Miravete Anticline, Maestrat Basin, Spain

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Received: 14 October 2019 | Revised: 2 March 2020 | Accepted: 6 March 2020 DOI: 10.1111/bre.12447

EAGE ORIGINAL ARTICLE

Tectono-sedimentary evolution of Jurassic–Cretaceous diapiric structures: Miravete anticline, Maestrat Basin, Spain

1Group of Dynamics of the Lithosphere (GDL), Institute of Earth Sciences Jaume Abstract Almera, ICTJA-CSIC, Barcelona, Spain Integration of extensive fieldwork, remote sensing mapping and 3D models from 2Independent Geologist, Bordeaux, France high-quality drone photographs relates tectonics and sedimentation to define the 3 Department of Environmental Earth Jurassic–early Albian diapiric evolution of the N–S Miravete anticline, the NW-SE Science, Eastern Connecticut State Castel de Cabra anticline and the NW-SE Cañada Vellida ridge in the Maestrat Basin University, Willimantic, CT, USA 4CGG Robertson. Tynycoed, Llanrhos, (Iberian Ranges, Spain). The pre shortening diapiric structures are defined by well- Llandudno, UK exposed and unambiguous halokinetic geometries such as hooks and flaps, salt walls 5Departament de Mineralogia, Petrologia and collapse normal faults. These were developed on Triassic salt-bearing deposits, i Geologia Aplicada, Universitat de previously misinterpreted because they were hidden and overprinted by the Alpine Barcelona, Barcelona, Spain 6 shortening. The Miravete anticline grew during the Jurassic and Early Cretaceous EQUINOR ASA, International Offshore Exploration, Brazil, Fornebu, Norway and was rejuvenated during Cenozoic shortening. Its evolution is separated into four 7EQUINOR ASA, Exploration Research, halokinetic stages, including the latest Alpine compression. Regionally, the well-ex- Fornebu, Norway posed Castel de Cabra salt anticline and Cañada Vellida salt wall confirm the wide- 8 EQUINOR ASA, Exploration Regional & spread Jurassic and Early Cretaceous diapiric evolution of the Maestrat Basin. The Access, Houston, TX, USA 9 NE flank of the Cañada Vellida salt wall is characterized by hook patterns and by a EQUINOR ASA, Research Center, Bergen, Norway 500-m-long thin Upper Jurassic carbonates defining an upturned flap, inferred as the roof of the salt wall before NE-directed salt extrusion. A regional E-W cross sec- Correspondence Jaume Vergés, Group of Dynamics of the tion through the Ababuj, Miravete and Cañada-Benatanduz anticlines shows typical Lithosphere, Institute of Earth Sciences geometries of salt-related rift basins, partly decoupled from basement faults. These Jaume Almera, ICTJA-CSIC, Lluís Solé i structures could form a broader diapiric region still to be investigated. In this section, Sabarís s/n, 08028 Barcelona, Spain. Email: [email protected] the Camarillas and Fortanete minibasins displayed well-developed bowl geometries at the onset of shortening. The most active period of diapiric growth in the Maestrat Funding information Basin occurred during the Early Cretaceous, which is also recorded in the Eastern Generalitat de Catalunya, Grant/Award Number: AGAUR 2017 SGR 847; Spanish Betics, Asturias and Basque-Cantabrian basins. This period coincides with the peak Ministry of Economy and Competitiveness, of eastward drift of the Iberian microplate, with speeds of 20 mm/year. The transten- Grant/Award Number: ALPIMED (PIE- sional regime is interpreted to have played a role in diapiric development. CSIC-201530E082) and SUBTETIS (PIE-CSIC-201830E039); EQUINOR ASA Research Center, Bergen

The peer review history for this article is available at https://publons.com/publon/10.1111/bre.12447

This is an open access article under the terms of the Creative Commons Attribution License, which permits use, distribution and reproduction in any medium, provided the original work is properly cited. © 2020 The Authors. Basin Research published by International Association of Sedimentologists and European Association of Geoscientists and Engineers and John Wiley & Sons Ltd.

wileyonlinelibrary.com/journal/bre | 1653 Basin Research. 2020;32:1653–1684. 1654 VERGÉS et al. | EAGE

KEYWORDS Iberian Ranges, Jurassic–Early Cretaceous halokinetic depositional sequences, Maestrat Basin, Miravete salt anticline, salt walls, salt-welds, Triassic diapirism

1 | INTRODUCTION Highlights In the decades preceding the 1980s, salt tectonic interpretations • The Miravete anticline grew for tens of millions were commonly invoked in many fold and thrust belts world- of years during the Jurassic and Early Cretaceous wide, in which large masses of salt-bearing rocks disrupted the periods. regional tectonic grain. These regional studies resulted in the • Peak diapirism began in Hettangian-Barremian compilation of salt tectonic activity within the Tethys realm ages with coeval western diapir flank collapse and (reviews in Hudec & Jackson, 2007; Letouzey et al., 1995). salt extrusion. The overwhelming application of thrust tectonic geometries • Early Aptian W-prograding carbonate platforms and kinematics in fold and thrust belts beginning in the 1980s might relate to the N-S growth of the Miravete salt (examples in McClay, 1992; McClay and Price, 1981) modi- wall. fied previous interpretations of diapirism, but emphasized the • Upturned flap in Cañada-Vellida salt wall con- influence of salt detachments (pre- and syn-compression) as firms the diapiric history of the Maestrat Basin. essential elements of the geometry of thrust systems. • Early Cretaceous increase of Iberia eastward drift Extensive interpretation of excellent quality seismic could trigger diapirism in many of Iberian rifted lines from salt-influenced continental margins mostly basins. along the North Sea, Gulf of Mexico, Brazil and Angola (Davison et al., 2000; Stewart & Coward, 1995), studies of exceptional field examples (e.g. La Popa Basin in Mexico; Giles & Lawton, 2002; Giles & Rowan, 2012) and pro- fuse analogue modelling (e.g. Brun & Fort, 2011; Jackson indicated by red circles in Figure 1 and discussed in Vergés & Vendeville, 1994; Vendeville & Jackson, 1992) have et al. (2019). These include the Basque-Cantabrian Basin demonstrated the importance of salt tectonics in fold and (1–4: Bodego & Agirrezabala, 2013; López-Horgue et al., thrust belts, and constitute the basis of a solid geometric 2010; Poprawski et al., 2014; Poprawski, Basile, Jaillard, and kinematic compendium of salt-related tectonics that Gaudin, & Lopez, 2016; Quintà, Tavani, & Roca, 2012), can be applied elsewhere (e.g. Jackson & Hudec, 2017; the Pyrenees (5–9: Canérot, Hudec, & Rockenbauch, 2005; Soto, Flinch, & Tari, 2017). Jammes, Tiberi, & Manatschal, 2010; Lopez-Mir, Anton The Mesozoic domains of the Iberian plate contain Muñoz, & García Senz, 2014; McClay, Muñoz, & García- large outcrops of Upper Triassic salt-bearing deposits (e.g. Senz, 2004; Saura, Ardèvol i Oró, Teixell, & Vergés, Escavy, Herrero, & Arribas, 2012; Ortí, Pérez-López, & 2016), the Iberian Range (10: Canérot, 1991), the Betics Salvany, 2017; Rodríguez-Fernández & Oliveira, 2014), (11–16: Escosa, Roca, & Ferrer, 2018; Martínez del Olmo a number of which were interpreted as diapiric. Recently, et al., 2015; Pedrera, Marín-Lechado, Galindo-Zaldívar, an increasing number of salt-related structures were re- & García-Lobón, 2014; Soto et al., 2017; Soto & Flinch, interpreted in the various Iberian fold and thrust belts as 2017), the Algarve Basin (17, 18: Ramos, Fernández,

FIGURE 1 (a) Pre-breakup reconstruction of Pangea in the Early Triassic (modified from Lawver, Dalziel, Norton, & Gahagan, 2009; Moulin, Aslanian, & Unternehr, 2010). (b) Late Triassic palaeogeographic map of the western Neotethys area (modified from Dercourt, Gaetani, & Vrielynck, 2000; Martin-Rojas et al., 2009; Ortí et al., 2017). (c) Simplified geological map of Iberia with position of the Maestrat Basin and location of the main salt diapirs growing during the Mesozoic with most recent references (red circles). 1: Laredo and Pondra diapirs (López- Horgue et al., 2010); 2: Poza de la Sal diapir (Quintà et al., 2012); 3: Bakio diapir (Poprawski et al., 2014, 2016); 4: Lasarte sub-basin salt controlled basin (Bodego & Agirrezabala, 2013; Bodego, Iriarte, López-Horgue, & Álvarez, 2018); 5–7: Gaujacq and Ossun diapirs (Canérot et al., 2005); 6: Mauléon basin diapirs (Jammes et al., 2010); 8: Cotiella extensional salt area (McClay et al., 2004); 9: Sopeira and Sant Gervàs diapirs (Saura et al., 2016); 10: Villahermosa del Rio diapir (Canérot, 1991); 11: Parcent diapir (Pedrera et al., 2014); 12: Altea diapir (Pedrera et al., 2014; Martínez del Olmo et al., 2015); 13, 14: Finestrat and Elda diapirs (Martínez del Olmo et al., 2015); 15: Jumilla diapirs (Escosa et al., 2018); 16: Western Betics (Soto & Flinch, 2017); 17, 18: Faro and Albuferia diapirs (Ramos et al., 2016); 19, 20: Santa Cruz and Caldas da Rainha diapirs (Alves et al., 2003; Pena do Reis et al., 2017). Iberian Range AB: Aragoneses Branch; Iberian Range CB: Castillan Branch; PB: Parentis Basin; AB: Asturian Basin; AP: As Pontes Basin; ALZ: Asturoccidental-Leonese Zone; CZ: Cantabric Zone; CM: Cantabrian Mountain; CS: Central System; CCR: Catalan Coastal Range; GB: Guadalquivir Basin VERGÉS et al. 1655 EAGE |

A (a) (b) Irish

B A L T I C A N G A R Porcupine Massif A A L A U R E N T I Bank Flemish W D N O G T E T H Y Cap Armorican Massif S Grand Bay of Biscay rift Central A Banks N Iberian Massif Massif A Moroccan Ebro basin Meseta IberianCatalan basin basin Emerged areas Siliciclastic Maghrebian-Gibraltar Adria Mainly evaporites Evaporites and clastic

Evaporites and carbonate Rift Shallow platforms (c) –8º –6º –4º –2º0º2º PB AB 5 1 3 4 AP 7 PYRENEES CZ 43º 2 6 ALZ CM 8 9

DUERO AB IB EBRO E RIAN 41º R CCR IBERIAN . MASSIF Valencia Trough CS CB TAJO 10 Figure 2 20 A 19 Central Iberian Zone Maestrat Basin 39º 11 15 12 Ossa Morena Z External 13 14

S. Portuguese Z MEDITERRANEAN SEA

GB BETICS 37º 18 17 16 Internal

ATLANTIC OCEAN Alboran Sea

Iberian MassifNCenozoic Mountain ranges Foreland basins eogene basins Triassic evaporites Pyrenees basement Internal Betics Basement

Terrinha, & Muñoz, 2016) and the Lusitanian basin (19, The Iberian Range formed from the inversion of the 20: Alves, Gawthorpe, Hunt, & Monteiro, 2003; Peno dos Mesozoic Maestrat intraplate rift basin (e.g. Guimerà, Mas, Reis, et al. 2017). & Alonso, 2004; Salas & Casas, 1993), in which widespread 1656 VERGÉS et al. | EAGE unconformities within the Jurassic and Lower Cretaceous to other nearby structures where we collected additional data successions were traditionally interpreted in terms of syn-rift that confirmed the fundamental role of salt movement prior to post-rift differential subsidence between fault-bounded tec- to the onset of Alpine contraction (Castel de Cabra salt anti- tonic domains (Aurell et al., 1992; Campos, Aurell, & Casas, cline and Cañada Vellida and Pancrudo salt walls, Figure 2). 1996; Guimerà, 1988; Liesa, Soria, Meléndez, & Meléndez, These additional studies corroborate that the Maestrat Basin 2006; Roca & Guimerà, 1992; Roca, Guimerà, & Salas, 1994; in the southeastern Iberian Range is a newly identified diapiric San Román & Aurell, 1992). The only previously documented province. In this region we identify masked halokinetic struc- examples of halokinesis within the Maestrat Basin are a di- tures of early diapirism that influenced the local deposition, apir located in the Penyagolosa block near Villahermosa del but were then significantly overprinted by later contraction. Río village and in Lucena del Cid, north of Castelló (Canérot, Nevertheless, this study is particularly restricted to the Jurassic 1989, 1991; Trell, Canérot, & Martín, 1979) (see location in and Early Cretaceous evolution of diapiric structures in the an- Figure 1). However, in a recent reappraisal of seismic and alysed region well before Alpine compression. well data of the Maestrat Basin, Nebot and Guimerà (2016a, 2016b) clearly document the migration of Middle Triassic salt as a consequence of a Cenozoic detachment, promoting 2 | GEOLOGICAL SETTING: THE the development of salt pillows in the subsurface. MAESTRAT BASIN In this contribution, we explore the hypothesis that Triassic salt-bearing layers of the Maestrat Basin flowed soon after The NW-SE trending Iberian Range is interpreted as an their deposition producing diapirism, well before the Late intraplate chain resulting from the Alpine inversion of the Cretaceous onset of regional contraction (e.g. Macchiavelli Late Permian to Mesozoic NW-SE Iberian rift system and et al., 2017; Martín-Chivelet & Chacón, 2007). We focused of the nearly coeval NE-SW Catalan rift system (Guimerà, our study on the vicinity of the Miravete anticline, a N–S Rivero, Salas, & Casas, 2016; Salas & Casas, 1993; Salas trending structure, that has been classically interpreted as a et al., 2001). The Iberian Range comprises the northeastern fold related to the Cenozoic compression despite its trend Aragonese branch and the southwestern Castilian branch, subparallel to the direction of tectonic shortening (Simón, predominantly containing Cretaceous and Jurassic depocen- 2004). This region of the Maestrat Basin, especially to the tres respectively (Figure 1). The Aragonese branch is con- north of the Miravete anticline, has very complex fold pat- nected with the almost orthogonal Catalan Coastal Ranges, terns composed of sets of anticlines and synclines with dif- whereas the Castilian branch is linked to the NE domain of ferent and sometimes orthogonal trends that were interpreted the External Betics. as superposed buckle folds (Simón, 2004). However, in the The Late Permian to Mesozoic extensional Iberian sys- Miravete region, Triassic rocks form long and narrow out- tem is a failed rift, which reactivated the previous Hercynian crops along anticline axes or rectilinear faults trending either tectonic grain and formed during the opening of the Central NW-SE or N-S. These salt-bearing rocks are associated with and North Atlantic basins in the early stages of the break-up Jurassic and Lower Cretaceous depositional sequences char- of Pangea (e.g. Quesada and Oliveira, 2020; Salas et al., acterized by multiple intraformational unconformities, sedi- 2001; Stampfli & Borel, 2002). The Betic and Catalan rift mentary wedges, complex facies patterns, stratal onlaps and systems formed along a roughly NE-SW trend during the de- outward progradation of carbonate platform systems, usually velopment of the Ligurian-Tethys oceanic basins (e.g. Galán- associated with rifting. In the Miravete anticline, the high Abellán et al., 2013; Schettino & Turco, 2011). The evolution quality and continuous exposure of this fold led to the publi- of the Iberian Rift was characterized by two main extensional cation of numerous stratigraphic studies that are used to build stages: Late Permian to Late Triassic and late Oxfordian a detailed thickness, facies and age interpretations providing to late Albian according to numerous studies (e.g. Capote, a very detailed framework for our study (Bover-Arnal et al., Muñoz, Simón, Liesa, & Arlegui, 2002; Salas et al., 2001; 2010; Bover-Arnal, Pascual-Cebrian, Skelton, Gili, & Salas, Vargas et al., 2009). During the first rift stage, Upper Permian 2015; Embry et al., 2010; Garcia et al., 2014; Meléndez, Liesa, continental deposits and Triassic strata of typical Germanic Soria, & Meléndez, 2009; Navarrete et al., 2014; Navarrete, facies accumulated in approximately NW-SE trending fault- Rodríguez-López, Liesa, Soria, & Veloso, 2013; Peropadre, bounded depressions (Arche & López-Gómez, 1999, 2005; Liesa, & Meléndez, 2013; Vennin & Aurell, 2001). Benito, 2005). These deposits include two principal Triassic We established the interplay between tectonics and sedimen- salt layers, one in the middle Muschelkalk unit and another in tation in the Miravete salt anticline (Figure 2) through numerous the Keuper unit (Nebot & Guimerà, 2016; Ortí et al., 2017). field campaigns (mostly during years 2015 and 2016), remote After the first rifting stage, Jurassic shallow-water platforms sensing and high-quality photography to build drone-derived developed in an epeiric sea that connected southwards to the virtual outcrop models. Once the contributions of halokinesis Tethys oceanic domain (Alnazghah, Bádenas, Pomar, Aurell, in Miravete anticline were established, we extended the study & Morsilli, 2013; Aurell, Bádenas, Ipas, & Ramajo, 2010; VERGÉS et al. 1657 EAGE |

Castel de Cabra Ejulve Las Parras Escucha de Martín La Zoma

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Keuper salt-bearing red clays (locally Quaternary Paleocene to Early Cretaceous Middle Jurassic Late Oligocene with embedded Muschelkalk rocks)

Late Oligocene Late Cretaceous Basement rocks to Miocene Late Jurassic Early Jurassic Tectonic features anticline axis syncline axis thrust inferred salt structure possible salt weld

FIGURE 2 Geological map of the study area made using remote sensing mapping (for the Masías de Ejulve, Castel de Cabra, Miravete and Cañada Vellida areas) combined with 1:50.000 IGME Magna geologic maps of Argente (Martín & Canérot, 1977), Montalbán (Canérot et al., 1977), Alfambra (Olivé et al., 1981) and Villarluengo (Gautier, 1979) and the map published in Simón and Liesa (2011)

Bádenas & Aurell, 2001; Dercourt, Ricou, & Vrielynck, Albian ages during the Late Jurassic–Early Cretaceous exten- 1993; Gómez & Fernández-López, 2006). A second rifting sion of the Maestrat Basin. stage occurred from Late Jurassic to Early Cretaceous, co- This study focused on the western Maestrat Basin eval with the opening of the southern segment of the North (Figure 2), which is limited to the south by NW–SE Iberian- Atlantic, between Iberia and Newfoundland, and the opening trending normal faults, and to the north by a system of ap- of the Bay of Biscay (Alvaro, Capote, & Vegas, 1979; Capote proximately E–W south dipping normal faults (Nebot & et al., 2002; Salas & Casas, 1993; Van Wees, Arche, Beijdorff, Guimerà, 2016; Salas et al., 2001). The position and orien- López-Gómez, & Cloetingh, 1998). During this second rift- tation of these basin-bounding structures, and that of sub- ing stage the Jurassic carbonate platforms were broken-up sidiary faults within the basin, controlled the thickness of and newly formed faults defined individual basins, namely Cretaceous deposits (Liesa, Soria, Meléndez, & Meléndez, the Cameros, Maestrat and Columbrets basins, which were 2006; Navarrete et al., 2013) and influenced the formation characterized by independent subsidence and stratigraphic of thrust ramps and fold belts during later tectonic inversion histories (Etheve et al., 2018; Salas et al., 2001). More re- (Liesa & Simón, 2009; Simón, 2004). cently, in Martín-Chivelet et al. (2019) have distinguished Folds in the Maestrat Basin, including the Miravete anti- a Neocomian (late Berriasian–Hauterivian) post-rift phase cline, are traditionally assumed to be the consequence of basin between rifting cycles of Late Jurassic and Barremian–early inversion during the Alpine compression triggered by the 1658 VERGÉS et al. | EAGE roughly N-S convergence between Africa and Europe (e.g. Cugny, Pardo, Salas, and Villena (1982), Liesa et al. (2006), Capote et al., 2002; Guimerà, 1984; Guimerà et al., 2004; Liesa et al. (2018), Gómez and Fernández-López (2006), Nebot & Guimerà, 2016; Salas & Casas, 1993; Simón, 2004). Bover-Arnal, Salas, Moreno Bedmar, and Bitzer (2009), The N-S to NNE-SSW shortening direction is documented Bover-Arnal, Salas, Guimerà, and Moreno-Bedmar (2014); north of the Miravete anticline, where a NW-SE sinuous belt of Bover-Arnal et al. (2010, 2015, 2016), Embry et al. (2010), salt-cored anticlines and exposures of Triassic deposits are in- Peropadre et al. (2013), Aurell et al. (2016) and Navarrete terpreted as the frontal part of a N-directed thrust sheet (Utrillas et al. (2013, 2014). Strata range from Triassic to poorly dated thrust; Simón & Liesa, 2011). This thrust sheet detaches above Cenozoic ages, and are arranged herein into six sedimen- either the middle Muschelkalk evaporites in its northern part tary units related to different age-based tectono-sedimentary (Maestrat Basement Thrust, Nebot & Guimerà, 2016) or Upper phases linked to the evolution of the Galve sub-basin. Triassic evaporites (Liesa, Casas, & Simón, 2018). The E–W The Upper Triassic deposits (sedimentary unit 1 in trending structures of Camarillas and Jorcas thrusts and the El Figure 3) comprise red clays with secondary gypsum that Morrón box-fold in the western flank of the Miravete anticline contains bipyramidal quartz crystals which are attributed to grew according to the N-S direction of shortening (Figure 4). diagenetic replacement of anhydrite crystals (Querol et al., The total shortening along a NNE-SSW profile of the 1992). These sediments are locally accompanied by red Iberian Ranges was estimated as 20.5% (Guimerà, Salas, shales, evaporites and dolostones of Middle Triassic age, Vergés, & Casas, 1996; Salas et al., 2001) across the Maestrat (e.g. Cañada Vellida area; Figure 2). In the Miravete anti- Basin, and 26% near the Cameros Basin (Guimerà et al., cline, Triassic strata weather easily and only crop out in the 2004). De Vicente et al. (2009) provided a similar 20% short- core of the anticline (Figures 2 and 3), where they are highly ening for the Castilian Branch only. Consequently, structures deformed by regional and local tectonic stresses. Although oblique or subparallel to the main direction of shortening are difficult to calculate, the local thicknesses of Upper Triassic expected to give shortening values lower than 20%. In any along the anticline are 20–30 m thick and might disappear event, fold superposition is observed in the study area and laterally. In the subsurface, however, Upper Triassic evapo- a relative chronology was established where E-W to ENE- rite deposits in the Maestrat Basin reach thicknesses up to WSW trending folds and thrusts (assumed as Early Miocene 250 m, whereas Middle Triassic Muschelkalk units range up age) overprinted earlier N-S to NNW-SSE trending folds (as- to 600 m, locally forming salt structures with larger thick- sumed as Eocene–Oligocene age; Simón, 2004; Figure 2). nesses at depth towards the NNE of the Miravete salt anticline (Nebot & Guimerà, 2016 and references therein). Jurassic strata (sedimentary unit 2 in Figure 3) are com- 3 | THE MIRAVETE SALT posed of shallow carbonate platform sediments ranging in age ANTICLINE from the Hettangian to the Tithonian. In the Miravete area, Liesa et al. (2006) differentiate eight Jurassic sedimentary The Miravete anticline, located in the Galve sub-basin that was lithostratigraphic units composed of shallow marine to tran- open towards the Tethys (Salas and Guimerà, 1996), was previ- sitional carbonates. Flanking the Miravete anticline, however, ously interpreted as resulting from the inversion of the roughly the Jurassic record is relatively thin, incomplete, and contains N–S trending westward-dipping Miravete normal fault (Liesa numerous angular unconformities. According to Liesa et al. et al., 2006). The greater thickness of Lower Cretaceous forma- (2006), Liesa et al. (2018) and thicknesses by Gautier (1979), tions observed on the western limb of the anticline was attrib- the preserved part of the Early Jurassic succession corresponds uted to the larger accommodation space in the hangingwall of to the Cortes de Tajuña (50 m) and Cuevas Labradas (60 m) the normal fault. Non-balanced published cross sections of the formations (Hettangian to Pliensbachian in age), the Late anticline are included in the Villarluengo map sheet, 1:50.000 Jurassic includes the Loriguilla (100–200 m) and Higueruelas scale (MAGNA geological map; Gautier, 1979), and in articles (60–70 m) formations (Oxfordian-Kimmeridgian) and the up- by Simón (2004) and Liesa et al. (2018). In order to demonstrate permost part is the Tithonian–Berriasian Villar del Arzobispo that the Miravete anticline developed as an early diapiric struc- Fm. showing a maximum of 250 m of thickness. A stratigraphic ture during the Jurassic and Early Cretaceous, which was never gap ranging from the earliest Berriasian to Hauterivian times mentioned in previously published studies, we first provide gen- (Salas et al., 2001) is recorded in the Miravete area as an un- eral stratigraphic and structural descriptions of the anticline. conformable boundary between the Villar del Arzobispo Fm. and the Hauterivian El Castellar Fm., and represents a major marine regression. Recently, Aurell et al. (2016, 2019) charac- 3.1 | Stratigraphy of the Miravete anticline terized three new formations (Cedrillas, Aguilar de Alfambra and Galve) along the latest Kimmeridgian–Berriasian succes- The sedimentary and stratigraphic framework of the Miravete sion of the Galve sub-basin, and proposed to restrict the Villar anticline (Figure 3) is based on detailed studies by Canérot, del Arzobispo Fm. to the València Basin (Aurell et al., 2019). VERGÉS et al. 1659 EAGE | Age (Ma) SU SE FIGURE 3 Representative stratigraphy column of the Miravete T6 2300 io. T5 anticline and surrounding regions showing ages, lithostratigraphic

eM T4 6 units, thicknesses, lithologies and sedimentary packages described in T3

T2 this study. The compiled stratigraphic log is after Canérot et al. (1982),

CENOZOIC T1 Paleogen Vennin and Aurell (2001), Bover-Arnal et al. (2009, 2010, and 2016), 66.0 Fortanete Fm La Cañadilla Fm Organ. de Mont. Fm Embry et al. (2010), Peropadre et al. (2013) and Aurell et al. (2016). Barranco de los Degollados Fm Late Mosqueruela Fm H: Hettangian, S: Sinemurian, P: Pliensbachian, T: Toarcian 100.5 Cretaceous Utrillas Fm

Albian Escucha Fm 113.0 5 Furthermore, Aurell et al. (2019) placed the intra-rift Berriasian to Hauterivian unconformity between the Berriasian Galve Fm. 1800

Benassal and the Hauterivian El Castellar Fm. However, this paper fol- Fm

Late Aptian lows the Jurassic stratigraphy mapped by Liesa et al. (2006), Liesa et al. (2018).

Villarroya Sedimentary unit 3 comprises the El Castellar, de los Pinares Fm Camarillas, Artoles and Morella lithostratigraphic units and spans the Hauterivian to late Barremian time interval (Figure 3). The El Castellar Fm. (Hauterivian to CRETACEOU S Barremian) was deposited in alluvial plain, palustrine, Forcall Fm

Early Aptian and lacustrine environments (Liesa et al., 2006; Meléndez et al., 2009; Navarrete et al., 2013), and consists of sand-

Facies stone, mudstone and limestone facies that show rapid lat- 125.0 1200 eral variations with distance from the anticline crest and Urgonia n

4 its faults (Liesa et al., 2006). Recently, the continental

Xert Fm Galve Formation has been defined and recognized in the strata of the Galve sub-basin (Aurell et al., 2016, 2019). The Galve Formation is equivalent to the basal El Castellar Formation as mapped in this study, suggesting the regional Morella Fm Berriasian unconformity may occur within this unit as

Artoles Fm well. The Camarillas Fm. (in the Weald facies, Figure 3) is

Barremian composed of discontinuous lenses of cross-bedded fluvial sandstone encased in reddish floodplain mudstone (Bover-

Camarillas Arnal, Moreno-Bedmar, Frijia, Pascual-Cebrian, & Salas, Fm 2016; Canérot et al., 1982; Embry et al., 2010; Navarrete 3 Weald Facies 600 et al., 2013, 2014). Both the El Castellar and Camarillas

129.4 formations record variations in occurrence, thickness and n El Castellar facies around the Jurassic core of the anticline, suggesting Fm that their deposition was strongly influenced by an actively 132.9 Hauterivia 145 Villar del growing topographic high (Miravete anticline) at the time Arzobispo Fm Tithon. of deposition, resulting in facies partitioning. In addition, Higueruelas Fm these units contain internal unconformities and erosional Kimmer. Loriguilla Fm surfaces. The Artoles Fm. (early to late Barremian accord- Chelva Fm 2 Mid. Turmiel Fm ing to Bover-Arnal et al., 2016) is composed of alternating

T. Barahona Fm JURASSIC

P. Cuevas green marl and bioclastic limestone rich in benthic foramin- Labradas Fm S. Cortes de Tajuña ifera and oysters suggesting very shallow marine to transi- 201.3 H. & Imón Fm 0 m tional environments (Vennin & Aurell, 2001). It has more

Late Keuper 1

TRIA S facies consistent thickness and facies distribution patterns around Cross-bedded the anticline compared to the El Castellar and Camarillas Continental sandstone Limestone Transitional Nodular Clay limestone formations. The last lithostratigraphic unit of sedimentary Shallow Limestone marine Evaporites nodules unit 3, the upper Barremian Morella Fm., is composed of Sandy Hemipelagic limestone Dolostone red mudstone and sandstone, and is interpreted as having Conglomerate Marl Breccia formed in tidal flat and high energy fluvial environments SE: Sedimentary environments SU: Sedimentary units (Bover-Arnal et al., 2016; Salas, 1987). Bover-Arnal et al. 1660 VERGÉS et al. | EAGE

LasCubetas

Loma de las Fig. 7c Remenderuelas

Remenderuelas fault

MasdeSangesa

Fig. 7b

Camarillas Fig. 5b Camarillasfault

Fig. 7a Pe adelaCingla Pe adelas Higueras El Batnfault

LasMingachas

Quaternary Late Oligoceneto Miocene Late Cretaceous Escuchaand Utrillas Fm. Benassal Fm. Villarroya Fm. ForcallFm. Tectonic features Xert Fm. Normal fault Villarroyade MorellaFm. losPinares Unconformity ArtolesFm. Fig. 5a Camarillas Fm. Miravete Anticline El CastellarFm. Syncline axis Late Jurassic Thrust Middle Jurassic Weld

Mushelkalk andKeuper Fold-axisPlunge VERGÉS et al. 1661 EAGE | FIGURE 4 Structural map of the core of the Miravete anticline, showing the major stratigraphic horizons and bedding attitudes obtained by remote sensing mapping and fieldwork. Note Camarillas Fm. (lower Barremian) bedding attitude and relationships with the Jurassic and Triassic core of the anticline.

(2010) noted that the Morella Fm. is more developed on the Villarroya carbonate platform. These authors interpreted the western flank of the anticline, where it unconformably a partial tectonic control for sea-level changes, but favoured rests on the Artoles Fm. a mainly eustatic origin to develop these unconformities. Above the Morella Fm., sedimentary environments be- Moreover, on the western flank of the Miravete anticline, the came fully marine and are composed of mostly carbon- top of the Villarroya de los Pinares Formation is locally not ate platform strata towards the top of the Xert Fm. (latest preserved due to recent erosion (Bover-Arnal et al., 2010). Barremian in age). The Xert Fm. is characterized by a sandy The lower part of sedimentary unit 5 contains the late and marl-dominated basal part that changes vertically into Aptian Benassal Fm. This latter lithostratigraphic unit carbonate strata containing coated grains, green algae and is arranged into two transgressive-regressive sequences benthic foraminifera (Bover-Arnal et al., 2010; Embry et al., (Bover-Arnal et al., 2010, 2016; Embry et al., 2010). The 2010; Vennin & Aurell, 2001). This unit marks the base of transgressive parts are made up of marls and marly lime- Urgonian facies in the Miravete region (sedimentary unit 4 stones with orbitolinids and gastropods, whereas the regres- in Figure 3). In addition, the Xert Fm. is thicker and contains sive units correspond to platform carbonates rich in rudists deeper facies on the western compared to the eastern flank and corals (Figure 3). The top of the Benassal Formation is (Bover-Arnal et al., 2010). These observations indicate that characterized by sand-grade siliciclastic input (Figure 3). The subsidence was greater on the western than on the eastern first transgressive–regressive sequence of the Benassal Fm. flank during deposition of sedimentary unit 4. The top of the shows similar facies and thickness patterns on both sides of Xert Fm. contains chondrodontid bivalves and miliolid fora- the anticline. The second transgressive–regressive sequence minifera suggesting a pronounced shallowing of relative sea likewise shows similar facies patterns on either side of the level, although no direct evidence for subaerial exposure has anticline but is thinner on the western side as a result of been recognized. later Palaeogene erosion. Furthermore, the lithostratigraphic The Xert Fm. marks the beginning of a major, Tethyan- units of sedimentary units 4 and 5 also show a progressive wide, transgression, which culminated with deposition of the thickness increase and a deepening of the sedimentary en- overlying Forcall Fm. The Forcall is interpreted as basin to vironments from north to south at the scale of the sub-ba- slope deposits, and is mainly composed of marls, marly lime- sin (Bover-Arnal et al., 2010; Embry et al., 2010; Vennin & stones, limestones and storm-induced turbidites. This unit is Aurell, 2001). dated as early Aptian based on ammonite occurrences, and Above the Benassal Formation, the sedimentary succes- includes the Oceanic Anoxic Event 1a (Bover-Arnal, Salas, sion records an unconformity and a transition back to tran- Martín-Closas, Schlagintweit, & Moreno-Bedmar, 2011, sitional and continental facies, which belong to the Escucha 2016; Moreno-Bedmar et al., 2009, 2010). The uppermost and Utrillas Fms. (Figure 3). The Escucha and Utrillas Fms. part of the Forcall Fm. passes laterally and is overlain by the are Albian-earliest Cenomanian in age (Canérot et al., 1982). Villarroya de los Pinares Fm. (upper part of sedimentary unit They are composed of coal-bearing deltaic deposits that 4; Figure 3), which is composed of coral, rudist-dominated change vertically into fluvial and locally aeolian sandstone floatstones and rudstones deposited in carbonate platform (Querol et al., 1992; Rodríguez-López, Meléndez, Soria, & shelf and slope environments during the late early Aptian De Boer, 2009). (Bover-Arnal et al., 2009, 2010, 2015). The facies are thicker The overlying Cenomanian to Maastrichtian sedimentary and shallower on the eastern flank of the anticline, whereas record (Late Cretaceous in Figure 3) consists of shallow ma- they thin and transition laterally into basinal deposits at the rine carbonates and fine siliciclastic strata with gypsum and Las Mingachas location on the western flank (Bover-Arnal lacustrine limestone (Canérot, 1991; Gil, Carenas, Segura, et al., 2009, 2010), suggesting that subsidence continued to Hidalgo, & García, 2004). The Late Cretaceous formations be greater on the western flank during the late early Aptian are only preserved on the eastern flank of the Miravete anti- (Figure 8a). A regionally recognized exposure surface char- cline, having been eroded from the west flank before deposi- acterized by local incision and karst dissolution occurs near tion of Palaeogene red beds. An unconformity associated with the top of the Villarroya Fm., indicating a significant fall in a major relative sea level drop at the end of the Maastrichtian relative sea level during the latest early Aptian (Bover-Arnal marks the top of sedimentary unit 5. et al., 2009, 2015, 2016). Alternatively, Peropadre et al. The youngest deposits exposed in the study area corre- (2013) identify as many as six erosional surfaces within this spond to Palaeogene alluvial to lacustrine conglomerate, interval, and interpret a complex drainage system recording sandstones and shales (sedimentary unit 6 in Figure 3). This southward and westward flow, coeval to the development of succession, was inferred to range from earliest Palaeocene to 1662 VERGÉS et al. | EAGE Miocene in age and was grouped into six tectono-sedimen- coarse succession of Palaeogene growth strata. The Miravete tary units bounded by unconformities associated with suc- anticline also preserves its southern periclinal termination cessive Alpine compressional events (González & Guimerà, (Figures 4 and 5a) while along its central segment is charac- 1993; Simón, 2004). Recently, K-Ar isotopic dating of illites terized by a complex, discontinuous and parallel to the axis from clay gouges near the SE front of the Iberian Ranges (Río normal fault system that collapsed its western flank. At a re- Grío Fault) provided three groups of absolute ages, for the gional scale, the Miravete anticline is bounded by two rela- first time in the study area (Aldega et al., 2019). The Río tively broad synclines: the N-S trending Camarillas syncline Grío Fault system was active during Permian-Triassic and to the west and the NNW-SSE trending Fortanete syncline to Late Jurassic (Mesozoic rifting phases) and then recorded the the east (Figure 2). compression stages during Campanian (72 Ma) and middle The core of the Miravete anticline, delineated by Eocene (43 Ma). the Keuper, Jurassic, and Lower Cretaceous to the mid Barremian (Artoles Fm.) part of the succession, shows a tight geometry especially along its central sector (Figure 4). 3.2 | Present geometry of the Miravete The southern sector displays an easterly verging crestal do- anticline and of surrounding structures main within the Jurassic and Lower Cretaceous El Castellar Formation (Figure 5a). The central sector of the anticline, The Miravete anticline is a 16-km long, almost N-S trend- recognizable by the Remenderuelas–Camarillas normal ing fold that reaches 20 km in length when coupled with fault system, locally exposes the Triassic succession along the Campos anticline to the north (Gautier, 1979; Figure 2). its core (Figures 4a and 5b). Where the Triassic is missing, The northward transition from the Miravete anticline to different subvertical to overturned Jurassic–Barremian suc- the Campos anticline is across the ESE-WNW trend- cessions of the two limbs of the Miravete anticline are jux- ing Cobatillas thrust, producing a local verticalization of taposed. Finally, in the northern sector, close to the Aliaga the anticline plunge (Figure 2; Simón & Liesa, 2011). The village (Figure 2), the anticline preserves its Jurassic cr- Campos anticline is embedded in the large ESE-WNW estal domain. The northern sector of the Miravete anticline trending Aliaga synclinorium, which is filled with a thick, was folded across the E–W trending La Olla monocline,

(a) Miravete Anticline E-W

Villarroya Benassal

Villarroya de Forcall los Pinares

Xert

Artoles

0 300 m

Two drone pictures (b) Miravete Anticline W-E FIGURE 5 Camarillas Syncline Remenderuelas Fault Fortanete Syncline showing the structure of the Miravete

Late Cretaceous anticline: (a) view to the south of the Villarroya Escucha- Utrillas southern termination of the Miravete Forcall Artoles Villarroya Xert anticline delineated by the Villarroya Camarillas Castellar Aptian carbonate platform smoothly rounded and east-vergent with a very Xert Jurassic Camarillas steep eastern limb; and (b) view to the Jurassic north of the central sector of the Miravete Triassic fold, cored by Triassic and Jurassic rocks displaying halokinetic features and exposing

0 200 m Cretaceous successions on both flanks (see location in Figure 4) VERGÉS et al. 1663 EAGE | resulting in a steep northward fold plunge of 70–80° and geometry and thus involving considerable offset. The lack an almost circular, an outstanding subvertical fold clo- of any hangingwall ramp at the level of Jurassic carbonate sure (Simón, 2004). The Remenderuelas–Camarillas nor- as well as the sudden changes in stratigraphy on both flanks mal faults were previously described by Liesa (2006) and along the central segment of the Miravete anticline (Figure 4), Navarrete et al. (2013, 2014) as a set of listric normal faults are more compatible with a salt weld interpretation. This dia- compartmentalizing the NNW-SSE trending Galve graben, piric explanation is also sustained by the existence of Jurassic a local sub-basin of the Maestrat Basin. angular unconformities and Lower Cretaceous ones infilled by Camarillas Fm. indicating tectonic activity along the Miravete structure that steepened its flanks generating a pre- 4 | EARLY JURASSIC TO APTIAN compression palaeorelief as described in this section. GROWTH OF THE MIRAVETE SALT Along the eastern flank of the Miravete salt anticline, the ANTICLINE Jurassic carbonate succession is >200-m thick and is characterized by two unconformities (Figure 6). The basal part (units In this section, we describe in greater detail the tectono-sedi- 1, 2 and 3 in Figure 6) is composed of thick breccia depos- mentary relationships along the core of the Miravete anticline its, attributed to the Jurassic 1, showing evidence of karstic from the Lower Jurassic through the lower Aptian Villarroya overprint. This interval is truncated by a well-bedded carbon- de los Pinares Formation. This section is supported by the ate unit with sparse biota and numerous metre-scale cycles collection of a large amount of structural data (2,400 dips), (units 5 and 6), which is attributed to the Jurassic 2. Bedding from field and remote sensing datasets, to better constrain within this Unit 5 is parallel to the basal unconformity (a in the tectonic and sedimentary relations. 3D geomodels were Figure 6). These Lower Jurassic carbonate platforms are trun- made for the region of Las Mingachas using high-quality im- cated towards the top by a high-angle planar erosional surface ages acquired with drones, where carbonate platforms of the (b in Figure 6) that cuts down through the stratigraphy and is Villarroya de los Pinares Formation, from late early Aptian associated with brecciation, a pink coloration, and reddening age, display several progradational bedsets in a hard-to-reach of the underlying carbonates. This erosional unconformity is cliff. The entire sedimentary succession, showing abundant onlapped at a relatively low angle (>10°) by cross-bedded evidence of growth of the Miravete anticline, which we inter- oolitic packstones and grainstones of the uppermost Jurassic pret to be related to salt tectonics, is examined in the follow- Villar del Arzobispo Formation (Figure 6). The subparallel ing Sections 4.1–4.3. deposition of the Villar del Arzobispo above its basal unconformity indicates previous tilting of the Lower Jurassic carbonate platforms. 4.1 | Jurassic salt anticline (salt The Villar del Arzobispo Formation is truncated by an mobilization) erosional unconformity onto which the lower Barremian fluvial system of the Camarillas Formation onlaps, filling The Jurassic to earliest Cretaceous structural evolution of an observed palaeotopographic relief of more than hundred the Miravete salt anticline is best illustrated in the central metres located near the active ridge of the rising Miravete sector of the anticline at the Peña de las Higueras locality salt wall (Figure 6a). Towards the south, the Hauterivian El (Figure 6). At this outcrop, the core of the anticline is char- Castellar Formation onlaps the top of the Villar del Arzobispo acterized by subvertical Jurassic carbonate formations with Formation and forms the eastern flank of the salt weld in an eastward stratigraphic polarity and a reduced total thick- contact with the west-dipping Jurassic strata (Figure 4). East- ness compared to regional. These Jurassic sequences are dipping Lower Cretaceous Artoles to Utrillas formations are in contact with steeply westward-dipping El Castellar and conformable above the Jurassic through Lower Cretaceous Camarillas formations along the western flank of the anti- Camarillas halokinetic sequence on the eastern flank of the cline. The contact between these two opposing successions Miravete salt anticline. is sharp and steeply east-dipping (079/84°), showing sub- The Peña de las Higueras locality (Figure 6) was used to parallel flanks and was previously interpreted as a thrust reconstruct the evolution of the eastern flank of the Miravete fault since the thick Jurassic carbonates seem to thrust salt wall by examining variations in bedding attitude of the above the subvertical to overturned alluvial and lacustrine Jurassic 1 (Lower Jurassic) carbonates and of progressively strata of the El Castellar Formation (Gautier, 1979; Liesa younger deposits, namely: Jurassic 2; uppermost Jurassic et al., 2006). Villar del Arzobispo Formation and lower Barremian flu- Interpreting this contact as a simple compressional thrust vial deposits of the Camarillas Formation through time. is not straightforward and it might only be possible thrusting We applied a sequential restoration, flattening layers above an original west-verging closed fold in which the hanging- each unconformity to calculate the rotation of layers below it wall shows a flat geometry and the footwall displays a ramp (Figure 6b). The first restoration (unfolding of the Camarillas 1664 VERGÉS et al. | EAGE W - E Utrillas (a) Benassal Western flank Salt weld Eastern flank Villarroya Forcall Xert Artoles

Camarillas Camarillas Jurassic 2 Villar del 62º 55º Arzobispo El Castellar Jurassic 1 A 62º 89º B 84º 45º 6 50º 5 80º 45º 2 68º 1 3 87º 86º 78º 8 Camarillas Fig.6c Fig.6d

Peña de la Higuera locality 0 100 m

(b) Present Time Unfolding Camarillas Fm. Unfolding Villar del Arzobispo Unfolding Jurassic 2 082/74º

032/78º

057/62º Jurassic 1 356/28º 1 358/11º Mean dip direction º planes: Jurassic101/21 335/49º º Jurassic 1 Camarillas Fm. 149/39 Villar del Arzobispo 072/78º Jurassic 2 125/26º n=23 Jurassic 1 (rotation: 62º, rotation axis: 00-147º) (rotation:26º, rotation axis: 00-215º) (rotation:49º, rotation axis: 00-064º)

Unit 5

A Unit 3 Erosional unconformity

Unit 1

FIGURE 6 (a) View to the north of the outcrop of the Miravete west-verging diapiric weld in the Peña de la Higuera that juxtaposes east- dipping Jurassic carbonates (eastern flank) against Early Cretaceous El Castellar strata dipping west (western flank) (see its location in Figure 4). The eastern flank shows multiple unconformities within the Jurassic formations and the Early Cretaceous Camarillas onlapping the Villar del Arzobispo Formation. (b) Dip attitudes of successive formations have been restored to the horizontal to calculate the orientation of the Jurassic 1, through Jurassic 2, Late Jurassic (Villar del Arzobispo Formation) and Lower Barremian (Camarillas Formation) times. The stereoplots show that the Jurassic 1 carbonates attitudes changed orientation significantly over time during successive restoration. (c) Base of Unit 1 composed of fragmented clasts interpreted as a reworked deposit of karstified carbonates. (d) Erosional unconformity affecting peritidal carbonates of Unit 3 with conglomerates marking the transition to the subtidal limestones of Unit 5 VERGÉS et al. 1665 EAGE | Fm.) involves a rotation of 62° about an axis of 00–147° pro- (a) Peña de la Cingla SW-NE ducing a Jurassic 1 dip of 101/21°; the second restoration Forcall Xert (unfolding Villar del Arzobispo Fm.) involves a rotation of 26° with an axis rotation of 00–215° giving a Jurassic 1 dip of Early Jurassic 358/11° and the third and last restoration (unfolding Jurassic Camarillas faul 2) needed a rotation of 49° with a rotation axis of 00-064o Artoles 203/57º t 281/85º resulting in a Jurassic 1 dip of 149/39°. Summarizing, from 248/72º Triassic o older to younger, Jurassic 1 layers were tilted 39 to SSW (be- 270/81º 264/85º 063/86º fore Jurassic 2 time), 11° to N (before Villar del Arzobispo 283/71º Fm.), and 21° to ESE before the deposition of the Camarillas 272/65º

Camarillas Formation. These changes in both dip angle and dip direction 223/67º do not seem to be typical of fault motions in which slightly more systematic rotations are observed. The unconformity at the top of the Villar del Arzobispo 0 100 m El Castellar Formation corresponds to a rough surface that bounds the (b) Mas de Sangüesa E-W Camarillas fault outcrops of Jurassic carbonates. The unconformity shows Eastern flank Western flank an angle with the onlapping Camarillas strata in its lower Remenderuelas fault Villarroya+Benassa l part, whereas it is overlaid by younger Camarillas strata in Forcall its upper part and thus constraining its palaeo-height. The 285/90º Xert Early Jurassic 096/80º flattening of the older onlapping Camarillas strata indicates Xert

109/74º Artoles 114/89º 260/55º that the unconformity surface was dipping about 26 degrees 121/61º 269/50º towards the ESE as shown in Figure 6b. The present vertical- 294/37º 328/30º ization of flanks occurred during the Palaeogene tightening Camarillas of the anticline that closed the salt wall along the central sec- 285/39º tor of the N–S trending Miravete anticline. A potential re- El Castellar 292/45º verse-slip component for the salt weld is not disregarded, thus 255/53º representing a thrust-weld (e.g. Rowan, Jackson, & Trudgill,

0 100 m 1999; Figure 6a). 261/44º

Remenderuelas fault 4.2 | Hauterivian–Early Barremian salt Jurassic wall and its western flank collapse 254/50º 273/63º

Artoles 259/73º The Remenderuelas–Camarillas listric extensional fault sys- Triassic 265/80º 246/80º tem characterizes the western flank of the Miravete anticline 249/82º 75º in its central region (Liesa et al., 2006; Figure 7). The plane Camarillas of the Remenderuelas–Camarillas extensional fault system 0 10 m Artoles is subparallel to the Triassic rocks cropping out in the core of the anticline and cuts through the Jurassic succession FIGURE 7 Drone images of three localities to define the (Cortes de Tajuña to Villar del Arzobispo formations). The structure of the Remenderuelas–Camarillas collapse fault system along Hauterivian–Barremian El Castellar continental to transi- the western flank of the Miravete diapiric anticline. From south to tional deposits are partly coeval with faulting, and the con- north, (see locations in Figure 4): (a) Peña de La Cingla, (b) Mas de tinental Camarillas and shallow marine Artoles formations Sangüesa and (c) Loma de las Remenderuelas outcrops. Descriptions show both syn- and post-faulting depositional patterns re- of each location can be found in the text lated to displacement on the two large Remenderuelas and Camarillas concave fault planes (location in Figure 4). The flank of the Miravete anticline constitute the footwall of geometry of the fault system is described hereinafter from the fault that cut the carbonates at a high angle. The fault south to north, in the Peña de la Cingla, Mas de Sangüesa and flattens along the Triassic salt-bearing rocks to the south Loma de las Remenderuelas localities (Figure 7, locations in illustrating its listric geometry (Figure 7a). The hanging- Figure 4). wall of the Camarillas fault contains approximately 80 m of At the Peña de la Cingla locality the Camarillas fault is Hauterivian El Castellar Formation. Above it, several hun- well exposed, as shown in the interpreted drone image of dred metres of Barremian Camarillas strata infill and onlap Figure 7a. The Lower Jurassic carbonates of the western the hangingwall fault plane showing a slight thickening 1666 VERGÉS et al. | EAGE towards the fault, which can define growth strata pattern. The eastern flank of the Miravete salt anticline at Peña de Upper Camarillas beds thin and overlie the topmost part las Higueras locality (Figure 6a) shows a well-preserved pa- of the fault, whereas the upper part of the mid-Barremian laeorelief carved in the Jurassic limestones and infilled by Artoles strata show no sign of growth and thus represent- non-marine sediments of the El Castellar and Camarillas ing post-faulting deposition in this locality (Figure 7a). formations. The Camarillas strata onlap the previously tilted The El Batán fault (from Liesa et al., 2006) constitutes the Jurassic units of the eastern flank of the Miravete salt anti- southern end of this 2.3-km-long Camarillas depocentre cline showing relatively constant thickness and an apparent (Figure 4). To the south, the Miravete anticline preserves subparallel attitude. Earliest Cretaceous facies distribution its complete fold geometry but is heavily faulted at the El along the central segment of the anticline in both the east- Castellar Formation level within the southern sector of ern flank (footwall) and the western flank (hangingwall of plunge domain 3 (Figure 4 for location) although faults are Remenderuelas–Camarillas fault system) indicate the exis- not represented at this scale (see details in Gautier, 1979 tence of a variable palaeorelief, defined by steeper Jurassic and Liesa et al., 2006). carbonates. This variable palaeorelief could be explained by At the Mas de Sangüesa locality, the Remenderuelas fault deposition along an elongated and relatively narrow salt wall hangingwall is exposed (as observed in a southward aerial characterized by the collapse of its western flank and by the view from drone photography in Figure 7b). The fault hang- potential extrusion of salt along its footwall. This palaeoto- ingwall is composed of Jurassic carbonates, the El Castellar pography was covered by the Camarillas river system, that and the basal Camarillas formations. The Hauterivian El would eventually traverse the rising Miravete salt wall. Castellar Formation thins southwards and the circa 250-m thick lower part of the early Barremian Camarillas Formation is deposited conformably on the underlying strata. At the Mas 4.3 | Late Barremian–Aptian salt anticline de Sangüesa locality, however, a deep incision cuts almost the growth and effects on carbonate platform entire lower Camarillas and is filled with middle Camarillas distribution fluvial deposits onlapping against the walls of the palaeorelief (Figure 7b). The upper part of the Camarillas Formation Depositional facies and thickness patterns suggest the is continuous, and thus postdates infill of the palaeovalley on Miravete anticline exerted control on sedimentary units the western flank of the Miravete salt anticline. These obser- throughout the early Aptian, primarily by creating more vations show that collapse of the western flank was coeval accommodation (subsidence) on the western flank than the with the mostly continental deposition of the El Castellar and eastern flank (Figure 4). Evidence supporting this conclu- Camarillas formations and influenced their facies, thickness sion includes: (a) the continental to transitional Morella distributions and stratal geometries. Formation is thicker in the western flank; (b) the overly- At the Loma de las Remenderuelas locality, the ing shallow marine carbonates of the Xert Formation are Remenderuelas fault is well exposed dipping 055/72° thicker and contains deeper facies on the western flank and (Figure 7c). Here, Jurassic carbonates and remnants of (c) the carbonate platforms of the Villarroya de los Pinares salt-bearing Upper Triassic rocks form the footwall of the Formation record deeper water facies, as well as west-di- fault. The upper part of the Camarillas Formation onlap the rected progradational geometries away from the crest of the fault and the lower part of the Artoles Formation, above an anticline, on its western flank. In the Las Mingachas local- unconformity, onlap both the Camarillas Formation and the ity, located on the western limb, near the village of Miravete fault plane. The upper marine Artoles Formation unconform- de la Sierra (Figure 4), Bover-Arnal et al. (2009) described ably overlies older growth strata and fossilizes the palaeore- three superposed systems tracts (highstand, lowstand, and lief developed during the activity of the Remenderuelas fault. transgressive) within the lower Aptian Villarroya de los We interpret the W-dipping Remenderuelas–Camarillas Pinares platform, preserving clinoforms that we analysed extensional fault system to be related to the collapse of the to determine their direction of progradation with respect western flank of the growing Miravete salt anticline or elon- to their stratigraphic position (Figure 8). This was accom- gated salt weld starting before the deposition of the early plished using a virtual outcrop model based on high-quality Barremian Camarillas Formation. The collapse of the central photographs collected by drone photogrammetry. The mod- segment of the anticline could be related to increasing exten- elled dip directions of the clinoforms were verified with di- sion or sediment loading (Liesa et al., 2006), or to removal of rect measurements in the field. The results of this analysis salt at depth flowing towards the active salt wall. show that the clinoforms of the highstand systems tract are Reconstructing the evolving topography during growth prograding towards the SW, whereas those of the subse- folding or diapiric structures is always difficult unless growth quent lowstand systems tract prograde towards the SSW, or halokinetic depositional sequences directly fossilize previ- and those of the overlying transgressive systems tract pro- ous tectonic or erosional features (Burbank & Vergés, 1994). grade towards the W (Figure 8b,c). VERGÉS et al. 1667 EAGE | Taking into account that regional platform progradation footwall of the Remenderuelas–Camarillas fault system. In was southwards, towards the Tethys, analysed platforms pro- addition, stratigraphic thicknesses suggest a shift to decreased grading roughly towards the west suggest that the Miravete subsidence on the eastern flank of the Miravete anticline rel- anticline was a bathymetric high that partially controlled the ative to the western flank during the Early Cretaceous, sug- platform architecture, along with relative sea level variations. gesting primary welding had occurred beneath the Fortanete To verify the potential growth of the Miravete salt anticline syncline by this time. These Barremian–Aptian carbonate during deposition of the upper Barremian–Aptian carbonate platforms could locally or entirely onlap against the flanks platform successions we analysed different published strati- of the salt ridge and thus produce a complex growth of the graphic columns in areas relatively away and close to the axis carbonate sedimentary system as occurs in other diapiric do- of the Miravete anticline (Figure 9b). The stratigraphic col- mains like in the La Popa Basin (Giles et al., 2008), in the umns of the Barranco de las Calzadas in the eastern flank Central High Atlas (Martín-Martín et al., 2017; Saura et al., of Miravete anticline and the Estrecho de la Calzada Vieja 2014; Teixell, Barnolas, Rosales, & Arboleya, 2017), in the (Bover-Arnal et al., 2010) in the western flank are located 1.2 Basque-Cantabrian Basin (Poprawski et al., 2016), or on and 0.8 km away from the axis of the anticline respectively the present margins of the Red Sea (Purkis, Harris, & Ellis, (Figure 9b). 2012). Assuming that the Miravete salt anticline was rising during deposition of these units, the thinner Las Cubetas stratigraphic column would represent a relatively proximal 4.4 | Reconstruction of the Miravete position above the crest of the anticline, whereas the other salt anticline sections along the flanks would correspond to more distal areas away from the crestal domain. Therefore, we have Although field evidence documents the growth of the projected and correlated the 279 m thick succession of the Miravete salt anticline from the Early Jurassic until at least Las Cubetas stratigraphic column together with the west- the Aptian, the construction of a constrained cross section ern flank section (a minimum of 572 m) and the Eastern is not straightforward due to the erosion of the anticline flank section (547 m thick) stratigraphic columns located crestal domains, a crucial part of the geological cross sec- in the central part of the anticline (Figure 9b). The com- tion (Figure 9). Therefore, two end-members models are parison shows that all the stratigraphic units, except the constructed: (a) a buckle fold model overlying an inverted Villarroya de los Pinares Formation thin towards the crest normal fault, fitting the present structural relief difference, of the anticline, indicating amplification of the salt anti- with its western flank higher than the eastern one, according cline during the late Barremian to Aptian. The Villarroya to published interpretations (Figure 9a), and (b) a growing de los Pinares Formation thins and records deeper facies salt anticline model during the Jurassic and Early Cretaceous towards the western flank of the Miravete salt anticline above the same inverted normal fault, as interpreted in this (Bover-Arnal et al., 2010), and is relatively thicker on its study (Figure 9d). eastern flank (Figure 9b). Such a configuration may be explained by lateral facies changes related to carbonate platform production and progradation above the more dis- 4.4.1 | Buckle anticline model tal facies of the Forcall Formation on the western flank, as observed in the Las Mingachas locality (Figures 8a and The buckle anticline model, was built according to: (a) 9b). Alternatively, since carbonate platforms preferentially techniques of balanced cross-sectional construction as- develop in the photic zone above palaeohighs, they may be suming minimal shortening; (b) a large number of new relatively thicker above the growing salt structures, as ob- structural dips measured in the field along the line of the served in other diapiric examples like the El Gordo diapir cross section (n = 154) and through remote sensing map- in the La Popa Basin (Giles, Druke, Mercer, & Hunnivutt- ping, along the entire length of the anticline limbs and Mack, 2008), the Bakio diapir in the Basque-Cantabrian core; (c) compilation of thickness data extrapolated from Basin (Poprawski et al., 2016), and the Tazoult salt wall in our geological map and from previous stratigraphic studies the Central High Atlas (Martín-Martín et al., 2017). This (Bover-Arnal et al., 2009, 2010, 2015, 2016; Embry et al., suggests that the crest of the Miravete anticline, and maybe 2010; Meléndez et al., 2009; Navarrete et al., 2013, 2014; its eastern flank, remained in shallower depositional en- Peropadre et al., 2013) to constrain stratal thicknesses; and vironments during the deposition of the Villarroya de los (d) constant thickness for groups of strata across the anti- Pinares Formation compared with the western flank. cline, except where clear thickness variations were identi- During the late Barremian to Aptian, the Miravete anti- fied in the field or from our stratal thickness dataset. This cline is interpreted to have continued to evolve either as a model shows a fold amplitude of 1.4 km between its crest growing salt anticline or as an elongated salt wall along the and its western flank, whereas increasing to 2.4 km with 1668 VERGÉS et al. | EAGE (a)a SW-NE

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c(c) Prograding directions VERGÉS et al. 1669 EAGE | FIGURE 8 (a) Interpreted aerial photograph (taken from Bover-Arnal et al., 2009) and schematic line drawing of the Las Mingachas locality (see location in Figure 4) showing the highstand (green), lowstand (yellow/orange) and transgressive (purple) systems tracts that were analysed. (b) Interpreted drone-derived outcrop model showing traced beds of the highstand (green), lowstand (yellow/orange), and transgressive (purple) systems tracts preserved in the early Aptian Villarroya de los Pinares with plots showing the restored orientations of clinoform progradation. Arrows in the stereoplots indicate clinoform measured directions (note each systems tract preserves its own unique direction, and both the highstand and transgressive systems tracts have a westward component, directed away from the crest of the Miravete anticline); and (c) schematic line drawing of the Las Mingachas locality (taken from Hunt and Tucker, 1992, 1995) showing the highstand (green), lowstand (yellow/orange) and transgressive (purple) systems tracts that were analysed and a rose diagram showing the direction of progradation for each systems tract respect to its eastern flank (Figure 9a). Shortening at the Xert Formation, the early Aptian Forcall and Villarroya de los base of the Xert Formation is 20% (2 km) in an E–W direc- Pinares formations with thicknesses of 75 and 87 m, respec- tion, perpendicular to both the anticline axis and the re- tively, and the latest early–late Aptian Benassal Formation, gional direction of shortening in the Maestrat Basin. with a minimum thickness of 77 m (Bover-Arnal et al., 2010). This 279-m-thick Las Cubetas succession is about half the total thickness of the equivalent succession outcropping on 4.4.2 | Growing salt anticline model the eastern and western flanks of the anticline along the E-W cross section (Estrecho de la Calzada Vieja and Barranco de The cross section considering the anticline as a growing salt las Calzadas logs; Figure 9b). structure during the Jurassic–Early Cretaceous periods was In the growing salt anticline model, the projected posi- built using the same general assumptions as the buckle anti- tion of the base Xert carbonate platform in the E-W cross cline model and identical structural dip and stratal thickness section does not permit thick preservation of the underlying datasets. However, we used four additional constraints by Hauterivian–Barremian pre-Xert sedimentary units in the (a) projecting the base of the Xert Formation along a lon- core of the anticline (El Castellar, Camarillas, Artoles and gitudinal section to constrain its position in the intersecting Morella formations; Figure 9d). Field observations described E–W cross section (Figure 9c; see its position in Figure 4); earlier show that these steeply dipping pre-Xert sediments (b) using the thicknesses of the Las Cubetas stratigraphic suc- onlap against Jurassic platforms (Figure 6), and are wedged cession projected from the northern termination of the an- towards the Miravete salt weld as observed by an abrupt de- ticline, as representative of the crestal domain stratigraphy crease in dip at the boundary between Artoles and the Morella and compared to the equivalent successions in the flanks formations. Above the Xert Formation, the geological cross of the anticline (Figure 9b); (c) drawing appropriate stratal section is constructed considering the decrease in thickness geometries for growing diapiric anticlines above salt walls, of Xert, Forcall, Villarroya de los Pinares and Benassal for- when observed in the field and (d) ensuring that the general mations using typical growth triangle geometries in both geometry of the growing salt anticline model replicates the flanks (Figure 9d). This reconstruction is consistent with the preserved east-vergent southern termination of the anticline interpretation of the Las Mingachas locality where the car- (as imaged in Figure 5a). bonate platforms of the Villarroya de los Pinares Formation The longitudinal cross section was constructed using prograded roughly westward and thus outwards from the about 200 dip measurements to define 5 plunge domains N–S trending core of the growing Miravete salt anticline (Figure 9c). The plunge of domain 1 in the northern termi- (Figure 8). This model shows a fold amplitude of ∼0.8 km nation of the Miravete salt anticline is 70° north due to its between its crest and its western flank, whereas increas- north-bending across the ENE-WSW trending Cobatillas ing to 1.9 km with respect to its eastern flank (Figure 9a). thrust (Figures 2 and 4), which produced the verticalization Shortening at the base of the Xert Formation is only 10% of the anticline termination and the beautiful geological fea- (1 km) in an E-W direction; about half the amount of short- tures of smaller folds with subvertical axes near Aliaga as ening obtained for the buckle anticline model. described by Simón (2004). Domains 2 and 3 are plunging 3° An analysis of the well-calibrated cross section provides and 5° north respectively. Domains 4 and 5 show the southern other important results regarding the variations of the sedi- plunge of the anticline with very similar values of 9° and 8° mentary thicknesses across the Miravete anticline. From the respectively. base of the El Castellar Formation (Hauterivian) to the base At the intersection between longitudinal and E-W cross of the Benassal Formation (latest early Aptian) the total cu- sections, the base of the Xert Formation, corresponding to the mulative sedimentary thickness is 570 m (~30%) greater on projected Las Cubetas log, is estimated to lie at an elevation the western flank than in the eastern one. If we compare only of ∼1,690 m. asl, in contrast to its position at 2,200 m asl at the El Castellar and Camarillas formations (Hauterivian– the anticline model buckle (Figure 9b,c). This stratigraphic early Barremian) it turns out that these units are ~40% thicker succession encompasses the 40-m thick upper Barremian in its western flank. 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%DVHPHQW NP VERGÉS et al. 1671 EAGE | FIGURE 9 (a) Buckle fold model cross section across the Miravete anticline constructed with constant thicknesses wherever possible (location in Figure 4). (b) Thickness variations from the Xert to Benassal formations (upper Barremian–Aptian) across the Miravete salt anticline comparing the Las Cubetas section (see location in Figure 4) with that of the Western and the Eastern flanks (taken from Bover-Arnal et al., 2010); c) Longitudinal cross section defining the plunges of 5-axis fold domains (see map in Figure 4) along the base of Xert Fm. represented by a thick green line. The elevation of the base Xert Fm. in the E–W trending model is based on this longitudinal section. (d) Cross section across the core of Miravete anticline constructed with the constraints of the results shown in (b) and (c): The base of Xert Fm. is located at 1,690 m above sea level at the crest of the anticline and thickness projections of Las Cubetas log are applied to the top of the anticline

30% is still determined during deposition of Xert, Forcall and by a narrow strip of Upper Triassic rocks in its core overlain Villarroya de los Pinares carbonate platforms in the western by thick Jurassic carbonates defining an elongated anticline flank of the anticline (Figure 9b). Despite the greatest western (Figure 10). The sedimentary infill of the adjacent asymmet- flank thicknesses throughout most of the Lower Cretaceous ric syncline to the north, composed of a few hundred metres sedimentation, in agreement with the Remenderuelas– of lower Barremian to Upper Cretaceous deposits, shows Camarillas west-dipping extensional fault system, the significant thinning of lower Barremian to Aptian, and pos- configuration of the two flanks currently shows a reverse sibly Albian, strata towards the crest of the Castel de Cabra arrangement. In this way, the base of the Xert Formation is anticline. The most striking feature is the well-developed presently located >1,500 m higher in the Camarillas syncline Albian unconformity bevelling the crest of the anticline at (to the west) than in the Fortanete syncline (to the east), in- the base of the Escucha and Utrillas formations. Above the dicating a post-Xert tectonic inversion during the Cenozoic Utrillas Formation, a thin package of Upper Cretaceous car- Alpine compression along a west-dipping basement normal bonates is the youngest preserved deposit within the Castel fault. The base of the Cenozoic red beds deposited on both de Cabra growth syncline (Canérot, Crespo, & Navarro, flanks of the anticline are located almost at the same eleva- 1977). This stratigraphic thinning towards the anticline crest tion but showing the most significant erosive unconformity indicates that folding and erosion occurred before deposi- in the Camarillas syncline cutting down to the basal part of tion of the non-marine Albian Escucha-Utrillas succession. Benassal Formation (Figure 9d). In this paper we associate The growth of the Castel de Cabra anticline during Early the 1,500 m of uplift as related to the compressional reacti- Cretaceous is partially coeval with the diapiric growth of the vation of the west-dipping basement normal fault at depth, Miravete salt anticline. A simple structural restoration using triggering the east-vergence of the Miravete salt anticline as the base of the Utrillas Formation as a flat reference level exposed along its southern termination (Figure 5). in the Castel de Cabra salt anticline, confirmed an approximately 12° dip of the northern flank of the salt anticline before Albian deposition. This unconformity at the base of the 5 | JURASSIC AND EARLY–LATE Albian Escucha-Utrillas formations is observed at regional CRETACEOUS REGIONAL DIAPIRIC scale in the Maestrat Basin above underlying stratigraphy in- STRUCTURES cluding Upper Triassic evaporites. This observation agrees with the outcrops of two 2-m-thick microconglomerate beds In this section, we propose a regional analysis of tectono- within the Escucha Formation containing bipyramidal quartz sedimentary relationships using published geological maps (around 35-km northwest of the study area; Querol et al., and fieldwork in order to show evidence of other nearby 1992). According to these authors, these idiomorphic crystals salt-related structures that followed a similar evolution as of quartz, showing large and abundant anhydrite inclusions, the Miravete anticline. The regional evidence for salt-related grew within the Triassic evaporites and their erosion, short structures growing from the Early Jurassic to Late Cretaceous transport and deposition, indicate the exposure and dissolu- includes: well-exposed discordant contacts between salt- tion of large volumes of evaporites during Albian period at bearing rocks and younger strata, unconformities, growth least. strata and onlap, and typical diapiric patterns like hooks and flaps. Two of the best examples, located at Castel de Cabra and the Cañada Vellida (Figure 2), are described below. 5.2 | Late Jurassic flap to Aptian passive diapir development along the Cañada Vellida salt wall 5.1 | Earliest Cretaceous to Aptian Castel de Cabra salt anticline growth The Cañada Vellida NW-SE striking structure, located north- east of the town of Galve, forms an elongated outcrop of The near E–W trending Castel de Cabra salt anticline, located Triassic red clay and gypsum in map view, up to 10-km long to the south of the village of Castel de Cabra, is characterized and a few hundred metres wide (Figure 11; see geological 1672 VERGÉS et al. | EAGE

S Castel de Cabra Syncline N Castel de Cabra La Muela Cabezo Lagonera Salt anticline 350/59º 297/25º Late Cretaceous Late Albian-Cen omanian 018/30º 302/24º 353/62º Albian

350/64º 307/22º La 331/76º te Barrem ian-Aptian Early Jurassic Early Cretaceous-Barremian La Solana

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La Muela Cabezo Lagonera Quaternary Late Cretaceous Late Albian–Cenomanian Albian (Escucha and Utrillas Fm.) Late Barremian–Aptian Castel de Cabra Salt anticline Early Cretaceous–Barremian Late Jurassic Middle Jurassic Early Jurassic Keuper salt-bearing red clays (locally with embedded Muschelkalk rocks) Salt diapir La Solana Axis of the Castel de Cabra salt dome Unconformity

FIGURE 10 Drone picture and interpretation of the asymmetric syncline involving Hauterivian-Barremian-Aptian growth sequences below the Albian unconformity (base of the Escucha Formation). The map shows the general structure of the Castel de Cabra salt anticline with a long exposure of Upper Triassic evaporites, interpreted as an elongated diapiric structure (see location in Figure 2) maps of Villarluengo and Argente; Gautier, 1979; Martín to Aptian unconformity is interpreted as a halokinetic hook & Canérot, 1977). This structure has been traditionally in- (Figure 11c). The NE flank of the central part of Cañada terpreted as a normal fault bounding the Cretaceous Galve Vellida shows a spectacular stratal relationship between sub-basin (Liesa et al., 2006), inverted in its SE part along small patches of overturned Jurassic carbonate beds that the E-W trending Cobatillas thrust (Simón, 2004; Simón & lie unconformably on top of a thick subvertical Barremian– Liesa, 2011) (see location in Figure 2). Aptian succession (Figure 11b). The Jurassic beds have over- The Cañada Vellida structure displays different strati- turned dips that vary from 53° SW in the lower part in contact graphic successions on both sides of the Upper Triassic rocks with the Upper Triassic evaporites, to only 17° SW in contact cropping out along its core (Figure 11). The SW flank con- with younger Upper Cretaceous strata. We interpret the thin tains a thick Lower Jurassic to lower Barremian succession Jurassic patches as remnants of a large overturned flap against (equivalent to Camarillas Formation) and lacks younger which the younger sediments were onlapping during the infill deposits, whereas the NE flank shows a reduced Upper of the basin to the NE of the Cañada Vellida salt wall. The Jurassic to lower Barremian succession followed by a rela- Cañada Vellida salt wall separated the Galve minibasin to the tively thick upper Barremian to Upper Cretaceous succession SW from the Aliaga minibasin to the NE. The present deeper (Figure 11). Along the NE flank, the Upper Triassic rocks position of the Galve minibasin to the SW, together with the are in contact with Upper Jurassic through Aptian units indi- SW-dipping flap on its NE flank, strongly indicates that a cating a discordant limit. Two salt-related bedding structures large breakout of salt extrusion was NE-directed soon after within the NE flank of the Cañada Vellida confirms its evo- the deposition of Upper Jurassic carbonate platforms cover- lution as a salt wall: a small hook within Lower Cretaceous ing the salt wall roof. Lower Cretaceous deposition infilled beds and a large flap of Jurassic carbonates of which only the SW side of the Aliaga minibasin onlapping against the at remnants crop out (Figure 11). Along the contact with Upper least 500-m-long upturned flap. The Jurassic thin carbonate Triassic salt-bearing rocks, a local intra-upper Barremian patches forming the flap structure are part of the NE flank of VERGÉS et al. 1673 EAGE | (a) SW-NE Cenozoic

047/15º Jurassic Jurassic overturned flap 230/30º Late Cretaceous overturned flap Albian 238/50º 053/65º Triassic 047/71º

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Cañada Vellida Fault a Cenozoic Late Cretaceous Albian (Escucha and Utrillas Fm.) b Aliaga Synclinorium Late Barremian-Aptian Early Barremian Early Cretaceous Late Jurassic Middle Jurassic Early Jurassic Triassic Galve Basin c Salt diapir

Late Jurassic Flap

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FIGURE 11 (a) Drone aerial view to the NW along the NE flank of the Cañada Vellida salt wall where upturned Upper Jurassic platform carbonates lie above subvertical Barremian and Aptian units displaying onlapping geometries against an overturned flap. Below, the map shows the position of characteristic salt-related flap (a and b) and hook (c) shapes. b) Field picture showing a close up of the NE segment of the 500-m long of Upper Jurassic flap structure. (c) Hook geometry of two Early Barremian continental halokinetic depositional sequences (see location in Figure 2) the Cañada Vellida salt wall and therefore represent the oldest the uppermost Jurassic to the Albian. Field examples of units outcropping along this flank. Their attitude dipping to salt walls, slat-related normal faults, hook and flap struc- SW along the contact with Upper Triassic evaporites does tures are described in the Alps (Graham, Jackson, Pilcher, not permit to interpret them as remnants of a potential Alpine & Kilsdonk, 2012), Pyrenees (Saura et al., 2016), Central hangingwall thrust. High Atlas (Saura et al., 2014) and the Sivas Basin in Turkey The NW-SE elongated structure at Cañada Vellida is (Ringenbach et al., 2013), among others (Rowan, Giles, interpreted in this study as a salt wall that was active from Hearon, & Fiduk, 2016). Offshore examples, analysed on 1674 VERGÉS et al. | EAGE seismic profiles, are very common in a large variety of of the upper lower Albian Las Mingachas carbonate platform geological settings (Jackson & Hudec, 2017). Described progradation directions on the western flank (Figure 8). We structures at Miravete, Castel de Cabra and Cañada Vellida interpret this as a period of growth of salt anticline with a thin- provide evidence for a regional halokinetic history of Early ning of the carbonate halokinetic sequences towards the crest Jurassic through Albian, and possibly later, but prior to of the anticline. However, the Miravete salt wall growth on the regional Palaeogene compression. This compression tight- footwall of the Remenderuelas–Camarillas fault system would ened most of the pre-existing diapiric structures, including also be possible until at least the beginning of the Albian, con- those analysed in this study, as well as rejuvenated others sidering the coeval evolution observed in the Castel de Cabra like the Teruel diapir, active during Tortonian–Messinian structure (Figure 10) and in the Cañada Vellida (Figure 11). deposition (e.g. Alonso-Zarza & Calvo, 2000). The duration of this stage of salt wall growth would be related to the amount of salt below adjacent synclines, which produced variations in depositional thicknesses and differential ages of 6 | DISCUSSION primary welding (as described in Fortanete and Aliaga synclines-minibasins). The fourth and last stage of diapiric growth A model for the integrated halokinetic and stratigraphic evolu- is related to Alpine shortening during which the described tion of the Miravete anticline, from the Jurassic through Alpine diapiric structures were squeezed, welded and thrusted (thrust- compression extending into the Miocene, is shown in Figure 12. weld of Miravete anticline, potential salt withdrawal in the We address the implications of this model, as described for Cenozoic Aliaga synclinorium and the Miocene Teruel diapir). the Miravete salt anticline, Castel de Cabra salt anticline and This investigation of the Maestrat basin builds on important Cañada Vellida salt wall first, at the scale of the Maestrat Basin, advances in salt tectonics over the last decades, beginning in the and then at the broader scale of the northeastern margin of the 1940s through 1980s with studies of the Iberian fold and thrust Iberian plate towards its limit with the European plate. belt where salt tectonics and halokinetic sequences are preserved, such as in the Pyrenees and Basque-Cantabrian Basin and the Betic Cordillera (e.g. Brinkmann & Logters, 1968; 6.1 | Implications of salt tectonics at the Moseley, Cuttelll, Lange, Stevens, & Warbrick, 1981; Ríos, Maestrat Basin scale 1948). More recent investigations into the role of salt tectonics, specifically in the large European and North African Permo- The diapiric structures described in the Miravete anticline, in Triassic salt basins, illustrate its influence during both extension the Castel de Cabra and Cañada Vellida localities, evolved and subsequent compressional inversion (Soto et al., 2017). The prior to Alpine compression, from the Jurassic through late identification of halokinetic depositional sequences (e.g. Giles Early Cretaceous and were later reactivated during compres- & Lawton, 2002; Giles & Rowan, 2012), even in regions where sion from the Palaeocene through Miocene. The diapiric evo- no trace of salt-bearing rocks is preserved, has been associated lution model of the studied region of the Maestrat Basin has with diapiric structuration, and the age of contemporaneous dep- been divided into four different periods and is summarized ositional units determines the timing of salt tectonic-related de- in Figure 12. The first stage, during the Jurassic, is character- formation. Some excellent examples occur in the Western Alps ized by the formation of salt anticlines, as described in the La (e.g. Graham et al., 2012), the southern Pyrenees and Basque- Peña de la Higuera outcrop where Jurassic carbonate strata Cantabrian Basin (e.g. Bodego & Agirrezabala, 2013; López- of different units rotated with unsystematic orientations near Horgue et al., 2010; Lopez-Mir et al., 2014; Poprawski et al., the Miravete anticline culmination (Figure 6). The overturned 2016; Saura et al., 2016) and the Central High Atlas (Martín- Upper Jurassic carbonates of Cañada Vellida, interpreted as Martín et al., 2017; Moragas et al., 2017, 2018; Teixell et al., a diapiric flap, indicate that the roof of the anticline during 2017). One of the most significant characteristics of these exam- Jurassic time could have been formed by a thin carbonate se- ples is the lack of extensional faults cutting the post-salt deposi- quence (Figure 10). The second stage of evolution during the tional sequences. The lack of extensional faults in the post-salt Hauterivian and early Barremian is widely represented in the strata is due to decoupling of the presalt structure (basement) outcrops along the western flank of the Miravete anticline at and the post-salt structure. In most cases, the bending of post- Loma de las Remenderuelas, Mas de Sangüesa and Peña de salt units after a short phase of extension produces long, narrow la Cingla (Figure 7). This stage is characterized by the growth grabens that trigger reactive, active and passive diapirism along of the Miravete salt wall producing differential subsidence, salt walls (e.g. Dooley & Schreurs, 2012). collapse and growth of the Remenderuelas–Camarillas fault By applying these salt tectonic concepts, a new geolog- system, potential extrusion of salt, and formation of variable ical cross section has been constructed between the eastern palaeorelief along the flanks of the salt wall. The third stage of Cañada-Benatanduz and western Ababuj anticlines enclosing evolution is less constrained due to lack of direct observations the Miravete salt-related anticline in its centre (Figure 13). in the Miravete anticline, with the exception of the analysis The geological cross section is constructed using the detailed VERGÉS et al. 1675 EAGE | 5HJLRQDOREVHUYDWLRQV &DPDULOODV 0LUDYHWH )RUWDQHWH V\QFOLQH DQWLFOLQH V\QFOLQH $JH 0D 6( 7 VHFRQFRQGDQGDU\ZHOGQGDU LR 7HUXHO0LRFHQHGLDSLU 7 6WDJH 3UHVHQW 7 7 7 5HMXYHQDWHGGLDSLU

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FIGURE 12 Schematic model of pre-Cenozoic compression diapiric evolution of the Miravete salt antilcine combined with results from Castel de Cabra growth anticline and Cañada Vellida salt wall. During the first stage (Jurassic), the anticline shows thinner platform sequences along its crest. Second stage records the increase of subsidence in the western flank coevally its collapse along the Rememderuelas–Camarillas fault system in its central sector. Potential salt extrusion along the footwall of the fault system occurred as well as in the Cañada Vellida salt wall. The third stage of diapiric evolution records both the growth of the salt anticline or salt wall in Miravete and continued extrusive diapirism at Cañada Vellida salt wall. The fourth and last stage occurred during the Alpine shortening, tightening previous diapiric structures geological section across the Miravete anticline and the geo- Moissenet, 1981). The presalt basement is cut by a westerly logical sections from the IGME (1979) geological maps of dipping fault located beneath the Miravete anticline, as deter- Villarluengo and Alfambra (Gautier, 1979; Olivé, Godoy, & mined by the presence of thicker Lower Cretaceous strata on its 1676 VERGÉS et al. | EAGE W Miravete anticline E

Cañada-Benatanduz anticline Camarillas syncline La Lastra syncline Fortanetesyncline Ababuj anticline Cross section

0 1 2 345 km

W E Ababuj anticline Camarillas syncline Miravete anticline Fortanete syncline La Lastra syncline Cañada-Benatanduz 2 anticline

Late Cretaceous 1 Xert Artoles Escucha-Utrillas

Camarillas Benassal 0

Jurassic –1

–2 0 1 2 345 km

Cenozoic Benassal Fm. Villarroya Fm. Xert Fm. Camarillas Fm. Jurassic Late Cretaceous Escucha and Utrillas Fm. Forcall Fm. Morella-Artoles Fm. El Castellar Fm. Triassic

FIGURE 13 Regional geological map and E-W trending line locating the geological cross section encompassing the Ababuj, Miravete and Cañada-Benatanduz anticlines separating the Camarillas and the Fortanete-La lastra synclines (Villarluengo MAGNA; Gautier, 1979). Most interesting is the low structural relief of the Miravete antilcine core as well as its apparent poor continuity of Jurassic and lowermost Cretaceous layers within it. The regional cross section is based on diapiric interpretations as discussed in this paper (see location in Figure 2) western flank when restored at the base of Upper Cretaceous Seillé et al., 2015) and likely includes numerous salt struc- strata. The extensional fault system of Remenderuelas– tures that still need to be studied, of which Miravete, Castel de Camarillas could possibly be related in space and time to the Cabra and Cañada Vellida-Pancrudo, have been identified in basement fault beneath the Miravete anticline at depth, but this study. Other sedimentary basins developed above Upper is not necessarily connected. In fact, in our interpretation, Triassic salt show comparable numbers of salt structures with the Remenderuelas–Camarillas fault system is a salt-related similar geometries. For example the Central Polish Basin is growth fault that collapsed the western flank of the Miravete about 140-km wide and contains five central diapiric salt walls salt wall along its central segment. Excellent examples of simi- and marginal salt anticlines (Krzywiec et al., 2017), and the lar growth faults are imaged on seismic lines crossing the Horn Central Glückstadt Graben displays a total of eight salt walls Graben in the southern North Sea (Nalpas & Brun, 1993), in the centre of the graben and salt anticlines along its margins and in the offshore Campos, Santos and Espírito Santo basins (Warsitzka, Kley, Jähne-Klingberg, & Kukowski, 2016, mod- on the Brazilian margin (Alves, Cartwright, & Davies, 2009; ified from Baldschuhn, Binot, Fleig, & Kockel, 2001), bound- Demercian, Szatmari, & Cobbold, 1993), among others. ing minibasins which may contain different stratigraphies. The extensional geometry of this part of the Maestrat Basin is evident after restoration at the base-Upper Cretaceous level. This geometry resembles other preserved salt basins of 6.2 | Diapiric evolution of the Maestrat Europe located away from the Iberia-Africa and Iberia-Europe Basin in the Iberian microplate framework plate boundaries, which experienced little to no modification by Alpine compression. The depocentre of the SE part of The halokinetic evolution of the Maestrat Basin shares a sim- the Iberian Basin is 120- to 140-km wide (Salas et al., 2001; ilar history with other salt basins in Iberia during the Jurassic VERGÉS et al. 1677 EAGE |

EasternBetics Basque-Cantabrian Asturian basin Platekinematic model basinonshore offshore Iberia-Europe; point42.8 N, 2.0 E, present day Miocene

Oligocene

Eocene Rejuvenateddiapir squeezing & secondarywelding Paleocene Maastrichtian

Campanian

Santonian Coniacian Turonian Cenomanian

Albian Salt anticline Salt wall Aptian primarywelding

Barremian Hauterivian Salt wall faultcollapse& Valanginian salt extrusion Berriasian

Upper Jurassic Salt anticline Middle earlysalt Jurassic mobilization

Lower Jurassic

Late Triassic Earlysaltmobilization Reactive andactivediapirism Passive diapirism Diapir rejuvenation e.g.,15=locationsinFig.1

FIGURE 14 Compilation of the main diapiric phases that occurred in the diapiric provinces described for the Iberian Peninsula; dashed lines indicate uncertain ages for the corresponding diapiric phases. The interpretation of diapiric stages from the Iberian Range is based on field evidence listed in the figure and detailed in previous sections of this paper. Time scale according to Gradstein and Ogg (2012). Numbers and letters next to red circles refer to locations in Figure 1 and Early Cretaceous and was possibly influenced by the & Rubinat, 2012) and probably also in the South-Central larger scale Mesozoic and Cenozoic tectonic evolution of the Pyrenees (Cámara & Flinch, 2017; Saura et al., 2016). Iberian microplate (Figure 14). Diapiric activity seems to have diminished or even completely Widespread Upper Triassic salt diapirism was active in stopped during the Late Cretaceous in the Maestrat Basin. In most of the extensional basins within the Iberian microplate contrast, this period corresponds to widespread diapiric ac- during the Mesozoic (e.g. Vergés et al., 2019), including: the tivity in other areas of the Iberian Peninsula (Figure 14). In Basque-Cantabrian Basin (Bodego & Agirrezabala, 2013; the Pyrenees, the development of listric faults detaching on López-Horgue et al., 2010; Poprawski et al., 2014, 2016; Triassic evaporates, created raft systems, which were active Quintà et al., 2012), the Pyrenean Basin (Canérot et al., 2005; during the Late Cretaceous up to the onset of inversion as- Jammes et al., 2010; Lopez-Mir et al., 2014; McClay et al., sociated with the Alpine orogeny (Cámara & Flinch, 2017; 2004; Saura et al., 2016), the Iberian Basin (Canérot, 1991), López-Mir, Muñoz, & García-Senz, 2015; Saura et al., 2016). the Betic Basin (Martínez del Olmo et al., 2015; Pedrera In the diapiric areas of the Atlantic, the Basque-Cantabrian et al., 2014), the Algarve Basin (Ramos et al., 2016) and the and Asturias basins and the Bay of Biscay, both raft tectonics Lusitanian Basin (Alves et al., 2003). In all of these regions, and passive diapirism were active during this period result- salt tectonics occurred during Jurassic and Early Cretaceous ing in very well-developed diapiric structures (Cámara, 2017; times, and most show evidence for reactivation during Alpine Ferrer et al., 2012; Zamora et al., 2017). compression starting in the Late Cretaceous and continuing In the study region, Alpine reactivation of the precom- into the Miocene (Figure 14). pressional diapiric structures is indicated by the Teruel di- From the Late Jurassic to late Early Cretaceous, a major apir within the Iberian Range, which was active during the transcurrent-transtensional event has been determined along Tortonian–Messinian (e.g. Alonso-Zarza & Calvo, 2000). the Europe-Iberia plate boundary according to Nirrengarten, Elsewhere, in the Pyrenean, the Betic-Rif and Iberian fold Manatschal, Tugend, Kusznir, and Sauter (2018). Late and thrust belts, the large number of diapir reactivations Jurassic–Early Cretaceous extensional rifting reactivated during Alpine shortening, and their widespread distribution diapirs and listric fault systems in the Basque-Cantabrian suggests that this phenomenon is regional, and that the role and Asturias basins (Cámara, 2017; Zamora, Fleming, & of salt mobilization during the Mesozoic extension was very Gallastegui, 2017), the Bay of Biscay (Ferrer, Jackson, Roca, important. This has been recently established by detailed 1678 VERGÉS et al. | EAGE tectono-sedimentary studies of high-quality northern Iberian as indicated by well-exposed typical salt-related fea- outcrops (e.g. Cámara, 2017; Cámara & Flinch, 2017; tures (salt walls, collapse normal faults, hook and flap Canérot et al., 2005; Ferrer et al., 2012; López-Horgue et al., geometries), and unambiguous halokinetic depositional 2010; López-Mir et al., 2015; Poprawski et al., 2014; Saura sequences that are documented in three examples, in- et al., 2016; Zamora et al., 2017; among others). dicating protracted salt movement starting during the In the large-scale Atlantic-Tethys context, Jurassic open- Jurassic and extending to the Albian at least. ing of the northern domain of the Central Atlantic triggered 2. The Miravete anticline is interpreted as a diapiric anti- the southeastward transtensional drift of Africa with respect cline, despite the scarcity of outcrops of Upper Triassic to Iberia and Europe, forming the highly segmented Ligurian- evaporites. The growth of Miravete occurred over tens of Tethys ocean and margins. Considering the segmented na- millions of years during the Jurassic and especially dur- ture of the Jurassic plate boundary defined by several authors ing the Early Cretaceous. Halokinesis developed in four (Frizon de Lamotte et al., 2011; Handy, Schmid, Bousquet, stages, including the last one related to the Alpine shorten- Kissling, & Bernoulli, 2010; Sallarès et al., 2011; Schettino ing that defines the present shape of the anticline. & Turco, 2011; Vergés & Fernàndez, 2012), the NW-SE 3. This halokinetic interpretation is supported by the core Iberian-Maestrat Basin can be considered as a transform zone of the anticline interpreted as a subvertical salt weld or of the Ligurian-Tethys margin limiting the two ENE-WSW thrust-weld, separating two steep flanks with opposing margin of the Betics and NE-SW Catalan Coastal Ranges. orientations and different stratigraphies and ages, which According to the model of Nirrengarten et al. (2018), the correspond to halokinetic depositional sequences of the Iberian plate during the Jurassic, is marked by a period of Jurassic and Early Cretaceous. relative tectonic quiescence in the relative movement of the 4. The Miravete salt anticline started to grow during the Iberian plate with respect to Europe (Figure 14). This wide- Jurassic, as indicated by thin platform sequences of this spread extensional phase ended in the Early Cretaceous, age separated by angular unconformities attributed to coinciding with the northward propagation of the Mid- early salt movement along the central segment of the salt Atlantic Ridge across the south Newfoundland-Iberia margin weld (stage 1). (Nirrengarten et al., 2018). This crucial event triggered the 5. During the Hauterivian–Early Barremian, the central sec- large transtensional motion of Iberia relative to the rest of tor of the Miravete salt anticline evolved as a salt wall Europe, with an eastwards movement of the Iberian micro- ridge along which the El Castellar and Camarillas depos- plate of about 720 km during Early and Late Cretaceous up to its onlapped an already developed palaeotopography. This late Santonian at 83.5 Ma. The faster eastwards drift occurred period was also characterized by the collapse of the west- over about 28 Myr from earliest Cretaceous to the earliest ern flank of the salt anticline along a 10-km-long N-S fault Albian at a rate of 20 mm/year, followed by a slower period system, west-dipping and subparallel to the edge of the of drift of 8 mm/year. It is interesting to note the synchroneity diapir. Potential extrusion of salt along its footwall may of the highest drift motion of the Iberia microplate with the occur (stage 2). highest diapiric activity in the Maestrat Basin (Figure 14). 6. During the Late Barremian–Aptian times, the anticline evolved as either a salt anticline or as a salt wall influ- encing the growth of carbonate platforms (Xert, Forcall, 7 | CONCLUSIONS Villarroya de los Pinares and Benassal formations) as indicated by the apparent reduction in thickness along the cr- A halokinetic model for the origin of the Miravete anticline is estal domain. The progradation directions of the Villarroya the best model for explaining the structural and stratigraphic de los Pinares is at a high angle to the anticline trend in- observations made in the field. Earlier models, based solely dicating that their deposition was influenced by the rising on Alpine reactivation of normal faults do not adequately diapiric ridge up to the end of the Albian (stage 3). explain the facies distribution patterns, platform prograda- 7. Regionally, the well-exposed Castel de Cabra salt an- tion directions, formational thickness variations on oppo- ticline and Cañada Vellida salt wall diapiric structures site flanks of the anticline, intraformational unconformities, confirm the widespread diapirism during the Jurassic and nor the progressive changes in bed orientation with distance Early Cretaceous in the Maestrat Basin. The NE flank of from the anticline core, all of which strongly suggest an the Cañada Vellida salt wall is characterized by hook pat- actively growing structure from the Jurassic through Early terns and by a 500-m-long upturned flap, comprising thin Cretaceous. The following conclusions summarize the pro- Upper Jurassic carbonates. An incomplete 500-m-thick posed halokinetic model and its implications. Lower Cretaceous succession onlaps against the flap during the infilling of the SW flank of the Aliaga minibasin. 1. Widespread diapiric structures are recognized for the first 8. An E-W trending regional cross section across the time in the Miravete anticline and surrounding structures Ababuj, Miravete and Cañada-Benatanduz anticlines was VERGÉS et al. 1679 EAGE | constructed, representing distinctive geometries of salt-re- Alnazghah, M. H., Bádenas, B., Pomar, L., Aurell, M., & Morsilli, M. lated rift basins. The diapiric development and its control (2013). Facies heterogeneity at interwell-scale in a carbonate ramp, Upper Jurassic, NE Spain. Marine and Petroleum Geology, 44, 140– on the growth of salt anticlines and diapir walls were sig- 163. https://doi.org/10.1016/j.marpetgeo.2013.03.004 nificant and partially decoupled from basement faults. The Alonso-Zarza, A. M., & Calvo, J. P. (2000). Palustrine sedimentation in Camarillas and Fortanete minibasins already displayed an episodically subsiding basin: The Miocene of the northern Teruel bowl geometries at the onset of Palaeogene shortening Graben (Spain). Palaeogeography, Palaeoclimatology, Palaeoecology, (stage 4). 160(1–2), 1–21. https://doi.org/10.1016/S0031-0182(00)00041 -9 9. The most active period of diapiric growth in the Maestrat Alvaro, M., Capote, R., & Vegas, R. (1979). Un modelo de evolución Basin occurred during the Early Cretaceous and this was geotectónica para la Cadena Celtibérica. Acta Geológica Hispánica. Homenage a Lluís Solé I Sabarís 14 also recorded in the Eastern Betics, Asturias and Basque- , , 172–177. Alves, T. M., Cartwright, J., & Davies, R. J. (2009). Faulting of salt-with- Cantabrian basins. This period coincides with the peak of drawal basins during early halokinesis: Effects on the Paleogene Rio eastward drift of the Iberian microplate at rates of 20 mm/ Doce Canyon system (Espírito Santo Basin, Brazil). AAPG Bulletin, year, followed by a decreased rate of 8 m/year in earliest 93, 617–652. https://doi.org/10.1306/02030908105 Albian time. Deviatoric stresses related to plate kinemat- Alves, T. M., Gawthorpe, R. L., Hunt, D. W., & Monteiro, J. H. (2003). ics thus possibly playing a role in diapiric evolution. Post-Jurassic tectono-sedimentary evolution of the Northern Lusitanian Basin (western Iberian margin). Basin Research, 15(2), ACKNOWLEDGEMENTS 227–249. https://doi.org/10.1046/j.1365-2117.2003.00202.x Arche, A., & López-Gómez, J. (1999). Tectonic and geomorphic con- This work was funded by Equinor Research Centre, trols on the fluvial styles of the Eslida Formation, Middle Triassic, Bergen (Norway), by the Spanish Ministry of Economy Eastern Spain. Tectonophysics, 315(1–4), 187–207. https://doi. and Competitiveness Projects ALPIMED (PIE-CSIC- org/10.1016/S0040-1951(99)00291-7 201530E082) and SUBTETIS (PIE-CSIC-201830E039) Arche, A., & López-Gómez, J. (2005). Sudden changes in fluvial with additional support from the Generalitat de Catalunya style across the Permian-Triassic boundary in the eastern Iberian grant AGAUR 2017 SGR 847. We thank Toni Mestres for Ranges, Spain: Analysis of possible causes. Palaeogeography, the drone photographies. We also thank Emilio Casciello, Palaeoclimatology, Palaeoecology, 229(1–2), 104–126. https://doi. Eduard Saura and Giulio Casini for scientific discussions and org/10.1016/j.palaeo.2005.06.033 Aurell, M., Bádenas, B., Canudo, J. 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