during (Calderón the wedge accretionary of in Sarmiento deformation prevailed during progressive Cordillera Ma uplift rates ofca. 1–2 80 mm/yr that ca. 85 and fast considerations suggest between also occurred 1995; to Maprior Klepeis 86 (Cunningham, obduction floor and ocean Verdes Basin Rocas of closure (55°SL,1), Fig. channel Beagle (Calderón crystallization with synchronous mica and 4C; Calderón and 4C; Calderón (Figs.zircon Ma U–Pbyielded SHRIMP ofca. 1 152–142 inthe Complex ages Sarmiento Formation (Riccardi Rolleri, (Fig. 1949) and & 1980), in Chile 2; Thomas, that Tobífera Argentina in Complex Quemado El called rocks volcaniclastic and volcanic siliceous This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This crust (Cunningham, 1995;crust (Cunningham, Stern &de 2003; Calderón Witt, duringthe(Dalzielocean floor Late Cretaceous ofthe initiallyPatagonianinvolved the southern Rocas Andes Uplift closure BasinVerdes of 4; 1949;Thomas, 1991). Wilson, (Calderón sedimentation age of Hauterivian indicating a zircons withthe Mayer Zapata Río Formations, detrital maximum and Calderón 2003; DeWitt, & Stern and 4C; 1 zone(Figs our study of located SW Complex Ophiolite are andinterfingered groupedintoSarmiento lavas sea floor the bimodal magmatism the (Dalziel, northern Middle pillow of time remnants during 1981). The Jurassic Late to Basin Verdes inthe Rocas crust oceanic and produced margin Pacific the along maximum (Biddle Basin to Mesozoic information show that the earlywas rift trending N-S NNW in theAustralmainly by means of of zirconand phengite U–Pb bycombined means shown as Ma, ca. 85 at occurred Sarmiento Cordillera in the obduction ophiolitic the ensuing 2010; McAtamney et al., et al., et al., et 2007). Lower Cretaceous sag deposits composed of distal turbidites from from distal turbidites of composed deposits sag Cretaceous Lower 2007). 2012). The basement domain experienced continuous uplift and denudation uplift and continuous experienced domain basement The 2012). et al., et al., 1986, Uliana 1986, 2007; Hervé 2007; Hervé 2011). Subduction inception within the Rocas 2011). inceptionVerdes within theRocas Basin Subduction and et al., et al., 1989, Ghiglione et al., 2013). Stretching was etal.,2013). Ghiglione Stretching 1989, 2007). Outcrop orientation and seismic orientation 2007). seismic Outcrop and et al., et al., et et al., 2007), cover the 2 2007), synrift units (Figs and cover 40 Ar/ 1974), and obduction of its oceanic oceanic its of and obduction 1974), Further2012). south, along the 39 Ar age data representing cooling datarepresenting cooling age Ar

et al., et al., 2010). Geobarometric Geobarometric 2010). 2007, 2012; Klepeis Klepeis 2007,2012; et al.,

Accepted Article & Ramos, 2005; Ghiglione & Cristallini, 2007; Lagabrielle et al. 2009), enhanced by fast byfast enhanced 2009), al. et Lagabrielle 2007; Cristallini, & 2005;Ghiglione Ramos, & Suarez Kraemer,1998, 2003; 2005; (Ramos, 1989, ridge collision or subsidence offast related toepisodes ages Miocene and of Eocene events compressional principal two least at deformation, including Cenozoic well-documented experienced belt ± (Fildani 1Ma), of detrital analysis thezircon basis on age (92 Zapatayielded 1991), sedimentation of a (Wilson Turonian Formation that maximum the of deposits sag theoverlaying 2) Formation (Fig.Barrosa thePunta of sandstones South of Lago (Fig. infill Argentino is byrepresented 3)the first turbiditic coarse clastic 2012). etal., (Varela a concordia ageof96.23Mataof withlayer yielding Formation U-Pb ± Amarilla tuff Ma 0.71 deposits estuarine and Formation, byCerro fluvial overlaid Toro andis of lateral equivalent Kraemer & Riccardi, Lago 1997). East of theViedma Formation the AlbianPiedraClavada is 1984; Hechem, & 2;Arbe (Fig. Formation Mayer Rio the of deposits the sag overlaying Formation Toro Cerro Campanian - lower Albian theupper of section lowerthe is lakes and uplift betweenArgentino theViedma tectonic with sequence associated 2009). first The Urreta &Ramos, 1981;Aguirre-Urreta, 1991; 2002; 1990; Arbe, Romans Wilson, ofdeeperdepositional direction (Fig.the environmentsinthe 1;Aguirre- presence same including the of depocenter, Late fill-thickness in the southwardmain Cretaceous increase first-order a is Basin northern Austral the of phase theforeland of development in the (see America southernmost South Ghiglione of and relatedbasins onset phaseinthe a foreland of units, indicating Austral the sag the on topof sediments clastic coarse of thedeposition caused erosion and uplift Hinterland 2013). et al., (Fosdick sequences theUpper Cretaceous labilefine-grained of erosional denudation due to unroofing (Kraemer, 1998; 2005; &Ramos, Ghiglione Fosdick deformation of the fold-thrust episodes beltthat taper of critical experienced multiple This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This et al., 2010 and references therein). A key-point therein). A and references 2010 et al., et al.,

2011). The Patagonian fold-thrust fold-thrust Patagonian 2011).The 2003). The onset of turbidite of onset The 2003). et al., 2000; Ghiglione 2000;Ghiglione et al.,

Accepted Article turbidity currents (Fig.turbidity 2;Katz, & currents Dott, 1979; 1963; Hubbard Winn deposited and sandstone sequence predominantlyby low-density thin-bedded mudstone withina embedded channels submarine conglomerate-filled large, includes Formation Toro Cerro Argentino,the Lago South of Formation 2). (Fig. Toro theCerro of conglomerate Barrosa of Punta The and overlainby Formation to 2000mudstone, sandstone, is up m was belt underway incipient the Albian. formation showingas that as latest early thrust 101 transition Albian zircon yielding ±age of zone (Fig. a late U/Pb formations 2) 1.1 Ma Fosdick arc. volcanic a juvenile and complex, ophiolitic theSarmiento complexes, basement metamorphic to the 250 km (Fig. south 1, McAtamney (Fildani 2005;Fildani & Hessler, Barrosa sediments that Punta indicategeochemistry andmudstone geochrononology, zircon et al., 2005;Romans Hessler, Formation & (Fildani Punta Barrosa of composition clastic by shown the as basaltic Verdes Rocas floor, of obduction with the sedimentation coincided partial This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This Bernhardt Lowe, 2008; bathymetric high from the axial channel system (Fig. 2; Bernhardt Bernhardt (Fig.2; system thechannel axial high from bathymetric secondarystarted channel earlier(87Ma)system by Silla tothewest, separated syncline a 84Matrough since was (Fig. active 3) (Hubbard water "Sierradel axial withToro" oftransport the system southward along channel the axis water wide along a trough (Figs A4 long deep- 2 and by deep marine to km km 3). >100 8 (Bernhardt channels linked (Winn & Dott, 1979; Dott Dott Dott, 1979; (Winn & linked channels their were at points wheretrace, interconnected theythe some probably conglomerate (Fig.subsidiary thrusts they for were of splay by 3), andalthough a most separated high al., weresystems partially time (82Ma, andlasted up to early coeval Bernhardt Campanian 2012); the main channels were confined were and front to west channels the by uplifted the confined basement the 2012); main 2010; Fosdick 2010;Fosdick et al., 2012) of coarse-grained deep-water strata up to 400 m thick took place place took thick 400 m to up strata coarse-grained deep-water of 2012) et al., et al. et al., 2011; McAtamney McAtamney 2011; (2011) dated a volcanic ash at the Zapata/Punta Barrosa Barrosa attheZapata/Punta ash volcanic a dated (2011) 2011; Jobe 2011;Jobe et al., 2008), and equivalent units in Peninsula Brunswick Brunswick Peninsula in units equivalent and 2008), et al., et al., et al., et al., 2011) were derived from uplifted Paleozoic uplifted Paleozoic from were derived 2011) 1982; Arbe & Hechem, 1982; Arbe&Hechem, 1984; Hubbart 2010). The ca. 87-84 Ma Theca. 87-84 inception abrupt 2010). et al., 2011). Sandstone petrography, detrital detrital petrography, Sandstone 2011). 2008; Bernhardt 2008;Bernhardt

et al., et et al., 2011, 2012). Both 2008; Crane & & Crane 2008; et al., 2012). The 2012).The et al., et

Accepted Article wells (Fig.wells 3). exploratory available from correlated was horizons seismic of Age in thetext. discussed vertical distances used thefor toof was calculation depth sections, conversion although time (Figs. 5, dataand 6B)previous studies.6A Seismic areillustrated two-ways-time in welldata data seismic oncollected (Figs and 3 and8),based field previously unpublished (Fig. new the 4) four of zone allowed cross sections geology the construction study of serial integrated 1).The (Fig. Chile in Esperanza region the Última Argentina and in Viedma resulted in progradation of fluvial deposits of theSanta Formation resulted Cruz inover of the deposits progradation fluvial and deformation Miocene uplift by created space theaccommodation of infilling Fast (Centinela/Estancia 25 deMayo Parras et al., Formation; &Scasso, 2008; Cuitiño 2010). Miocene a transgression affectingmajor Patagonia, as known (Fig. 2; Manassero, 1988; Malumián Leona Formations Turbio-Río Río of sediments syntectonic Eocene-Oligocene fluvial upper by unconformably/paraconformably followed environments lagoonal and estuarine marine, Romans Bernhardt and (2008) the& allowed deposition western of Aydin channels faultingduring uplift Gonzales and by of active 2009). confinement produced important Recently, indications sedimentary This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This km ~21,000 area of in an units stratigraphic and structures integrates that 3) on aninternationaljournal (Fig. present not published We a detailed geologic previously map SL to 50º30´ 49º30´ FROM STRUCTURE INTEGRATED Patagoniano Natland Natland Tres Formationby the turbiditic Formation Pasos Dorotea and deltaic (Fig. 2; Katz, 1963; represented are latitude this at Formation Toro theCerro of top on packages Progradational were uplift. tectonic channel product the systems of synsedimentary et al., et al., beds et beds (Cuitiño al., 2012). 1974; Macellari 1974; 2009, 2010; Hubbard Hubbard 2009,2010; et al. (2011) to interpret that the bathymetric highs separating that the interpret (2011)to the bathymetric et al., 1989; Armitage Armitage 1989; et al., et al., 2000).The former are cover by marine deposits of of deposits marine by are cover former 2000).The 2009), which are overlain by Paleogene shallow 2009),which shallow are overlainby Paleogene et al.,

2009; 2009; Covault Patagoniano et al., 2 between Lago 2009; 2009; Accepted Article supposedly directed to the west and south from to west the cratonwardsupposedly and during from closure, directed the south its margin Rocas ocean Verdes was2005; et of Ramos, subduction floor Klepeis 2010).The al., (Ghiglione& cover sedimentary the of deformation preceded uplift basement tectonic 1995; et Cunningham, Calderón ofLate al., 2011). Ensuing pulses Cretaceous-Cenozoic 1995; et al., (Kohn craton America South the against west margin its of collision consequent and floor ocean Basin Verdes Rocas theof closure final the of a consequences as time this started duringearly Cretaceous to crystalline domain late structural consolidation of of the thrust and basement 2003;(Fig. 1;Kraemer, 2007). front &Cristallini, Ghiglione Uplift means beltby fold-thrust tothe transferringshortening for responsible the is Fuegian Andes, Domain (i) Basement and western into internalsubdivided domain an (iii) external a (ii) eastern domain. 2012; 3 and thick-skinned Figs and 4):(i)The basement domain, the fold-thrust belt 1998; Kraemer Kraemer, (after east including,structural westregion understudyThe domains to into three from can be divided This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This Tobífera-El of Quemado (Figs synrift 3 and 4).deposits Jurassic ophiolitic northernmost The exposing the Upper grabens rocks Patagonian inverted totally from volcanic batholith, and and plutonic by Tertiary intruded rocks metamorphic Paleozoic-Triassic by constituted craton. America South the of top on Basin Verdes Rocas of margin theoceanward of uplift cratonward ocean of basin closure similar ages and later,both be discussed resulting they experienced they Sarmiento since the to belt, and shortening will Cordillera fold-thrust as both transferred with sector can be correlated a view,the of point Beagle the Canal from mechanical Sarmiento (Fig of Cordillera and in the flank et 4C; 2011). Therefore, Calderón eastern al., 2010) etal., 1995;Klepeis (Cunningham, channel Beagle the along domain the basement recognized within a with basinward vergence system fault and it actually constitutes major The regional basement domain recognized on the western flank of thePatagonian- of western flank the on recognized domain regional basement The In the Lago Viedma - Ultima - basementIn is Esperanza Ultima the Lago domain sector, the thick-skinned Viedma et al., 2002; Ghiglione 2002;

et al., 2009, 2010; Giacosa Giacosa 2010; 2009, et al.,

Accepted Article Fold-thrust belt Grey 3,Fosdick 1991; (Figs 4C, D; Wilson, the hinterlandthe and duplex, Lago as Zapata thrust, thrusts locatedwestTobífera such of over Formation theZapata backthrusts superposing of series a presents domain basement Esperanza depocenters. the region, extensional theIn the eastern boundary of Última indicating inversion total theof deposits, synrift eastward-thinning uplifting Jurassic the there Avellaneda(Fig.3).Inthese sectors Punta arewestward vergingback-thrusts (Kraemer, Río lakes, and Guanaco Argentino western in the of Viedma and in margin 1998) are located inverted depocenters betweenbest to totallyoutcrops, showing partially belteast with thefold thrust 3and Moreno bythe of the 4). thrusts Zapata-Perito (Figs Some to N trend NNE boundingthat an extensional depocenter, represent to the inverted main elongatedthe belt rocks eastern with These (Figs form Upper 3 and 4). Jurassic outcrops a 1 (Figs and4C). Complex the Sarmiento in domain, this within located are Verdes Basin Rocas of remnants This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This et al., et ofthe domain (Ramos, an eastward1989; al., 2002;Giacosa basement Kraemer advance way to and gives narrows progressively internal domain the (Fig.Martin1) San Lago north of A structural zone configurationsimilar while the is recognized (Figs along study 3 and 4), 4, and sheets thin-skinnedin the folds east,(Figs producing 5and thrust external domain 6). Fosdick 4, (Figs internal 5 domain and 6;Kraemer, Ghiglione 1998; western the in rifts Jurassic of inversion tectonic positive partial by primarily dominated outcropping folding,from partially with few thrusts The inverted structures. is structure to deep-marine toNeogene Cretaceous Upper beltexposes Thefold-thrust predominantly It shows 4). and (Figs 2,3 stage basin theforeland from nonmarine strata 2012). Major of the outcrops and ElQuemado Tobífera are Formations concentrated along et al., 2011). Inversion tectonics coexists with a shallow detachment surface to the detachment surface shallow with tectonics coexists a Inversion 2011). et al., 2011).

et al., 2009; Giacosa 2009; Giacosa et al. 2012; 2012; Accepted Article variations in width of this structural domain take place in discrete ~E-W transfer in zones ~E-W take in domain place widthdiscrete this structural variations of ofits place 3and position(Figs shift takes and an 4). westwardalong-strike overallStrong Likerman Likerman (Ghiglione depocenter extensional N-S a of boundary dipping westward a of trace the as interpreted irregulartrace, an has domain this boundary eastern of The and 4). (Figs 3 Turbio between localities theRíoa conspicuous and El monocline frontal Calafate without a backthrust (Fosdick (Fosdick without a backthrust frontal structure the explain interpretations Alternative 7). (Fig. modeling forward kinematic throughout validated was interpretation This 4C-D). (Fig. sequences foreland eastern the of base when its tip-point and dipping reaches backthrust monocline an eastward frontal a of the fault, development induces inverted westwardthethat normal dipping, positively interpret and 4C). We 3 (Figs anticline Toro the of core the on located are level regional to its Formation deposits the of upliftedrespect with that exploratory well,Tobifera showing synrift boundary (Likerman boundary is interpreted as the tectonic inversion of a westward-dipping, eastern boundary awestward-dipping, the inversion of tectonic boundary eastern interpreted of as is eastern The (Figs 3-6). vergence with eastward and folds back-thrusts trending thrusts, 1988; western of the of Harambour, belt sector 2002). This fold-thrust N-S is composed 2002; Fosdick 2002; Fosdick basement outthe thrust metamorphic Toro within Paleozoic (Harambour, fault that soles basement-seated a of presence the showing data in seismic-reflection amplitude reflectors of the structure internal by is the Toro anticline, cored domain westward-dipping, high- reflection seismic data del 5 and region, In (Figs the Torres Paine 6). the frontal main depocenter, bya Jurassic thrust, on represented main of the Simon based the analysis et al. 1999), and a similar configuration is valid in the Última Esperanza region (Soffia region(Soffia Esperanza Última the in valid is configuration similar a and 1999), et al. data betweenand as (Figs Lago Viedma show Lago Argentino 5 and6;Coutandby seismic Internal Domain The (ii) This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This et al., et al., 2013; this work). From north to south, the internal domain increases its width its increases domain internal the south, northto work). From this 2013; 2011) interpreted a inversion 2011) as byproduced tectonic rift of Jurassic the et al., is characterized by partial inversion of Jurassic depocenters depocenters Jurassic of inversion partial by characterized is 2013). The latter proposal is is by Toro latter proposal data 2013).The strengthen 1b drill from et al., 2011), although they do not account for the presence of of thepresence for account not do they 2011), although

et al., 2009; 2009; et al.,

Accepted Article an analog modeling designed to test this hypothesis, creating two rift-segments different with twocreating rift-segments designedtest this to hypothesis, an analog modeling (Ghiglione displacement strike-slip significant withoutinvolving inversion, this geometry duringtectonic map-view degrees extensionwith of would reflecting variables depocenters produce widths different this From thatextensional understanding, beensuggested adjacent conceptual it has 1994; Ghiglione (Kraemer, grabens accommodation zones ancient the separating Jurassic as of surficial extensional expression currently interpreted are zones transfer oriented theeast-west (1989), with Arbe agreement thethe basin. of In extensional phase extensional the of early depocenters from distribution N-S are and 3), structural contrasts being controlled hereinterpretedby these important as (1994, 1998) and Kraemer&Riccardi the (1997) 1 of Lago north (Figs sector for Argentino in lines Fig.3).According to first proposed by Arbe(1989)and an idea by Kraemer followed while 55`LS, thelakes, one located northat ~50º (reddotted of LagoSarmiento southern is andArgentino withViedma coinciding zones northern two the zone, study the recognized in are zones three transfer least (Fig.3).At boundaries thedomain of inflexions showing This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This the of east located and synclines anticlines broad N-S elongated lowamplitude of series are to sequences wedgethrusted Cretaceous thewest over a Upper (Figs 3, 4 5).and A where Maastrichtianzone to that Tertiary domain is developing amonocline, a triangle of (Figs 3 the westernlimit is and 4).The blind stylefront deformation the structural external of eastern Its 5). and 3,4 (Figs the east developed to are withvergence eastward thrusts and thin-skinned folds while a monocline, frontal wedgeforming toPaleogene Lower Cretaceous Marenssi 1997; Riccardi, & Kraemer 1989, 2002; (iii)The External Domain Likerman 3; belt (Fig. fold-thrust on thePatagonian found tothose similar zone, thetransfer occurred near theof model stage thecompressional thrusts during main of separated inposition andlateral zone.width extension by atransfer variation Astrong et al., involving outcrops of Campanian to Paleogene sequences sequences to Campanian of (Arbe Paleogene outcrops involving 2009). Recently, a work from Likerman et al. (2013) produced produced (2013) Likerman etal. work from a 2009).Recently, et al., 2009). et al., 2005), is thrusted westward over a westward over thrusted is 2005),

et al., 2013). 2013). Accepted Article structural sections are in general agreement with previous works (Kraemer, 1998; Giacosa Giacosa (Kraemer, works 1998; previous with general agreement in are sections structural (Figs 4, 5and theprogressively serial ~E-W towards domains andexternal Our 6). internal extensional whileand exhumation of depocenters, decreases inversion exhumation total represents domain basement the boundary of eastern the model, presented In the throughoutrecently analog (Likerman demonstrated experiments was as domain, theinternal of development delineated the rift depocenters Jurassic Upper (Ghiglione time or extension orthogonal duringMesozoic-Cenozoic totheir compression orientation of Jurassic amounts to reactivationPatagonian was array fault The prone under small STRUCTURAL MODEL 6). 5 and structures (Figs shallow Formation and Tobífera of deposits synrift affecting between faults interaction inversion, by 3 the strong monocline as (Figs show and 4)are tectonic by produced This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This region Esperanzain Última (Fosdick the (Kraemer, (~19%–23%) – Viedma lakes between the ~32 1998)and and 40 km Argentino of geometrical restorationspalinspastic (26%) ofretroarc previous shortening indicating 35 km (20%), 29 parameter is Figs in accordance with 4 and7).km of obtained shortening The (compare between and the backthrust theinternal and external domains, resulting monocline the including successfully, mimicked were data and seismic structures superficial The Ferrier – (Fig. Aike Pali 7)using the Cerro Section 4C of forward modeling by tested kinematically was model structural The and their 3and (Figs thrusts boundary 4; Kraemer et al., 2012; Fosdick 2012;Fosdick et al., 2013). Our structural model hinges on the idea that positive inversion of on of hinges Our 2013).the idea positivethat structural inversion model et al., 2011), and point out the lateral continuity of structural domains structural of continuity lateral the out and point 2011), 2D Move 2D et al., softwareMidland (© Ltd). Exploration Valley 2011). 2011). et al., 2002). 2002).

et al., 2013). Accepted Article & Dott, 1979; Hubbard Hubbard Dott, 1979; & (Katz, thick 1963; Winn m up to400 units conglomeratic lenticular with intercalated currents low-density representing turbidity mudstone sandstones and thin-bedded deposition from of composed Formation Toro Cerro the with continues sedimentation region, foreland 1991;Fildani 1979; Dott, Wilson & 2; FormationBarrosa (Fig. Win Punta the of turbiditic sandstones thick m the 250-400 represented is by stage foreland the of the onset indicating infill clastic coarse first the 3) (Fig. region Esperanza Ultima In the Member Asunción of the Anita Formation. Alta between Formation and the Vista the angular unconformities Campanian syntectonic lower Formationand (ii) Toro within theCerro angular unconformities Santonian syntectonic and to lakes, Argentino be theirin two (i) can divided according ages Coniacian- groups: theand data and beltin theregionofViedma across seismic outcrop fold-thrust recognized are sequences from and synkinematic angular unconformities Syntectonic UNCONFORMITIES SYNTECTONIC CRETACEOUS LATE sediments basementonlapping the high sediments generalized we(Fig. 6A).Although propose fault abovethe of Santonian uplift Simon thrustsyntectonic on thickness basement based Kraemer, 1989; Miocene to(Ramos, 1998). of latecalculate around Coniacian 600 m We during was belt, the were shortening intothemaximum deformation fold-thrust migrated Likerman Likerman of Figure 7a from (measured shortening 5% thana less with achieved been have could it the belt the of internalacross duringthe domain fold-thrust inversion Coniacian-Campanian, domain up to Campanian time (Fosdick domain upto Campanian time basement on the mainly concentrated was horizontalshortening lateCretaceous While This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This conglomerates areinterpreted deposits2010). belt as The a low-sinuosity, of channel axial et al., 2013). 2013). et al., 2008; Crane &Lowe, 2008; Crane 2008; Bernhardt et al., 2011; 2011; Calderón

et al., et al., et 2012), subsequent subsequent 2012), et al., 2008). On 2008). On that 2011; Jobe et al.,

Accepted Article outcrops from Toro Esperanza a Cerro outcrops from Formation spans toTuronian in Campanian Ultima Fildani 2; (Fig. lateAlbian-Turonian - Barrosa yieldingPunta range 101 decade, anage for ± from Formation 1.1 to 90.7 ±Ma 2.5 thelast over and sandstones ashes volcanic from zircons of dating U/Pb geochronological these of two intense Winn has Dott,been the agespan 1979). of & subject The units Natland 1966; Scott, 1963; (Katz, toCampanian Cenomanian Formation Cenomanianas to Toro latewas Cerro interpreted the while age, Albian a given was Formation Barrosa Punta Esperanza, the in Ultima content fossil of basis the On between Lakes (Kraemer 1050 and & Riccardi,m 1997). Viedma Argentino Hubbard Dott, 1979; & Esperanzaregion (Winn on theÚltima 2200 m 2000- ca. of thickness a cumulative has formation entire the whereas 1300 m, ca. reaches of SierratheNE slope del At type on Toro (Fig.its locality 3),the Formation Toro Cerro Hubbard Dott, 1979; & detritus (Winn clastic transporting coarse turbiditycurrents for a conduit as thatserved This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This arealso of widespread Pizzio, in the Cerro species 2009). Both upper member Toro steinmanni Inoceramus (Fig.and 3), Argentino Lago of Brazo Sur in Abril de 3 Laguna in located is Formation Toro Cerro from channels ofconglomerate outcrop known northernmost The 1963).(Katz, exposed, not is the formation of the base where Toro Cerro of slope NE On the column. stratigraphical with2) associated by mainly characterized was (1907) by classified and Wilckens Formation, by Hauthal in 1905 content collected At Toro the Cerro fossil the type locality of Bernhardt review from Ma (see 76 ca. youngas as is the south, to km 70 top, theformation whereas Ma) 90–82 (ca. interval Inoceramus steinmanni Inoceramus Inoceramus andinus Inoceramus et al., was recollected on top of the section (Fig. 2; Arbe & Hechem, 1984; Hechem, & Arbe 2; (Fig. section the of top on recollected was 2008). et al., still was encountered on top of a 700-m thick shale section section shale thick 700-m a of on top encountered was still 2012). et al., , covering a range of in , a the manyof covering hundred range meters 2003; Fosdick Fosdick 2003;

et al., et al., Thenorthern 2011). Inoceramus steinmanni Inoceramus 1974; Dott 1974; et al., 2008), and of 2008), of and et al., et 1982; 1982; (Fig. (Fig. Accepted Article channels to the south of Lago Argentino (Fig. 2; Arbe & Hechem, 1984; Kraemer & Riccardi, & 1984;Kraemer Hechem, & Arbe (Fig.2; Lago Argentino of tothesouth channels deep-water conglomeratic of deposition with the contemporaneous is age Santonian late to Coniacian early middle of CT2 upper member The 1997). & Riccardi, (Kraemer Formation a latetoearlybe correlated withindicates the Punta age andcan Albian Coniacian Barrosa content its of CT1 lower member ammonites and inoceramids. The age-diagnostic fossil content and and havean including between lakes the fossil abundant Argentino Viedma outcrop Formation extensively Toro Cerro the of turbidites facies 2002). The 1998; Arbe, FormationToro 2 (Figs and 6A; & Arbe 1984; KraemerHechem, &Riccardi, 1997; Kraemer, unconformityparaconformity laterally the Cerro corresponding and be differentiated in can byan separated sandstones and turbiditic mudstones of composed and CT2 CT1 members MayerRio (Fig. Formation 2;Arbe&Hechem, 1984; Kraemer &Riccardi, 1997). Two FormationCerro ofthe the Campanian Toro overlyingupper Albian-lower thesag deposits and is lakes betweenthe uplift Argentino associated tectonic Viedma with The sequence first Campanian. lower Santonian - upper the to it assigned (1997) & Riccardi Kraemer and lakes Viedma Argentino and the betweenFormation This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This was inversion tectonic under structure whole the of nature the and available, section seismic the portionof eastern the only had authors uplift. These isolated basement Cretaceous byKraemer &Riccardia Late andKraemer (1997) the of (1998),and interpretedas product YPFsections seismic 8124 in Fig.and 8125 This (CoU described unconformity6A). was first inreflectors seismic within Formation seen westward thinning the of Cerro as Toro onlap and bythe evidenced is unconformity angular syntectonic Argentino Coniacian Lago The Toro (i) Cerro ConiacianAngular SyntectonicUnconformity delthe thatfor 1907; Katz,locality Toro Sierra described (Wilckens, 1963). to association fossil similar a 1997), & Riccardi, (Kraemer Viedma Lago of SWshore the on Sphenoceramus cf. lingua 2002). 1997; Riccardi, Inoceramus steinmanni Inoceramus have been found in the upper member of Cerro Toro Formation Toro Formation Cerro of upper member the in been found have associated with associated

Inoceramus andinus, Inoceramus and Accepted Article lines along Lago Viedma (Figs 5A, B). In our view, the syntectonic unconformity is the is unconformity the syntectonic view, B). Inour 5A, (Figs Viedma Lago along lines in seismic be can recognized tectonic inversion of configuration structural similar north, a the west To 7). to (e.g. east Fig. transmittedwas from deformation whole as structure, the of inversion thepositive it represents that deduce we can depocenter (Fig.6A), symmetrical longinverted this of ~30 km theflank eastern in only recognized is the unconformity Although 6A). (Fig. basement of uplift limb thefrontal against disappearance until thins that sediments, onlapping toSantonian Coniacian the upper for thickness 600 calculatem a We (Fig. 3;Kraemer &Riccardi, 1997). Arroyo the paraconformity equivalent on La Sola Section westward be its with can correlated angular this syntectonic between Furthermore the unconformity and Coniacian. earlymiddle in the 6) Fig. (CoU angular unconformity syntectonic age of the CT2, bracketing syntectonic age for Campanian toCT1, andanearly lateSantonian-early Coniacian kinematic middle pre- top of the agefor Coniacian early to early Cenomanian indicated an information (Fig.depocenter 6A).Kraemer (1998) on and based seismic correlation outcrop between inverted rift benotedas Jurassic an can totality it onits considered not visible. When This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This 3; & 2008; Bernhardt Crane Lowe, Ma (Fig. 87 ca. duringtheConiacian area syncline Sillathe in complex channel-lobe oldest the deposition of for thesyntectonic further interpretations supports dataindependently Our deposition. Formation Torotimethe Cerro of the at actives probable structurally controlled paleochannels and areinterpretedhereas sediments, by syntectonic if theywere partially filled as section expression up tolose in that(PPC Fig. seem 6A), faults betweennormal inverted synclines of YPFsmall 8124aretheline alongseismic development important features Other Viedma. Lago probably to up most Argentino, and Lago of shore northern the along whole the internal domain of inversion by tectonic produced uplift theproduct relative of et al., et 2011, 2012). Thinning and disappearance of these of disappearance and Thinning 2012). 2011,

Accepted Article by Coutand within Formation the unconformities Torro Cerro are described equivalent Other syntectonic build-up. levee rather high-relief but syncline, Silla inthe channels of topographic confinement an of with interpretation that align not does data (2011)show et al. andCampion (2004) bypapers Beaubouef Aydin, However, 2008). (Gonzales the& flanking syncline faults thrust controlled primarilydefined by depression inastructurally place the took syncline Silla of units thecoarse-grained of Deposition (Bernhardt high a tectonic by the east to bounded trough ormini-basin narrow toa flows the of confinement reflect thesyncline of limb eastern the along units This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This Campanian sedimentation of Cerro Toro Formation (Coutand (Coutand Formation Toro Cerro of sedimentation Campanian were to showing wall andfaulting that ongoing during Albian hanging folding over anticlines, and condensed sequences in depocenters synclines areassociated with thick footwall faults the (Fig. the position, eastern on i.e. internal domain of boundary Inthis 3). place, reverse sequences including the unconformity are assigned to the the to including unconformity assigned the sequences are onlapping basal (Fig. 6B).The recognized beclearly levels can Santonian-Campanian up to Fuhrthrust, involving Paso Charles bythe produced westward-dipping monocline, reflectors. A of and correlation Fuhr lateral Viñas, 1985) & Charles (Ronchi well the Paso from andostracods foraminifera content of micropaleontologic from was obtained horizons the Paso involvedstratigraphic from Fuhr exploratory wellage of Charles The 6B). (Fig. east located 10 km is reflectors seismic of onlap Another unconformityeastward showing AnitaCampanianAlta Angular Formations Syntectonic / (ii)Unconformity Vista same pre-kinematic sequences, underlying older syntectonic onlapping sequences (Fig. onlapping sequences 6B). underlyingsyntectonic older sequences, same pre-kinematic the andaffects the Charles westward Fuhrwell, Paso located is from A monocline second 1985). &Viñas, (Ronchi Maastrichtian tothe Masiuk, Malumian (1975)and beassigned Campanian-lower of & can et al. (1999) on the northern shore of the Lago Viedma in the same structural in thesame Lago Viedma the of northern shore the on (1999)

Gaudryina healyi Gaudryina et al., 1999). foraminifera zone et al., 2011). 2011). Accepted Article DISCUSSION DISCUSSION 2). (Fig. Teta Cerro the unconformity at age for Campanian (Arbe lower also & Hechem,1984; Campanian Kraemer yielding& Riccardi, 1997), an early are Formation theAnita of lower levels while Campanian lower are Formation Vista the Alta of content, ~30º toSW (Fig.levels upper the dip of average diagnostic 8). fossil According Campanian Member of theAsunción lower AnitaFormation withare clearly an steeper, the of while sandstones overlaying SW, tothe ~10º dip Formation Alta Vista the upper onthe Lago Teta Cerro units (Fig. southern Viedma of of peliticshore Here Campanian 3). on at geometry outcrops the is partially envisaged with asimilar A equivalent unconformity Formation. Toro Cerro of deposition postdating i.e. theunconformity, yields agefor Campanian-early abroad Maastrichtian correlation althoughstructures with associated are synrift deposits Our them not identified. clearly (Fig.basement levels 6B). be These structures can broadly interpreted inversion as appear Both westward-verging tomonoclines of bethe in faults rooted result steep This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This 9). belt (Fig. thrust thefold of domain theinternal boundary of theeastern along located was deformation edge of leading the that shows data while our Conicacian, Campanian-early the during domain thebasement boundary of the eastern Calderon deformation & HesslerCretaceous 2005; to the hinterland(Fildani et 2011; Fosdick al., Patagonian fold-thrust belt of obduction,while thetime restricted Late works at previous difference withmain that on is active ourinterpretation faulting the data support our up sediment sequestered the dipsediment thereached Barrosa Punta before basin. The et al., (2005) by havebeenand Hessler Early Fildani & phases described by Calderon contractile Onset of deformation and inception of Cerro Toro Conglomerates (2007) among others. Fildani(2005) &Hessler propose a partitioned with arc basin et al., 2012). On these previous interpretations the orogenic front is located interpretations located along is the orogenic front Onthese previous 2012).

Accepted Article and deposition of the Sierra thedel Toro and deposition Sierra of channels. time withat the Santa the unconformity onlapping overlap in sequences Cruz onset and river (Bernhardtconglomerates Ma Silla syncline thewith deposition to of ~87 intime 82 Santonian, matching atwould Lago Coniacian- be sediments Argentino onlapping synkinematic unconformity and age span as the for early-middle conservative estimated A constrained Coniacian. be can 1997;Kraemer, 1998), & Riccardi, (Kraemer sequences Santonian synkinematic to orolder and lowerupper separating pre-kinematicConiacian strata Coniacian middle theunconformity of age The and 6A). 2 (Figs Argentino inLago deformation related and inversion graben synsedimentary observed with the time in coincide broadly conglomerates channel betweenToro ca. Ma 84-82 (Bernhardt the Ma, Sierra ca. between 87–82 del of conglomerates and that Silla the syncline age of isotope volcanic coupled with ashes stratigraphy,and sandstones, strontium from bracket EsperanzaÚltima conglomeratic region channels from (Fig. 2). zircons datingU/Pb New of to similar position stratigraphic a Formation (CT2), Toro of Cerro member upper to the Based on astratigraphic at sequences correlation, belong Lago Argentino the synkinematic This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This Kraemer & Riccardi, 1997). from d4 unconformity 9; 2 and inFigs (CoP/CoU FormationToro Cerro from CT2 and CT1 separating hiatus members and surface erosion large-scale a as the north,manifested to discontinuity Lago Argentino with associatedto atleast southward major a is deposition erosion north and of interpretation.bypass This transition from withinconsistent the lowstand (Fig. and not showed eastern that the this are boundbychannels is 3) levees, constructional study the a theory, although such support toevidence yield conclusive didnot (2008) ofthe A recentof analysis Hubbard et beltfrom architectural elements the channel al axial toplatform. introductionchannels theabyssal conglomeratic of eustatically induced, caused (1984) proposed Arbe Hechem or & sea-levellowering,tectonically that a relative et al., 2011). The Campanian-lower Maastrichtian 84-70Ma) TheCampanian-lower(ca. 2011). Maastrichtian et al., 2011). The basal ages for the for ages basal 2011). The

Accepted Article parts of theparts Zapata– under transition, Punta was thrust waybelt Barrosa incipient formation upper the within (Fig.sandstone and shale ash 7)interbedded turbiditic thin-bedded with volcanic of geochronology newU/Pb light of In 2005). Hessler, & (Fildani shortening crustal with to and cordillera restricted conspicuous deformation the basement domain involved thick of (>1 thepredominance of turbidite beds reflects presence a proto sand m) Andean of only levels The grabeninfill. e.g. exposing the thrust theupper-sag along basement front, theTuronian, during place taken have could grabens Jurassic of inversion partial positive the Barrosa FormationPunta argue, 2005). however, (Fildani that &Hessler, initial We of the composition influenced belt fold-thrust thattheAndean confirm data petrographic and early etas al., 101Ma 2011). as (Fosdick not inverted during the Punta Barrosa deposition (Fildanideposition Barrosa Punta during the not inverted in Formation rangeof the grains the grabens implied age that Tobífera wereknown Jurassic (Fildanicomplexes metamorphic Triassic and Paleozoic, Proterozoic, from derived grains zircon containing 2011) represents grained the 50°30´SL, first coarse entering the of sediments basin south The upper Albian-Turonian Punta Barrosa Formation (Fildani Formation Albian-Turonian Punta Barrosa upper The sedimentation onConiacian-Campanian effects A the orogenic andits front advanceof west by theZapata-Upsala(Fig. thrusts 3). the to duplex Tobífera the of the exposure showing 2005) Hessler, & (Fildani content detrital Ma (Calderón 85 to78 from place took deformation emplacement tectonic indeformation Sarmiento, withwhere Cordillera context concordance of ophiolite alocal also a is origin proposed tecto-sedimentary in synorogenic of the conglomerates for context The (1984). & Hechem Arbe from proposal the thatstrengthens channels conglomeratic propose andthe inthe aof We relation uplift domain, onset internal causative between This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This et al., et 2008). Previous the interpreted2008). Previous zircon studies that scarcity of

et al., et al., 2008), altought geochemical geochemical altought 2008), 2003; Fosdick Fosdick 2003; et al., 2012) and et al.,

Accepted Article 2001). Miocene uplift and deformation produced the change from the shallow marine the produced2001). Miocene the uplift anddeformation shallow marine change from exhumation total 30Ma indicating since of a tracks (Thomson fission 9 4 to amount km apatite from data by shown as domain, thebasement of byexhumation accompanied also condition of a major Cenozoic transgression affecting Patagonia, known as as known Patagonia, affecting transgression Cenozoic amajor of condition the basement thrust front since it is the only structure exposing significant outcrops of the the of outcrops significant exposing onlythe structure is it since thrust front the basement to Tobífera input represent a Santonian of The detritus into the of seems reactivation basin (Romans by time Maastrichtian detrital was sediments an important source of Formation Tobífera really to the Santonian to the started during and provide detritus basin an important Miocene an important Miocene (Kraemer, deformational 1998; Fosdick event 3,(Figs 4 orogenic and 6).front ismodern The deformation of leadingedge the present of the position sequences, matches synkinematic Coniacian-Campanian in front registered thrust theorogenic of advance forward The 3 (Figs and 6B). and 6A), theafterward it reaching another Fuhr well Paso of Charles moved 30 km east and 3 (Figs domain theinternal boundaryof the eastern to up basementthe front from km, (Fig. 6B). normal that 50 faults This orogenic means advanced the non-emergent some front eastward dipping of inversion with river Cruz Santa the reaching Campanian, the during ofthe (Figs 3,coast lakes 5 6A). continued its and Compressional advance deformation río west onthe extending and Argentino Guanaco from Lago Viedma, up tothe eastern Lago between rift depocenter a of inversion thepartial produced Coniacian-Santonian the during rift inversion of means by faulting and uplift basement that out data points our hinterland, the to deformation mainly Cretaceous Laterestricted works previous While the Formation Tobífera studyacross zone (Fig. 3). (Fildani sedimentation deep-water of the climax represents Formation Cerro Toro shale-rich The This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This et al., et 2008), where the appearance of grains ca. 160-145 Ma old indicates wherethat theof grains 160-145Maindicates 2008), the appearance ca. old to havereached its position during supposed

et al., 2013), that was that 2013), Patagoniano et al., 2009). 2009). et al.,

Accepted Article it is clearly noticeable that the deposition of conglomeratic channels was confined wasbetween confined channels conglomeratic clearly of that is it noticeable deposition the of theFollowing south the trace eastern boundary the internal domain of Lago Argentino, of Tectono-sedimentary setting Malumián lower et 1999). Oligocene; al., (upper Eocene– deposits fluvial 1991), by theRio Leona andRio and followed Guillermo (Griffin, environments indicating shallow coal with age,beds, Eocene Formation middle of Turbio theRio of sequences syntectonic including conglomerates and terrestrial sandstones of the andMan towards conditions Formations and to Dorotea Aike shallow marine marine marine from the passage involved event deformational Eocene The 2009): al., Lagabrielle et etsedimentation of shallow(see al., conditions thatalso et 1999;Fosdick forced al., 2013) (Malumián deformationalevent Oligocene Eocene–lower amiddle recording 3) Locality (Fig. are ofthe at along the Turbio flank SyntectonicRio unconformities eastern found monocline 2012). (Cuitiño (Centinela towards nonmarineFormation) 2010;Scasso, etal., & conditions Cuitiño This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This trough, were in tectonically deposited a confined althoughnecessarily not axial channels main the that concept The deposition. and conglomerate deformation between relationship a (Fig. strengthcausative to of its actual shape and boundaries 3),gives the idea following belt, thefold-thrust of domain internal present theto confined was channels conglomerate the thethat In syncline. of folding now fact deposition present immediately our of view, east and faulting slope zoneof a developedbehind mini-basin slope local a or Basin Magallanes the eitherzone of an in theSilla axial may mark early syncline the complex channel the western &Lowe channel depositionsystem. of Coniacian Crane interpreted (2008) that Esperanza in Última the duringthe were region active also domain, within internal the et al., Bernhardt and Aydin (2008) & Gonzales Lowe(2008), & Crane interpretation from data and structural constraint and Sedimentological 3). (Fig. domain internal the within anticlines main (2011) indicate that faults located east of the Silla syncline, i.e. a structural position structural i.e. the located a east Silla of (2011)indicatesyncline, that faults

Accepted Article front between Argentino and Viedma lakes advanced around80 lakes and the forward from km between Viedma front Argentino to the data, the possible during state that the presented is it orogenic Coniacian-Campanian, given domain, thebasement to deformation Cretaceous Laterestricted works previous While the (Fig. actual shape domainand boundaries of 3). belt, its fold-thrust following internal tothepresent confined was channels conglomerate of deposition that the fact in a causality see 6A). (Fig. We Lago Argentino at sequences thesynkinematic of deposition entire 4,Simon and Toro active (Figs along its (Fig. trace thrusts 5 was during 3) and 6) boundary represented domain, eastern the the that internal the logical to assume by of Fosdick (20%–23%; Toro toLago 1998) Kraemer, (26%;Viedma Lago ratefrom shortening similar a account into taking and view, of structural point a From 1991). the (Wilson, east to ramp the from topographically to foreland isolated was thatconfined trough an elongate was sedimentation Cretaceous Late to thatmid suggest relationships 2008). Regional (Hubbard contained within narrowed southward abelt that thatdistribution is sediment beenproposed active, Conglomeratehas before. outcrops south Sierra of del Toro show This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This followingparameters configuration an extensionalof withastructural inversion depocenter et al., broad structural as (Likerman shown by bystudy ridges, a submarine valleys divided recent longitudinal formed configuration This channels. axial of distribution and pattern dispersal paleogeographygrabens led to Late the a particular Cretaceous controlled that sediment Jurassic oriented N-S of inversion positive style of structural the described argue that We developed. conglomerates where the setting paleogeographic the magnitude, conditioning lesser with a maybe Argentino lake, of south domain theinternal affected probably also deformation that assume channels. We submarine large axial of inception triggered the somehow uplift orogenic context, this depocenter. In foreland theprevious affecting 4), and 3 (Figs east further and domain internal the boundary of eastern to the thrust front basement 2013). Figure 9 is an oblique view of a sandbox analogue model involving the positive positive the involving analogue model sandbox a of view oblique an is Figure2013). 9

et al., 2011; this work), it is is it work), this 2011; et al.,

Accepted Article affected the internal domain between Viedma affected andthe internal domain between Viedma Argentino producing the lakes, partial during theConiacian-Santonian rift inversion of by means and faulting Basement uplift C- of Lago Argentino, the producing earliersea shallo uplift north continued advancing B- andtopographic Earlyforedeep: thrust faulting Coniacian 9A). (Fig. place Formation took Barrosa thePunta of where deposition depozone developed, foredeep a the orogen from Eastward infill. graben of levels upper-sag thrust onlyduring the the exposing taken e.g. basement the place Turonian, front, along A- grabens of Jurassic have foredeep: AnTuronian inversion could initial partialpositive Fig.9): from to D A (stages stages schematic following the in summarized be can evolution bystep step proposed The geodynamic context. the Coniacian-Campanian customized to proposed was thatillustrate to ofthe Likerman similar those studied region(see This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This with of rates and 80Ma ca. 1–2 fast Campanian) uplift (Santonian-early mm/yr (Calderón the ca. study85 of thezone between constituting that occurred basement domain (Fig. 4C) in atthe Sarmiento with obduction 86Ma Cordillera ophiolite is in coincidence Campanian, the of the uptoConiacian-Santonian front, proposed advance thrust The that lasted Geodynamic Implications unconformityby 9D).the syntectonic (Fig. Campanian rift depocenters of continued duringthe as D- Deformation and inversion shown Campanian depozone(Fig. 9C). wedge-top ina Conglomerates Toro theCerro of the south thrust), encompassing deposition probablyinternal (Toro continued farther domain, the of boundary eastward thrust, the theSimon of Uplift rift depocenter. a of inversion wing in that northern region (Fig. 9B). 9B). (Fig. region northern that in wing et al.,

2013 for a detailed explanation) 2013 for et Accepted Article propagation of the orogenic front. front. theorogenic propagation of thecratonward inducing wedge, taper critical inthe increase an produced domain basement adjacent continental crust occurred Majustadjacent priortocontinental occurred crust ~86 (Klepeis topof Verdes on Basin theRocas of and thrusting inversion basin that show (Fig. 1) Channel Structural on granite data ages zircon from and plutons isotopic neartheU-Pb Beagle to500–600°C between1), Ma took 350°C, place from 90 and70 (Kohn (Fig. del Fuego atTierra domain basement the metamorphic of continuation therepresenting Darwin Cordillera the of cooling and rapid exhumation of episode a first More regionally, together with a ca. 8 km the exhumationwithtogether Sarmiento of ca.(Calderón 8 Complex a km the of advance ~80 orogenic front domain, internal the described km throughout The McAtamney 2005; Hessler, (Fildani& Basin Magallanes the stage in the the foreland of basement domain produced-induced initiation Rocas of Basin and bythe Verdes of thatobduction uplift marked ophiolitic closure al., This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This Anearlier forces. push due toridge stresses compressional intracontinental with the (measured Atlanticopening of Vérard Ocean from in Fig. et 2012), 5 al., in accordance 2008). Saffarana, also 103 MaThe thewith an to periodcoincides acceleration of 84 thatthe the episodically by(Somoza continent overrode and Andeantrench that time of South betweenMa,acceleration America in the and suggesting Late Cretaceous 90 80 10;Vérard Ma (Fig. 84 and the Antarctic Peninsula against Patagonian-F the and western margin its of predicting thecollision reconstructions geodynamic and ocean, ofthe closure Verdesin time with basinRocas the final eventcoincides This deformational deformation. Andean than subsequent wedge theorogenic widening of and uplift of deformational significant in terms the that was implies Cretaceous Late event more 2012) producing an increase in the critical taper wedge. It have been proposed before before proposed been It have wedge. taper critical inthe increase an producing 2012) et al., clearly2012). Itwiththe westward also coincides et al., et uegian Andes(Suarez et al., 2010) between 95 between 2010) Andes(Suarez etal., uegian 2011). We argue that this argue thatthe of uplift 2011). this fast We

et al., 2010). 2010). et al., et al., 1995). 2012), Accepted Article deformational event as the consequence of the Pacific ocean plate’s fast orthogonal fast plate’s ocean thePacific of consequence the as event deformational tectonic Previous the interpretedstudies further north Patagonian Late Cretaceous orogeny. collision-related needed to asignificant produce (Matthews Basin closure Verdes the Rocas driven have al. SHRIMP zircon agefrom yellow the Patagonian Batholith(see in Fig.1, hexagons Hervé 126 arc westto Mathe study of zoneas from shown by U–Pb 75 volcanic subduction-related a of absence the explain (Fig.10) configuration tectonic This opening. accelerated its to due forces push ridge with Atlantic together 2011) al., McAtamney et 2012; al., itself (e.g. building Suarez 1995; etan orogenic Cunningham, process et 2010;Calderón al., of Verdes the western rim Rocas datawas Basin theof Our supports collision idea that the the openingof (Ghiglione high-speed Ocean south al.,Atlantic et 2014). to during the forces against theassociated passive ridge push Aptian margin patagonian between northern and118Ma, ~122 occurred affecting Patagonia deformational event This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This basement present the to deformation Cretaceous Late restricted works previous While 1. CONCLUSIONS building. Andean and mountain closure producing Rocas geodynamic Verdes as Ghiglione, 2008)thatcould havealso factors acted &Ghidella2000; 2005,& 2005;Somoza &Cristallini, Ramos, 2012; Ghiglione 2007; Ramos (Suarez America South against collision or ridge subduction flat-slab subduction, , 2007). A major global plate reorganization that occurred between 105 and 100 Ma, could could Ma, 100 and between 105 occurred that reorganization global plate A major 2007). , rift depocenters the rift depocenters orogenic forming internalnon-emergent front advanced domain. The of inversion the partial produced theConiacian-Campanian during rift inversion of means by and faulting uplift during belt fold-thrust Basement began the Coniacian-Santonian. Andes thePatagonian of deformation initial that show sequences synkinematic domain, et al.,

2012) and provide the force the force provide 2012) and et al.,

et Accepted Article This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This Universidad de Buenos Aires. The authors are grateful to Parques Nacionales de Argentina de Nacionales toParques grateful are authors The Buenos Aires. de Universidad Move license Midlanddata. a for for Valley is Ltd and seismic acknowledged academic wantauthors The Epsur andMisahar of Argentina to wellthank grantingS.A. S.A for access Acknowledgments Cretaceous theLate of the position followed Miocenedeformation and Eocene Later 5. stresses event be compressional to orogenic can related south This Patagonian 4. domain, internal throughoutthe front theorogenic advance of km ~50-80 described The 3. belt of anddeposition fold-thrust inthe between deformation relationship A causative 2. conditions. insedimentary changes studied previously produced and also front, orogenic event. platereorganization global-scale a opening, during accelerated due toits forces push ridge and Atlantic closure, its during Basin Verdes Rocas of western margin the of collision the both combination of the by generated deformational stages. Andean subsequent wedge widening all than in wasorogenic of terms more significant deformational event Cretaceous Late that the implies domain, thebasement of the exhumation with together ridges. by broad submarine valleysdivided structural This longitudinal axial channels. configuration formed pattern and distribution of paleogeography dispersal a particular that theLate controlled sediment Cretaceous led Jurassic oriented N-S of grabens to positive inversion in awedge top-depozone. The place took conglomerates Formation Toro Cerro of deposition context, this In proposed. is systems, Cerro channels Formation contemporaneous Toro axial conglomeratic to the and afterward itanother 30 east. advanced km the 50 domain, thethe uptoboundarybasement front some from km, internal of eastern

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3 55-356 3 arc basin collapse and the and collapse basin arc Sediment. Geol., Geol., Sediment. ., ., 139 43 , 283-298. , 175–187. , 1-117. J. South Am. Earth 3 , 579-600. , 579-600. 265-266 , RICCARDI, A.C.RICCARDI, del (2002) Invertebrados Cretácico Superior. 1173-1306. Córdoba, Ciencias, de Nacional Academia Argentina, Regional Geología de & A.C. Patagónica ROLLERI, II E. Cordillera Austral. (1980) Simposio RICCARDI, Science, Quaternary delFuego, and Tierra of Patagonia LateCenozoic (Ed.), J., In Rabassa, thePatagonian evolutionof Andes. M.C. &GHIGLIONE, (2008)Tectonic V.A. RAMOS, 461-479. ElCalafate.461-479. Argentino, Geológico M.J.). (Ed. Congreso Cruz Haller, de Santa Naturales the Patagonian Andes. in deformation andtopography: Foreland subduction ridge Seismic (2005) V.A. RAMOS, Assoc. Petrol. Geol. Bull Argentina, Basin, Magallanes in Northern structure Foothills (1989) V.A. RAMOS, Gondwana. of with thebreak-up associated in Patagoniathe Antarctic chronology Peninsula: magmatism of and volcanism silicic Episodic (2000) KELLEY,C.M. S.P. & RILEY, FANNING, T.R., R.J., PANKHURST, Argentina. Patagonia, southern boundary Paleogene/Neogene the in across and affinities faunal determinations Ar-date Sr-and on based beds marine of (2008)Correlation MARENSSI, S. PARRAS, A., GRIFFIN,M., FELDMANN,R., CASADÍO, S., SCHWEITZER,C., & Accepted theAndes, Evolution of Magmatic on E.(Eds.), Symposium Andes. Linares, In: H., theAustral Cordani, Patagonian of Article evolution Magmatic (1982) & MUÑÓZ, J. J. SKARMETA, H., V.A.,RAMOS, NIEMEYER, Thesis (unpublished),Cruz. Universidad Bachelor 154pp. de Buenos Aires, Abril,Santa de de lalaguna3 de M.F.yPIZZIO, la región (2009) Estratigrafía estructura This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This 11 J. South Am. South J. Sci. Earth Tectonophysics , Elsevier, pp. 57- 71. 71. pp.57- Elsevier, , ., 73 , 887– 903. 903. 887– , Earth Sci. Review Sci. Earth , 399 J. Petrol., J. , 73-86. , 26 , 204-216. , 204-216. , 18 41 , 411 – 443. 443. – , 411 , 605–625. , 605–625.

In Geología y Recursos y Geología Recursos Developments in in Developments 15 , Relatorio: , Relatorio: Am. SOMOZA, R. & GHIDELLA, M.E. (2012)Late Cretaceous to recent plate motions in to platemotions M.E. recent Cretaceous GHIDELLA, SOMOZA, R. (2012)Late & western South America revisited. America South western Accepted Arg Geol. y Aluk. Farallon Nazca, de Subducción el Cenozoico: durante delsur América SOMOZA, R.GHIDELLA, & M.E. (2005) Co 22, v.Serie 36. p. 39, Comunicaciones de Chile, Universidad yMatematicas, Fisicas deCiencias Facultad Magallanes, Chile: Departamento deGeologia, Esperanza, de Ultima y plegado fallado C.,SOFFIA, P. HARAMBOUR, &SALVADOR, enelcinturon Estructuras (1988) S. Servicio de Santiago. yMinería, Nacional Digital. Geología Geológica digital.Publicación de Chile: versión Geológico MapaSERNAGEOMIN, 2003. southern Andes, Patagonian Chile sequence, Flysch Cretaceous a of pattern dispersal and Sedimentology K.M.(1966) SCOTT, Article Chile Basin, GRAHAM, Deep-Water (2011)Evolution Stratigraphic Of S.A. Architecture,Magallanes ROMANS, B.W., FILDANI, A., HUBBARD, S.M., COVAULT, J.A., FOSDICK, J.C. & Res., Chile (50º-52ºS). basin, theCretaceousMagallanes of analysis provenance basin: foreland aretroarc of sedimentaryfill on basin history predecessor Importance of (2009) ROMANS,B.W., FILDANI, A.,GRAHAM, S. Fiscales, Buenos 87 pp. Aires, Petrolíferos Yacimientos Cruz), Inedit report, deSanta Fuhr,YPF.SCA.PFu.es-1 Provincia (Paso del pozo Micropaleontológico (1985)Estudio D.I.& F. RONCHI, VIÑAS, This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This 19 pp. 10.1111/j.1365-2117.2009.00443.x doi: ., ., 60 .Mar. Petrol.Geol. , 797–809. 797–809. , 28 Earth Planet. Sci. Lett Sci. Earth Planet. , 612-628. .Am. Petrol. Assoc. Geol. Bull A., HUBBARDZ, S.M.COVAULT, & J.A. nvergencia en el margen occidental de nvergencia de occidental enel margen ., 331–332

, 152–163. 152–163. , ., 50 Rev. Asoc. , 72-107. Basin Petrol. Geol. Mem Geol. Petrol. Atlantic margins. North the stratigraphy of and deformation Extensional (Eds), H.R. Balkwill, A.J., In: Tankard, basins. sedimentary argentine of formation M.A.,ULIANA, and K.T. BIDDLE, the & CERDÁN, extension J. (1989)Mesozoic subduction processes. processes. subduction diferent toits correlation and Chile) (southernAndes thePatagonian of history denudation Mesozoic-Cenozoic The B.(2001) STOCKHERT, F. & S.N., HERVE, THOMSON, Bull. zone. fault Liquine-Ofqui intra-arc transpressional the from results 46°S: an appraisal 42°S based on and latitudes Andes betweenfission-track Patagonian and THOMSON, N. the evolution (2002) S. tectonic geomorphic Late Cenozoic of Chile. Province, Magallanes exploration in petroleum and (1949) Geology R. C. THOMAS, Gondwana. segmentation in southwestern slab A.(2010)Cretaceous DEMANT, M.,& R., BELL, LACRUZ, SUÁREZ, M., DE belt and thrust Patagonian along the fold deformation andoriginof (2000) Timing C.M. R. &BELL, LACRUZ, SUAREZ, M., DE Publications 218, 1–19. History.Society, Special London, Geological Earth in Ophiolites P.T., (Eds) Robinson, Y., Dilek, In: basin. back-arc margin continental in a crust oceanic-type development on of stages progressive of America: remnants STERN, C.R. &DE M.J. Verdes ophiolites, South southernmost WITT, (2003)Rocas Accepted ArticleLett Sci. Planet. cordillera. theAndean birthof the and hotspots theAtlantic of America, motion SOMOZA, Mi &ZAFARANA,C.B. R. (2008) This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This , 114 Am. Assoc. Petrol. Geol. Bull Geol. Petrol. Am.Assoc. , 1159–1173. ., 271 ., 46 , 267-277. 267-277. , , 599–614. , 599–614. Tectonics , 20 ., 33 , 693-711. , 693-711. , 1553-1578. , 1553-1578. . Geol. Mag . Geol. Geol. Mag d-Cretaceous polar standstill of South of d-Cretaceous polar standstill ., ., ., ., 137 147 , 345–353. 345–353. , , 193-205.

Geol. Soc. Am. Am. Assoc. Earth Cretaceous age, southern Cretaceous Chile. late of Deep-water (1979) conglomerates R.H. &DOTT,R.D. fan-channel WINN, Chile. theUltima-Esperanza-District, Record from -Stratigraphic Andes Southernmost (1991) WILSON, T.J. TransitionBack-Arc from to Foreland in Development the Basin Ber. Naturforsch. Ges. Freiburg Ber. (Sudpatagonien).Esperanza Ultima de Seno dem und LagoArgentino dem zwischen Gebietes des Skizze Geologischer Hauthals zu R. Erlauterungen (1907) O. WILCKENS, America–Antarctica South plate system. VÉRARD, C., FLORES, K.&STAMPFLI, reconstructions (2012)Geodynamic G. of the the Austral Basin. of evolution the with relationship its Patagonia, Argentina: Formation, Amarilla Southern AcceptedFIGURES ArticleHOFFMANN, S. & N., J. GELFO, J., F. GOIN, A., GERDES, T., MARTIN, G., D. POIRÉ, N., A. VARELA, information in kilometers are from Heine (2007) at (2007) Heine from are kilometers in information seismic from depocenters undeformed the within thickness sediment foreland al., Farr (SRTM; data Mission Topography (NASA)ShuttleRadar Administration and Space Aeronautics National processed from projection) Mercator (DEM; 1: Fig. This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This 126 to 75 Ma U–Pb SHRIMP zircon age for the Patagonian Batholith from Hervé Hervé from Batholith thePatagonian for age zircon SHRIMP U–Pb Ma 75 to 126 of distribution show hexagons Yellow not represented. is information outcrop 2007) showing sediment distribution from Austral basin. Contours indicate indicate Contours basin. Austral from distribution sediment showing 2007) Geol. Soc. Am. Bull Soc. Geol. Location of the study zone from high-resolution digital elevation model model digital the high-resolution elevation of Location studyzone from (2012). (2012). Andean Geology ., U-Pb zircon constraints on the age of the Cretaceous Mata onthe of theCretaceous zircon age constraints U-Pb 103 , 98-111. , 15 Sedimentology , , 22 p. p. , 22 39 , 359-379. , 359-379. J. Geodynamics, J. Geodynamics, , 26 , 203-228. , 203-228. 53

, 43– 60. 60. , 43– www.basinatlas.com et et ; Accepted Article et al., Malumián (1998); Kraemer (1991); Wilson (2003); SERNAGEOMIN on and data, 3: Fig. www.stratigraphy.org. (2013), ICS - Stratigraphy on Commission theInternational from is scale Time BuenosAires. of University CPBA,Paleontology Collection, Repository: (CPBA 20990.1). Specimenswhitened with ammonium chloride. Scalebar 1 cm. Laguna 3 de view inlateral from Abril mould external (CPBA 8061), Right, Formation Toro Cerro (1905), Hauthal of collection original CerroSolitario, from steinmanni angular unconformity; CoP: Coniacian Paraconformity; Paraconformity; Coniacian CoP: unconformity; angular syntectonic Coniacian CoU: unconformity; angular syntectonic Campanian and Bernhardt (1989) et Macellari al. is after profiles both between Lateral correlation Riccardi (1997). & Kraemer after modified lakes and Viedma Argentino between to sector correspond Right column therein. references and et al.(2011) Fosdick from sectors RíoTurbio and Esperanza Última of column isrepresentative Left correlation. their and Argentino Top: 2: Fig. Junction. Triple et al. This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This location. for 1 Fig. See (2007). al. et Hubbard from modified channels (2007). FTB – fold-thrust belt; RVB – Rocas Verdes Marginal Basin; TJ: TJ: RVB – Marginal – belt; Basin; Rocas FTB Verdes (2007). fold-thrust (2000); Gonzalez & Aydin (2008); Fosdick Fosdick Aydin (2008); & Gonzalez (2000); Integrated geological map of the study zone, based on collected field field on collected based zone, the study of map geological Integrated Wilckens. Left, specimen with partially preserved shell in lateral view view inlateral shell preserved with partially specimen Left, Wilckens. Simplified stratigraphic columns from north and south of Lago Lago of south northand from columns stratigraphic Simplified

et al., (2011). Deep Water Deep (2011). Water Bottom: et al., (2012). CaU: Inoceramus Accepted Article Ltd). Exploration Valley Midland copyright (© software 7 Fig. location 3for Fig. See (1998). andKraemer Riccardi& (1997) Kraemer after intervals Stratigraphic Formation. Mayer RMY:Río probable paleochannel; PPC: boundary; Cretaceous-Tertiary KTB: boundary; Jurassic-Cretaceous JKB: Formation; El Quemado ELQ: Paraconformity; CoP: Coniacian unconformity; angular syntectonic Coniacian CoU: unconformity; angular CaU: syntectonic Campanian CT: Toro Cerro Formacion; Formation; Vista Alta AV: Formation; Anita An: are: horizons Seismic text). wells (see exploratory available from was correlated horizons seismic Age of Formation. the Anita and Formation Vista Alta the between unconformities Campanian early river showing domain. the of internal boundary the northern along Formation Toro Cerro the within unconformity angular syntectonic Santonian aConiacian- showing LagoArgentino, of the shore linenorthern Seismic from Fig. 6 Fig. 3 location. for Fig. See Río Mayer RM: Formation. Formation; Quemado El EQ: Formacion; Toro Cerro CT: Formation; Vista Alta AV: Formation; Anita An: horizonsare: Seismic oftectonic inversion. influence conspicuous 5 Fig. (2012). al. et Calderón after ismodified 4C Section from sector 4: Fig. This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This : Forward kinematic modeling for section 4C constructed with the with constructed 4C section for modeling kinematic : Forward : Seismic time sections. : Seismic time sections showing syntectonic angular unconformities. unconformities. angular syntectonic showing time sections Seismic : Structural cross sections. See Fig. 3 for locations.Cordillera Sarmiento Sarmiento locations.Cordillera for 3 Fig. sections. See cross Structural . A-B: Profiles across the fold-thrust belt showing belt showing across the fold-thrust Profiles B: Seismic line along the Santa Cruz Cruz Santa the linealong Seismic

2D Move

A: A: Accepted Article convergence of Pacific ocenic plates is from Somoza & Ghidella (2012). (2012). Ghidella & Somoza isfrom ocenic plates Pacific of convergence Modifed from Vérard Verdes Basin; CDF:Canal Darwin faultmapped from Glasser& Ghiglione, 2009. Rocas RV: of shortening. transfer cratonward throughout front the orogenic of migration and forward uplift basement strong produced margin itswestern of uplift. basement initialwith coincident closure, geodynamic context of the study zone. study the of context geodynamic 10 Fig. discussion. for text See conglomerates. Toro Cero of deposition the for context geodynamic proposed showing reconstructions paleogeographic Campanian to Turonian 9 Fig. unconformity. angular syntectonic Campanian CaU: alsolowerCampanian. SW, ~30º of dip average an with Formation Anita thelower of Member Asunción the constitute thehill of on top sandtones overlaying while SW, to and dips ~5-10º the Alta Vista Formation upper lower Campanian to the hillbelogs of bottom the at crest Sandstone theSE. to islooking photograph 8: Fig. This article is protected by copyright. All rights reserved. rights All byprotected copyright. is article This Angular unconformity at Cerro Teta, on the southern shore of Lago Viedma, Lago Viedma, of shore the southern on Teta, Cerro at unconformity Angular : Top: : Paleotectonic reconstruction showing the changing regional regional the showing changing reconstruction : Paleotectonic Proposed Coniacian-Campanian geodynamic context. context. geodynamic Coniacian-Campanian Proposed et al. et (2012) and Suarez et al. (2010). Distribution and and Distribution (2010). al. et Suarez and (2012) A: Final stages of Rocas Verdes basin basin Rocas of Verdes stages Final B: Basin closure trough collision collision trough Basin closure

A to D

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