The Iberian Middle Jurassic carbonate-platform system: Synthesis of the palaeogeographic elements of its eastern margin (Spain)

1.1. G6mez a,*, S.R. Femandez-L6pez b

a Dpto. EstratigTajia, Facultad de Ciencias Geologicas (UCM) e lnstituto de Geologia Economica, (CS1C-UCM), 28040 Madrid, Spain b Dpto. Paleontologia, Facultad de Ciencias Geologicas (UCM) elnstituto de Geologia Economica, (CSIC-UCM), 28040 Madrid, Spain

Abstract

During the Middle Jurassic, the domain of the Iberian and Catalan Coastal ranges of eastern Spain was occupied by a system of fault-controlled carbonate platforms that flanked the Iberian Massif to the East. This platform system marked the transition between the shelves of the Alpine Tethys and the Central Atlantic Ocean. The palaeogeographic reconstruction of the Iberian Middle Jurassic platfOlm system is based on more than 199 surface sections and 37 wells. From southwest to northeast, eight main palaeogeographic elements with associated characteristic facies are recognized. These represent a system of horsts and grabens. In the southwest, the Internal Castilian Platform is characterized by the frequently dolomitized oolitic and restricted facies of the Yemeda FOlmation. To the nOliheast, the NW-trending open-marine carbonate environments of the External Castilian and Aragonese platforms were separated by the fault-controlled El Maestrazgo High that is characterized mainly by the dolomitized Rafales Formation. The External Castilian and Aragonese platforms consist from bottom to top of the micro filament mudstones to wackestones of the El Pedregal Formation, the bioclastic and oolitic grainstones to packstones of the Moscardon FOlmation, and the Domefio Formation, that reflects a return to an open-marine low-energy wackestone to mudstone facies, locally containing patches of oolitic grainstones. The highly subsiding Tortosa Platform, represented by the Sant Blai, Cardo and La Tossa formations, is bounded by the dolomitic facies deposited on the El Maestrazgo and the TalTagona highs, and by the Catalan Massif where no Middle Jurassic deposits have been recorded. The open-marine facies and condensed sections of the Beceite Strait separated the Aragonese and Tortosa platforms. A regional stratigraphical gap spanning the upper Callovian Lamberti Zone to the lower Oxfordian Cordatum Zone is evident. A system of northwest- and nOliheast-trending normal faults controlled thickness and facies distribution. Data from the Iberian carbonate-platform system indicate that expanded sections were not necessarily associated with open-marine environments. Condensed and expanded sections are developed in open and restricted-marine facies, even on such palaeogeographic highs as the El Maestrazgo High. Restricted and shallow-marine environments occasionally developed in patis of the External Castilian Platform.

Keywords: Middle Jurassic; Carbonate platforms; Stratigraphy; Palaeoenvironments; Palaeogeography; Spain

1. Introduction

Regional Middle Jurassic palaeogeographic recon­ structions of the early opening stage of the Central * Corresponding author. Tel.: +34 913944783; fax: +34 913944808. E-mail addresses: [email protected] (J.J. G6mez), Atlantic Ocean and the Alpine Tethys indicate that the [email protected] (S.R. Femandez-L6pez). East-Iberian area was occupied by a carbonate-plat- form system, the fades development and subsidence analysed in these areas 199 Middle Jurassic surface patterns of which were controlled by active faults (Fig. sections and data from 37 boreholes (Fig. 2). This 1; Ziegler, 1990; Bassoullet et aI., 1993; Enay et aI., permitted us to develop a detailed reconstruction of 1993; Thierry, 2000; Vera, 2001, 2004; Vera et aI., the palaeogeographic elements of the East-Iberian 2001; Stampfli and Borel, 2004). Middle Jurassic carbonate-platform system. In the ibe­ In the fold-and-thrust belts of the Iberian and Cat­ rian Range, Middle Jurassic carbonates, formerly at­ alan Coastal ranges of Spain, which evolved by Pa­ tributed to the "middle portion" of the Chelva leogene inversion of Mesozoic rifted basins (Salas et Formation (Gomez and Goy, 1979), were recently aI., 2001), Middle Jurassic carbonates are exposed subdivided into several hthostratigraphic Wlits Wlder outstanding outcrop conditions over a distance (Gomez and Fernandez-Lopez, 2004a,b) on the basis of more than 500 km. In the context of our studies, we of their distinct fades development that can be related

� Cratonic Shallow mann&­ Oceanic � high D continental basin basin

Fig. 1. Middle Jurassic palaeogeography of the Western Tethys and the Proto-Atlantic Ocean (Ziegler, 1990; Stampfli and Borel, 2004; modified) and location of the studied area. Ab: Alboran. Ad: Adria s. str. Ap: Apulia s. str. Bu: Bucovinian. CL: Campania Lucania. Cn: Carnic-julian. GB: Grand Bank. hA: High Atlas. He: Helvetic rim basin. Ig: Igal trough. La: Lagonegro. LBM: London-Braband Massif. mA: Middle Atlas . MC: Massif Central High. NFB: East Newfmmdland Basin. Pa: Panonnides. PI: Pelagonian. Se: Sesia (western Austroalpine) . Si: Sicanian. SI: Slavonia. Tu: Tuscan. Tz: Tizia. UM: Umbria-Marches. to their palaeogeograpbic setting (Fig. 3). In the Cat­ environments, Wlder which low-energy fossil-rich am­ alan Coastal Range, Cadillac et al. (1981) and Fernim­ monite-bearing fades developed, suggesting that they dez-L6pez et al. (1996, 1998) had analysed the were partly connected to the open ocean (AureU et aI., lithostratigraphy of Middle Jurassic deposits. Detailed 2002, 2003; Fernimdez-L6pez and G6mez, 2004). From palaeontological studies of these deposits, containing southwest to northeast, eight main palaeogeographic ammonites, allowed for a high-resolution biostrati­ elements can be recognized that were associated with graphic subdivision of this sequence at the scale of characteristic facies, and that represent a horst and zones, subzones and horizons (Hinkelbein, 1975; graben system (Fig. 4). In the southwestern area, the G6mez, 1979; Pemandez-L6pez, 1985; Melendez, Internal Castilian Platform was attached to the Iberian 1989). In this study, biostratigraphical data are referred Massif. To the northeast, the fault-controlled El Maes­ to the standard zones of ammonites. trazgo High sepamted the NW-trending open-marine During the Middle Jurassic, the so-called Iberian External Castilian and Aragonese carbonate platforms. Basin was occupied by a complex system of epiconti­ The highly subsident Tortosa Platform was delimited to nental carbonate platforms that in many cases were the north by the Tarragona High and the Catalan Mas­ tectonically controlled. Up-thrown blocks formed sif, that are devoid of Middle Jurassic deposits, and to palaeogeographic highs that were characterized by shal­ the south by the El Maestrazgo High. The Beceite Strait low-water depositional environments. Areas between fonned a tmnsitional area between the Aragonese and these highs were largely dominated by open-marine the Tortosa platforms.

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�" " I'VALENClA • Oil well 01020 3040 50 km The main objective of our study was to synthesize showing planar and through cross-bedding, wave rip­ the palaeogeography and facies distribution on the ples, bioclastic rills and bioturbation. Locally, low eastern margin of the Iberian carbonate-platform sys­ angle planar cross-lamination, algal laminae and fenes­ tem. The different fault-bounded platfonns show char­ tral porosity occur. Common are thickerung- and coars­ acteristic facies variations, ranging from restricted and ening-upward sequences generated by the migration of shallow-marine to open and deep-marine environ­ oolitic bars over low-energy restricted mudstones to ments that are associated with condensed and expand­ wackestones. Similarly, successions of calcareous oo­ ed sections (G6mez and Fernandez- L6pez, 1994; litic and bioclastic grainstones are common. Thickness 2004a,b; Ferruindez-Lopez and Gomez, 2004). of the Yemeda Fonnation in the type section (YE in Fig. 2; Gaibar-Puertas and Geyer, 1967, 1969; Vial­ 2. Internal Castilian Platform lard, 1973) attains about 250 m, marking a subsident area that defmes the Enguidanos Depocentre (Fig. 4; The Middle Jurassic Internal Castilian carbonate plat­ Femindez-L6pez and G6mez, 2004; G6mez and Fer­ fonn flanks the Iberian Massif to the east (Fig. 4). It is nandez-L6pez, 2004a). Another reference section is the characterized by the high-energy oolitic bars and asso­ Embalse de Contreras section, where this unit exceeds ciated low-energy, restricted shallow-marine facies of a thickoess of 225 m. Partial sections from Buenache the Yemeda Formation. Owing to successive post-Juras­ de la Sierra and La Toba have been described by sic erosional events, the transition between these carbo­ Viallard (1973) and Morillo-Velarde and Melendez­ nates and a continental facies is no longer preserved. Hevia (1981). The most fossiliferous deposits of this This lithostratigraphic unit consists of oolitic grain­ restricted internal platform area contain occasional stones to packstones, sometimes including ooids and/or remains of benthic organisms such as bivalves, echi­ bioclasts, which are interbedded with calcareous mud­ noids, calcareous algae, bryozoans, brachiopods, for­ stones to wackestones that can be the dominant facies aminifers and gastropods. Ammonites and belemnites in some areas. These carbonates, which are stratified are very scarce or absent in the whole unit. Yet, in the into thick beds, are locally partial or entirely dolomi­ Yemeda section, where micritic low-energy restricted tized. The unit often contains grainstone to packstone facies dominate, exceptionally Bajocian stephanocera­ bodies which display a well preserved bar morphology, tids in its lower and middle part, and Procerites,

Fig. 2. Outcrops of the lurassic sediments in the Iberian Range and in the Catalan Coastal Range, shov.ring the sections and wells studied in this work. Abbreviations of the surface sections: AA: Aras de Alpuente. ACI: Alcublas-I. AC2: Alcublas-2. AC3: Alcublas-3. AC4: Alcublas-V AF: Alfara. AG: Aguaton. AH: Almohaja-N. AJ: Areos de lalon. AL: Albarracin. ANI : Andorra-I. AN2: Andorra-2. AN3 : Andorra-3. AO: Alcotas. AP: Arroyo Picastre. AR: Arilio. AS: Alcorisa-E. AT I: Alustante-S. AT2: Alustante-E. AU: Aguilon. AV: Barranco del Av ellanar. AZ: Adzaneta­ NE. BB: Ababuj . BC: Balneario de Cardo. BD: Barranco de la Cedrilla. BE: Barranco de las Estacas. BG: Rio Bergantes. BH: Barranco de la Hontanilla. BI: Barranco de Milles. BL: Barranco de Valdecastillo. BM: Barranco Moro. BN: Buenache de la Sierra. BO: Barranco Las Ennitas. BP: Barranco del Sapo. BS: La Buenafuente del Sistal. BT: Beceite. BU: Buiiol. BV: Barranco del Vall. BZ: Belchite. C: Barranco La Canalej a. CA: Caudiel. CB: Corbalan-E. CD: Cedrillas. CE: Cella. CG: Coll de l'Argila. Cl: Chilches. CL: La Cerredilla. CM: Campillos-Paravientos. CN: Canales. CN: Caiiada Ve llida. CO: Codes. CR.: Bronchales. CS: Cap de Salou. CT: Villar de Cobeta. CU: Concud. CV: La Caiiada de Verich. CW: Corbalan-W. CHI: Alcoroches-W. CH2: Alcoroches-N\V. D: Molino Romedianos. DG: La AlmlUlia de Dofia Godina. DM: Domei'io. DR: Aladren. EB: Embalse San BIas . EC: Coll del Caragol. EG: En Grillo. EH: Embalse de Hijar. Ell: Ej ulve-SW. El2: Ejulve- S. ERI : El Coscojar. ER2: Entrambasaguas. ET: Embalse de Contreras. EZ: El Cabezo. FN: Frias de Alb arracin-N. FS: Frias de Albarracin-S. FW: Frias de Albarracin-W. FZ: Fuentelsaz. G: Rambla La Gotera. GA: Gea de Albarracin. GC: Graj a de Campalbo. GE: Embalse del Generalisllno . GI:Aliaguilla. GP: Embalse de Gallipuen. GS: Gaibiel-S. GU: Guadalaviar. GW: Enguidanos-N\V. HP: Hoya del Peral. HR.: Barranco del Chorrillo. HT: Hontanar. HU: Huerguina. RV: Chelva. ll.,: Cillas. lA: laulin. 10: Henarejos. lV: lavalambre. LC: La Cierva. LD: Lidon. LE: Lecera. LH: Las Higueruelas. LM: La Olmeda. LO: Coscollosa. LV: Les Vo ltes. LL: Llaberia. M: Moscardon. :MA: Mas Nueva. MC: Masia de la Sisca. MD: Masada del Diablo. ME: Maranchon­ SE. MG: Monteagudo de las Salinas. MI: Miravete. ML: Molinos. :MN: Montoro. MO: Montornes. MR Mas Riudoms. MS: Maranchon-S. MT: Masada Toyuela. MU: Montes Universales. :MY: Moneva-E. MY: Moyuela. NA: Buefia. NE: Alcaine. NG: Noguera. Nl: Montanejos. OE: Miravet. OG: Oj os Negros. ON: Obon-N. OS: Oset. OW: Obon-W. P: Sagunto. PA: Palomar de Arroyos. PC: Puerto del Caballo. PD: Pancrudo. PE: Peracense. PI: Espina. Pl: Pajaroncillo. PL: Pinilla de Molina. PMI: Areos de las Salinas. P:M2: La Puebla de San Miguel-2. PM3: La Puebla de San Miguel-3. PN: Pina de Montalgrao. PP: Rio Pena. PT: Peralej os de las truchas . PZ: El Pedregal. RB: Ribarroj a. RC: Ricla. RE: Rubielos de la Cerida-E. RF: Rafales. RG: Ribagorda. RJ: Torrijas. RN: Renales. RO: Revolcadero-Cucutas. RR: Barranco del Grevolar. RS: Rambla del Salto. RT: Carlades-L'Embarronat. RV: Riodeva. RW: Rubielos de la Cerida-W. SA: Sarrion. SB: Sant Blai. SC: Sot de Chera. SE: Santa Eulalia. SI: Siete Aguas-NE. SL: Salada. SM: Santa Cruz de Moya. SN: Sinarcas-N. SP: Sierra de El Pobo. SR Serretilla. ST: Rio de Estrets. SU: Sierra de la Bicuerca. TA: Torre las Areas. TB: La Toba-S. ID: Tordellego. TE: La Toba-E. TI: Toril. Tl: Tuejar. TL: Tejadillos. TM: Tonnon. TO: Tosos. TQ: La Tranquera. TR Checa-SW. TT: Beteta. TU: Tunniel. TV: TIvissa. TY: Tivenys. UA: Ufia. US: Chuvellus. V: Va llanca. VB: Vistabella del Maestrazgo-E. VC: Villar del Cobo. VD: Poveda de la Sierra. VF: Fordenchana. VII: Villar del Humo. VI: Villel. VN: Vandellos. VS: Valsalobre. VT: Villar de Tejas. XP: Xerta-Pauls. YE: Yemeda. YU: Talayuelas. ZA: Zafrilla. reineckeids and hecticoceratinae of Bathonian and Cal­ bivalves (microfilaments ), echinoderms and pellets. lovian age in its upper part have been found (Gaibar­ These may contain interbedded marls, sometimes bio­ Puertas and Geyer, 1967, 1969; and unpublished data clastic, which in the upper part of this unit locally of the authors). constitutes an alternation of marls and limestones. High-energy facies belts, reflecting the action of Chert nodules are common in limestones. In the basal waves, tides and storms, characterize the shallow­ parts of this formation, interbedded horizons consisting water Middle Jurassic Internal Castilian carbonate plat­ of limestones containing ferruginous and/or phosphatic form. It corresponds to a belt of bars and charmels and ooids are common (Geyer et aI., 1974). These are is characterized by high rates of carbonate production associated with the strati graphical gap that is located and accumulation. Oolitic and bioc1astic grainstone bars at the base of the El Pedregal Formation. On the system is associated with washover and beach facies. Aragonese Platform, ferruginous and/or phosphatic Low energy micritic facies were deposited between ooids are also common in the uppermost levels of this these high-energy bars and in extensive lagoons, as unit (Mouterde et aI., 1978; Fernimdez-L6pez, 1985; well as tidal flat deposits. In the southern parts of the G6mez and Ferruindez-L6pez, 1994). In the NW Exter­ Castilian Platform, the Montes Universales Fault marks nal Castilian Platform, peritidal dolomitic limestones the bOWldary between its internal and external areas. In and mudstones, showing microbial laminae and mud­ the northern parts of the Castilian Platform, the bound­ cracks (Fernimdez-L6pez, 1997), as well as oolitic grain­ ary between internal and external areas is more transi­ stones, are interbedded in the lower part of the sections tional, delineating a northwestern-trending belt of fine­ (Fig.5 ). Mounds formed by volcanic rocks occur on the grained limestones, oolitic, bioc1astic and oncolitic SE External Castilian Platform (Figs. 4 and 5; Gautier, packstones to grainstones and dolomitic deposits that 1968, 1974; G6mez et aI., 1976; G6mez, 1979, 1985a,b; are organized into shallowing-upward sequences. South Orti and Vaquer, 1980; Fernimdez-L6pez et aI., 1985; of La Mancha Fault, the oolitic facies continues south­ Martinez Gonzalez et aI., 1997, 1998; Cortes, 2001). In ward, but its chronostratigraphic attribution is still Wl­ the NW and Central Castilian platforms, sponge build­ certain in these areas. The Montes Universales and La ups and marls are common in the upper part of the El Mancha faults delineate a rapidly subsiding area that Pedregal Formation (Fig. 5; Fernimdez-L6pez et aI., corresponds to the Enguidanos Depocentre in which 1978; Fernandez-L6pez, 1985; G6mez, 1985a,b, 1991; tectonically controlled subsidencerates were fully com­ Friebe, 1995). Zoophycos and Thalassinoides are com­ pensated by sedimentation rates, as evidenced by the mon, and occasionally bioclastic rills, ferruginous crusts, persistence of shallow-water restricted facies during and remobilization surfaces are recognized. These ich­ most of Middle Jurassic. nofossils are widely represented in external platform facies of the Middle Jurassic deposits, ranging from 3. External Castilian and Aragonese platforms restricted and shallow to open and deep environments (Fernandez-L6pez, 1997; Olivero, 2003; Knaust and On the External Castilian and Aragonese carbonate Hauschke, 2004). platforms, which outcrop in the Iberian Range, most The El Pedregal Formation is generally organized of the Middle Jurassic is represented by open-marine into shallowing-upward sequences, usually composed facies that commonly contain ammonites, allowing for of a lower marly and an upper calcareous part, which is a high-resolution biostratigraphic zonation (Hinkel­ bioturbated and, on occasions, contains build-ups of bein, 1975; Fernandez-L6pez, 1985; Fernandez­ sponges and algae or dolomitic facies. The tops of L6pez and G6mez, 1978; Melendez, 1989). Three many of these sequences are marked by hardgroWlds, lithostratigraphic Wlits are recognized, that can be fol­ which are characterized by borings, ferruginous crusts, lowed over the entire Iberian Range, and which permit glauconitic, phosphatic and bioc1astic carbonates, as a detailed reconstruction of the palaeogeographic and well as reworked fossils (reelaborated and resedimented palaeotectonic evolution of these platforms. From bot­ fossils in Fernimdez-L6pez, 1991). tom to top, these are the El Pedregal, Moscardon and The thickness of the El Pedregal Formation reaches Domefio formations. more than 150 m in the Pozuel and Casinos depocentres (Fig.4 ). On the Central External Castilian Platform the 3.1. El Pedregal Formation thickness of this unit varies between 60 and 80 m. On the Aragonese Platform, remarkable thickness varia­ The El Pedregal Formation consists of lime mud­ tions are observed, ranging between 8 m in the stones and wackestones containing bioc1asts, mainly Andorra-l section and 45 m in the Ricla section (Fig.2 ). CATALAN COASTAL RANGE

Domet1OFm

La TossaFm Domet1OFm

Fig. 3. Middle Jurassic lithostratigraphic lUlits and the shallowing and deepening cycles of the Iberian and Catalan Coastal ranges, referred to the chronostratigraphical lUlits.

Remains of ammonites, belemnites and benthic itation of connections with open-sea Atlantic and West­ organisms, such as bivalves, brachiopods, echinoderms, ern Tethys waters. serpulids, gastropods, bryozoans, sponges and calcare­ ous algae, are abWldant in some levels. The base of the 3.2. Moscardon Fonnation El Pedregal Formation coincides with the upper part of the Aalenian Murchisonae Zone, although Aalenian and The Moscardon Formation consists mainly of bio­ lower Bajocian deposits are usually included in con­ clastic grainstones to packstones on which crinoids, densed sections, whilst its top is slightly diaclrronous at ooids and intraclasts are sometimes abWldant. Bioclas­ a regional scale. It corresponds to the Bajocian Nior­ tic wackestones and mudstones are locally represented. tense and Garantiana zones (Figs. 3 and 5). The Wlit, which commonly forms steep escarpments, is The El Pedregal Formation was deposited on an usually bedded in layers which may surpass 3 m in external platform, dominated by low-energy, open-ma­ thickness. Chert nodules as well as Zoophycos and rine, normal salinity, shallow-water environments, oc­ Thalassinoides are locally common. Among the sedi­ casionally affected by storms. Microbial laminae, mentary structures,planar and festoon cross-lamination, mud-cmcks and karstification smfaces indicate local, ripples, bioclastic rills, and sedimentary bodies showing occasional emersion in mudstones related to deposi­ bar morphology are common. On the Aragonese Plat­ tion in confined shallow-marine environments (Fernan­ form, the Moscardon Formation consists of calcareous dez-L6pez and G6mez, 1990b). In the upper part of the packstones to boundstones forming sponge build-ups El Pedregal Formation, facies, taphonomy and palaeo­ (Fig. 5; Femimdez-L6pez and Aurell, 1988). These biological evidence (Fernandez-L6pez and G6mez, lithologies and structures are generally organized into 2004) indicate depth increasing and, presumably, facil- shallowing-upward sequences with a lower part of cal- Cosoblonco-I +

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Fig. 4. Palaeogeographic reconstruction of the different platfonns inthe eastern margin ofthe Iberian platform system during Middle Jurassic. From southwest to northeast the Internal Castilian Platform, the External Castilian Platfonn, divided into the NW, Central and SE External Castilian platforms, the El MaestrazgoHigh, the AragonesePlatform andthe Tortosa Platform, linked by theBeceite Strait, the Tarragona Highand the Catalan Massif.

AAAGONESE PlATFORM NW NW

Limestones with sponges, Dolornitic facies � � including buildups _ Mori and limestone Ootitic groinstone and Rock of volcanic origing, r:-:-:l Mudstone and wackestone � pockstone _ forming mounds RI � Mudstone artd wackestone Crionoidol grainstone and Condensed section, locally _ � in thick be}1s (I �ft) . and in _ with iron oaids. pockstone thin beds (righl) � Bioclastic rnudstone and Limestone and mort Main regional hiatus � wockestone _

Fig. 5. Chronostratigraphic correlation chart showing the fades distribution on the Aragonese and Castilian platfonllS. careous mudstones to wackestones, which can be ab­ 3.3. Domeno Formation sent or replaced by a basal reworked level, and an upper part consisting of calcareous gminstones to packstones. The Domefio Formation is generally composed of Other, locally developed, sequence types are filling well-stratified wackestones of micro filaments, locally sequences. Their lower parts consist of calcareous pack­ packstones and mudstones, commonly with pellets, that stones to wackestones that contain large bioclasts and are interbedded with marly limestones and calcareous reworked fossils, sometimes phosphatic and imbricated marls. In the southeastern part of the External Castilian whereas their upper parts are made of calcareous wack­ Platform, it contains mOWlds formed by volcanic rocks estones to mudstones which can show ripple lamina­ (Gautier, 1968, 1974). Insome localities of the External tions. The thickness of the Moscardon Formation varies Castilian and the Aragonese platfonns, lenticular bodies on the Central External Castilian P latfonn between 3 of grainstones, containing calcareous ooids, are overly­ and 25 m (Fernimdez-L6pez, 1985), decreases towards ing the uppermost carbonates of the Moscardon Forma­ its SE parts where it is represented by a few meters of tion (e.g. Rambla del Salto, Aguaton, Obon-W and calcareous wackestones to packstones containing cal­ Andorra-l sections, respectively, Fig. 2). The Domefio careous ooids, and [mally pinches out near the Medi­ Formation locally contains chert nodules, and Thalas­ terranean coast. On the Aragonese Platform, the sinoides and Zoophycos are common. In the Iberian thickness of these bioclastic facies, containing crinoids Range, the top of the Middle Jurassic series is generally and sponges, reaches 23 m in Ricla and 17 m in the associated with ferruginous crusts and ferruginous Belchite sections (Sequeiros et aI., 1978; Fernandez­ ooids, fonnally defmed as the Anoyofrio Bed L6pez and Aurell, 1988). Laterally the Moscardon (G6mez and Goy, 1979), which marks a regional strati­ Formation pinches out towards the southeast (about 2 graphical gap. m in the Obon-W section, Fig. 2) and is missing on the The Domefio Formation is organized into upward­ El Maestrazgo High. shallowing and -thickening sequences which are char­ The Moscardon Formation commonly contains di­ acterized by a basal level that includes reworked fossils, verse and abWldant macrofossils indicative of open­ an intermediate part of marly limestones, marls and marine environments, such as ammonites, belemnites limestones, and an upper part of limestones with irreg­ and sponges. Echinoderms, calcareous algae, bryozo­ ular bedding that is capped by ferruginous crusts and ans, bivalves, bmchiopods, serpulids, and gastropods borings. The Domefio Formation attains a thickness of are also abundant. The unit is bounded by stratigraphic 45 m at the type section and more in other outcrops of discontinuities. The oldest sediments correspond to the the SE External Castilian Platfonn (e.g. Chelva, Alcu­ Bajocian Garantiana Zone, as seen in the Moscardon bIas, Ribarroja and Sagunto sections, Fig. 2). In the and in the Ricla sections. However, the lowest deposits Central External Castilian Platform, its thickness is of this unit can belong to the Bathonian Zigzag Zone, as usually smaller than a dozen meters. In the NW Exter­ in the Puebla de San Miguel section (Fernimdez-L6pez, nal Castilian Platform, its thickness is of the order of 1985). The age of the top of this unit varies from the 100 m, where it constitutes the main sediments filling Bajocian Parkinsoni Zone up to the Bathonian Zigzag the Pozuel Depocentre. On the Aragonese Platfonn, Zone (Fernandez-L6pez, 1985). there are expanded sections which surpass a thickness The Moscardon Formation was deposited Wlder of 100 m (e.g. Ricla and Aguilon), and which grade into open-marine, normal salinity, high-energy and very condensed sections thinner than 15 m, such as in the shallow conditions providing for high carbonate pro­ Andorra, La Caiiada de Verich, Barranco de las Estacas duction and deposition rates during a brief episode. The and Obon sections (Fig. 2, Sequeiros and Melendez, External Castilian Platfonn was dominated by wave 1987; Aurell et aI., 1994). action and the progradation of high-energy facies over Open-marine bivalves, brachiopods, echinoderms, the low-energy, open-marine shallow facies of the El serpulids, ammonites, belemnites and gastropods are Pedregal Fonnation. On the Aragonese Platfonn, de­ common. The base of the Domefio Formation is dia­ velopment of the Moscardon Formation was condi­ chronous at the zone scale, varying in age from the tioned by the growth of sponge mud-moWlds, similar Bathonian Zigzag Zone (e.g. in the Domefio section) up to those recorded on the Castilian Platfonn in the El to the Bathonian Progracilis Zone. The limestones with Pedregal Fonnation. Towards the end of the Moscardon ferruginous ooids of this formation vary in age from Formation the sea bottom relief of the external platform Bathonian to Oxfordian. The upper Callovian Larnberti areas was largely infilled, giving rise to a brief phase of Zone and the lower Oxfordian Mariae Zone have so far widespread shall owing of the Iberian platfonn system. not been identified. The top of the Domefio Formation, generally corresponds to the Arroyofrio Bed, which mudstones containing rare macro fossils (Barranco de represents condensed sections (Figs. 3 and 5) and las Ermitas and Adzaneta sections). Bioturbation tex­ includes a hiatus of regional extent. tures and structures and bioclastic rills are common. The sediments of the Domefio Formation were de­ The most common sequences are upward-thickening posited on an open-marine, normal salinity, external and -shallowing, showing hardgrounds with borings carbonate platform, the palaeogeographic configuration that can be filled with ferruginous crusts and glauco­ of which was varied during early Bathonian to middle nite. In some areas where dolomitization does not Oxfordian times. During the Bathoruan and Callovian, affect the whole Middle Jurassic sequence (e.g. in the thermal subsidence of this external platform was the Rafales section), the restrictedfacies of the Rafales overprinted by synsedimentary faulting controlling dif­ Formation grade into the open-marine bioclastic wack­ ferential subsidence of individual blocks (Salas et aI., estones of the Domefio Formation that contains 2001). During late Callovian and early Oxfordian, the ammonites. The Wlit reaches a thickness of 26 m in External Castilian and Aragonese platforms became the Rafales section, where the lower contact is fault­ extremely shallow and uniform. The top of the controlled, and about 25 m in the Barranco de las Domefio Formation reflects a phase of widespread Ermitas and in the Adzaneta sections (Canerot et aI., homogenisation and emersion of these platforms and 1985b). These condensed sections pass latemlly into is associated with a hiatus that is recorded in the entire 100-250 m thick dolomitic sections, identified in oil studied area. wells (Bobalar-1 and 2, Maestrazgo-2 and Salsadella-1 wells in Fig. 2; Lanaja, 1987; Ferruindez-Lopez et aI., 4. El Maestrazgo High 1996, 1998). In areas where this Wlit is not dolomitized, During Middle Jurassic, the El Maestrazgo area remains of benthic organisms, such as bivalves, echi­ formed a high that was flariked by the open-marine noids, calcareous algae, sponges, bryozoans, brachio­ External Castilian, Aragonese and Tortosa platfOlTIls. pods and gastropods, are common. In contrast, This high was transected by a complex array of NW­ remains of nektic organisms, such as ammonites and NE-trending synsedimentary faults (Vinaros, and belemnites, indicative of open-marine conditions, Ateca, Castellon, Caudiel, Teruel, and Requena-Mora are very rare or absent. However, in the lowermost faults in Fig. 4), which delimited a series of tectonically part of the Rafales section (Fig. 2), the occurrence of active blocks (Canerot, 1974; Burrollet and Winnock, sonninids and stephanoceratids indicates an early 1977; Cadillac et aI., 1981; Canerot et aI., 1985a,b; Bajocian age, whilst in its upper part parkinsonids Ferruindez-Lopez et aI., 1996, 1998; Gomez and Fer­ suggest a late Bajocian age. At the transition between mindez-Lopez, 2004a,b). restricted and open-marine facies, as seen in the On the El Maestrazgo High, restricted marine, upper part of the Rafales Formation type section, commonly dolomitic carbonates, fonning 20--40 m this Wlit is covered by the ammonite-bearing carbo­ thick condensed sections, were deposited. However, nates of the Domefio Formation, that permit to iden­ oil wells drilled in this area indicate that on some tify Bathonian and Callovian zones. The Rafales subsiding fault blocks up to 100-250 m thick ex­ Formation was deposited in a restricted shallow-ma­ panded dolomitic sections were deposited, thus form­ rine environment that was characterized by intense ing the so-called El Maestrazgo Depocentre (Fig. 4). production and accumulation of carbonates. Bars and The Rafales Formation (G6mez and Fernimdez­ channel belts chamcterize high-energy facies, whereas Lopez, 2004a,b) includes the restricted carbonate fa­ low-energy facies are represented by dolostones with cies, and the transition between internal and external local muddy limestones. facies, that are associated with the El Maestrazgo High. 5. Tortosa Platform

4.1. Ra/ales Formation On the Tortosa Platform, expanded Middle Jurassic sections surpassing 350 m in thickness are composed of The Rafales Formation is generally composed of open-marine external platform facies and testify to its massive, crystalline dolomitic limestones. These pass rapid subsidence (Fig.6 ; Fernimdez-Lopez et aI., 1996, laterally into higher energy facies consisting of bio­ 1998; Gomez and Fernimdez-Lopez, 2004b). Although clastic grainstones to packstones with calcareous ooids thickening- and shallowing-upward sequences predom­ (e.g. in the Ejulve sections), as well as into calcareous inate, some deepening sequences occur locally during Aragonese Platform Tortosa Platform CID

Beceite Pass Alfara-Cardo Andorra Alcorisa Colcndo Block Block

� Oolitic cnd bioclostic pockstcne l:....:...... !J to groinstone V:.�:/?l Microfi ' oment wockeslone

�:::::=:::=::: Alternating morl :::-:::-:.:.:::� and limestone

.j-/ / Salou-Tivissa �'6/ ,' Block �/ ,( Andorra ��'&'*;' \ � . Solo • f:-'li/

Fig. 6. Reconstructed cross-section of the distribution of the Middle Jurassic deposits in the Aragonese and Tortosa platfoTIlls. Several fault­ controlled blocks inthe strongly subsident Tortosa PlatfoTIll, and the drastic change inthickness and facies between both platfoTIlls can be observed. Source data from Fernandez-L6pez et al. (1996, 1998). early Bajocian. Palaeogeographic differentiation of the Ferruindez-L6pez, 1995; Femandez-L6pez and Melen­ Tortosa Platform commenced during early Toarcian. dez, 1996). Among the ammonoid assemblages, taxa Open-marine condensed sections developed during characteristic for neritic NW European platforms are middle and late Toarcian, Aalenian, middle and late common, whereas phylloceratids and lytoceratids Callovian and early Oxfordian. By contrast, Bajocian, characteristic of oceanic Tethyan environments are Bathonian and lower Callovian stages correspond to very rare or missing. During the Bajocian Garantiana expanded sections. The Tortosa Platform can be traced Zone, the Tortosa Platform was colonized by Medi­ into offshore areas through the Amposta Marino D-S 1 terranean elements, like juvenile phylloceratids; how­ and Casablanca-l wells (Fig. 4; Lanaja, 1987; Mal­ ever, these represent less than 0.1 % of the total donado L6pez et aI., 1986; Femindez-L6pez et aI., population. 1996). The Middle Jurassic series of the Tortosa Platform Stratigraphical gaps corresponding to a part of the consists from bottom to top of the Sant Blai Formation, Aalenian Murchisonae Zone and the Callovian Lam­ which includes the Tivenys and the Salou members, the berti Zone, recorded both in the Iberian and Catalan Cardo Formation, and the La Tossa Formation (Figs. 3 Coastal ranges, reflect two peaks of regional shallow­ and 6). ing that affected the entire Iberian platform system (Figs. 3 and 5). On the Tortosa Platform, maximum 5.1. Sant Blai Formation sedimentation rates were recorded during the Bajo­ cian Garantiana Zone, which corresponds to expand­ The Sant Blai Formation is composed of bioclastic ed sections that exceed 60 m in thickness. However, mudstones to wackestones and interbedded marls and as indicated by the colonization of the platform by marly limestones with occasional levels containing fer­ ammonite populations, maximum water depths were ruginous and/or phosphatic ooids. This lithostrati­ reached during the Bajocian Niortense and Garanti­ graphic unit, which is topped by a hard ferruginous ana zones (Femandez-L6pez and Mouterde, 1985; surface, is characterized by metric scale thickening- and coarsening-upward sequences, except for some thin­ 5.2. Cardo Fonnation ning- and fining-upward sequences that occur in the upper parts of the Tivissa, Vandellos and Llaberia sec­ The Cardo Formation is composed of alternating tions (Fig. 2). Zoophycos. Tholossinoides and Rhizo­ mudstones and marls, which tend to be more calcareous corallium are abundant whilst ammonites, belemnites, upwards (Fig. 6). Ammonites and bivalves (Bositro) are bivalves, brachiopods, crinoids, serpulids, gastropods, abundant whereas belemnites, brachiopods and benthic ahermatypic corals and bryozoans are common. Above bivalves are less frequent. Some carbonized plant the Aalenian Murchisonae Zone discontinuity, the remains have been observed in several levels. Never­ Tivenys and Salou members of the Sant Blai Formation theless, encrusting benthic organisms are virtually ab­ can be distinguished. sent. The layers, which do not show evidence for early The Tivenys Member is made up of wackestones to cementation, such as hardgrounds or borings, normally packstones, which commonly contain a variable pro­ extend over several hundred meters. Marls and lime­ portion of ferruginous and/or phosphatic ooids and stones are organized into shallowing- and thickening­ pisoids. Ooids are irregular and complex, showing upward sequences, although the basal parts of this unit evidence of several phases of reworking. Remains of locally show thinning-upward sequences. echinoderms, microfilaments, ammonites, bivalves, The Cardo Formation overlies in most cases a hard­ brachiopods, foraminifers, sponges, belemnites, ostra­ ground with ferruginous crusts that marks the top of the cods, gastropods and bryozoans, as well as wood and Sant Blai Formation. The Cardo Formation attains a bone fragments are present. Thalassinoides and Rhi­ maximum thickness of 100 m in the Tivenys and Cardo zocorallium are common. Although the thickness of sections. To the north and west of this area, its thickness the Tivenys Member is less than 2 m, it is a charac­ decreases to less than 1 m in the Engrillo, Rio de Estrets teristic unit on the Tortosa Platform. The Tivenys and Barranco del Avellanar sections. Member extends from the Aalenian Bradfordensis The base of the Cardo Formation is diachronous at Zone to the Bajocian Propinquans Zone. Biofacies the scale of zones. In the Cardo, Tivissa, Vandellos, identified in these deposits are indicative of open­ Llaberia and Cap Salou sections, its basal parts corre­ marine environments with ammonoid assemblages spond to the Bajocian Humphriesianum Zone, whereas supporting relatively free communications with open­ in the Tivenys, Xerta-Pauls, Mont Caro and Alfara sea waters. The lateral distribution of these deposits is sections its first layers belong to the Bajocian Niortense very discontinuous and indicative of episodic sedi­ Zone (Fig. 2). The top of the Cardo Formation corre­ mentation with finll- to hardgrounds prevailing. sponds to the Bajocian Parkinsoni Zone. Local occurrences of mud-cracks are indicative of NW Europe ammonoids dominated the assemblages temporary subaerial exposure. Such environmental of the Cardo Formation, whereas Tethyan representa­ conditions are confirmed by several taphonomic crite­ tives such as phylloceratids and lytoceratids are very ria, such as concretionary internal moulds without scarce (less than 0.1 % of the total; Femandez-L6pez, septa, internal moulds with ellipsoidal abrasion facets 1983; Fernimdez-L6pez and Mouterde, 1985; Fernim­ and annular abrasion furrows observed on ammonites, dez-L6pez and Melendez, 1996). The Cardo Formation which are indicative of shallow, subtidal to intertidal was deposited under open-marine conditions on a environments (Femandez-L6pez and Melendez, 1994; strongly subsiding and faulted external platform, Ferruindez-L6pez et aI., 1998). which had open connections to the NW Europe domain. The Salou Member consists of mud stones and inter­ By contrast, and as indicated by the small amount of bedded marls. Except for ammonites and some bivalves characteristic Tethyan taxa, communication with the (Bositra), macrofossils are mre, although Zoophycos Tethys domain was very poor. On the Tortosa Platform, are abundant. This 15-45 m thick member is organized maximum water depths were reached during Middle into aggradational, thickening- and shallowing-upward Jurassic and were associated with episodes of strongest sequences, but shows in its upper parts several deepen­ subsidence. On the Tortosa Platform, taphonomic and ing sequences in the Tivissa area. Its age spans the palaeobiological evidence of its ammonoid colonization Bajocian Propinquans and Humphriesianum zones, al­ during the Bajocian Polygyralis Subzone of the Nior­ though its upper and lower boundaries are slightly tense Zone indicates the establishment of maximum diachronous. The Salou Member was deposited below water depths and its free communication with the NW wave-base on a low-energy, open-marine platform that European domain (Femandez-L6pez, 1997; Femandez­ was dominated by soft to firm, well-oxygenated bottom L6pez and G6mez, 2004). Subsidence was only partly conditions. compensated by high sedimentation mtes that amounted during the Garantiana Zone up to 100 m of sediments represented by a much thinner dolomitic fades, or are per million years. missing altogether (Robles Orozco, 1974; Esteban and Robles, 1979; Anad6n et aI., 1982). These dolomitic 5.3. La To ssa Formation fades were deposited on a high area, referred to as the Tarragona High (Salas and Casas, 1993). During the In the area of the Tivissa section, the La Tossa Bathonian, an oolitic and dolomitic high-energy belt of Formation can be subdivided into a lower part, consist­ shallow proximal fades developed between the Tortosa ing of micro filament mudstones to wackestones, con­ and Aragonese platforms, which prograded over the taining thin marl interbeds, a middle part composed of low-energy open-marine external platform sediments mudstones and marly limestones, and an upper part of the Cardo Formation. fonned by bioc1astic mudstones and wackestones. The carbonates of these three units are generally organized 7. Catalan Massif into thickerung- and coarsening-upward sequences, ex­ cept for the middle unit in which locally fining- and This palaeogeographic element has been defmed on thinning-upward sequences are recognized. Ammonites the basis of wells that had penetratedthe entire Cenozoic and bivalves (Bositra), as well as Zoophycos and Tho­ succession of the Ebro Basin and bottomed in Mesozoic lassinoides, are abWldant. The lower part of this for­ strata. No Middle Jurassic sediments were encoWltered mation, which is in the order of 30 to 35 m thick, is by the oil wells Fraga-I, Mayals-I, Senant-I, Ebro-I latemlly quite continuous. However, the middle and and Caspe-I (Fig.2 ; Stoeckinger, 1976; Lanaja, 1987), upper parts, which reach a thickness of 90 m in the either owing to their non-deposition or erosion in the Tivissa section (Fig. 6), show significant lateral fades area of the postulated Catalan Massif (Canerot et aI., variations. In the area of the Tivenys and Alfara-Cardo I 985a,b; Femimdez-L6pez et aI., 1996). Due to post­ sections, they grade into thick bedded oolitic pack­ Jurassic tectonic deformation and erosion, it is difficult stones to grainstones with cross-bedding and bar geom­ to precisely define the outlines of the Catalan Massif;the etry, and in the Xerta and Pauls sections into a 90 m southeasternmargin of which may have been controlled thick dolomitic fades. by the Requena-Mora Fault (Fig. 4). The La Tossa Formation was deposited during the late Bajocian, Bathonian and Callovian. Its transitional 8. Beceite Strait boundary with the Cardo Formation is slightly diachro­ nous. Whereas in the Xerta, Pauls, Alfara and Coli del The Tortosa and the Aragonese platforms were Caragol sections the lowennost beds contain ammo­ connected via the Beceite Strait (Fernandez-L6pez et nites of the Bajocian Garantiana Zone; they contain aI., 1996, 1998) that is located between the positive ammonites of the Parkinsoni Zone in the area of the areas of the Catalan Massif and the El Maestrazgo High Tivenys, Cardo, Tivissa and Vandellos sections. The (Fig. 4). Condensed sections of the Chelva Group, not Bathonian deposits are 40 m thick in the Tivissa and exceeding 40 m in thickness, characterize the Beceite Vandellos sections, and the late Bathonian, which is Strait. These consist mainly of bioc1astic wackestones rarely recorded on the Castilian and Aragonese plat­ to packstones that were deposited on an open-marine forms, is represented in these areas by biostratigraphi­ external platform. The open-marine facies and con­ cally complete and expanded sections. In the about 45 densed sections of the Beceite Strait are the lateral m thick Callovian deposits of the Tivissa section, at equivalents of the expanded open-marine, external plat­ least the Bullatus, Gracilis, Anceps and Coronatum form successions of the Aragonese and Tortosa plat­ zones have been identified. The top of the Middle forms (Fig. 6), although stratigraphical features show Jurassic series is marked by a hardgroWld, characterized more affmities with the Aragonese Platform. by reworked fossils, glauconite and locally by ferrugi­ nous crusts. 9. Structural control on palaeogeographic elements of the eastern margin of the Iberian platform system 6. Tarragona High During the Middle Jurassic, the East-Iberian carbon­ The stratigraphic successions described for the Tor­ ate platform was affected by tensional tectonics and tosa Platform, on which Middle Jurassic deposits attain minor volcanic activity that can be related to the fmal a total thickness of 350 m, dramatically change to the rifling phase that preceded the opening of the oceanic north, where stratigraphical equivalent sediments are Alpine Tethys (Ziegler, 1990; Salas et aI., 200 I; Stamp- fli and Borel, 2004). Correspondingly, this carbonate another (Fernandez-L6pez et aI., 1996, 1998). Maxi­ platform was dissected into a system of differentially mum sedimentation rates were reached on the Tortosa subsiding fa ult and in some cases tilted blocks, each Platform during the Bajocian Garantiana Biochron. of which fo llowed a relatively independent evolution The different fa ult-bounded elements of the Iberian (Fernandez-L6pez and G6mez, 1990a). On these platform system show characteristic variations in terms fa ult-bounded blocks, carbonate platforms fo rmed of relative thickness (e.g. condensed versus expanded under diverse depositional environments giving rise to sections) that are associated with changes in the successions that laterally varied substantially, both in palaeoenvironmental conditions (e.g. restricted versus terms ofthickness and fa cies development. For instance, open-marine and shallow versus deep-water environ­ Aalenian and lower Bajocian deposits are represented ments, respectively), as shown in Fig. 7. Condensed on most platforms, which corresponded to relatively sections, that developed under restricted environments, slowly subsiding areas, by thin condensed sections. are represented by dolomitic sediments, for instance on On the Central External Castilian Platform, however, the El Maestrazgo and the Tarragona highs. By contrast, Aalenian and lower Bajocian deposits are represented the Enguidanos Depocentre, located within the Internal by expanded sections, suggesting that this area repre­ Castilian Platform, and the El Maestrazgo Depocentre, sented a downthrown block that subsided more rapidly represent expanded sections composed of restricted than adjacent blocks. In several cases, changes in sub­ fa cies that accumulated on relatively rapidly subsiding sidence rates can also be observed on the same block. blocks. Deposits representative of such restricted envir­ For instance, on the Central External Castilian Platform, onments on internal platforms are the mudstones and Aalenian and lower Bajocian deposits fo rm normal sec­ oolitic grainstones of the Yemeda Formation, and the tions, showing average sedimentation rates, to expanded mainly dolomitic deposits of the Rafales Formation on sections, whereas most of the Bathonian and Callovian the El Maestrazgo High. Detailed biostratigraphic dat­ deposits represent condensed sections, reflecting a slow­ ing of such restricted deposits is extremely difficult, ing down of the subsidence rate of this block. By owing to the scarcity of ammonites. On platforms, contrast, on the Tortosa Platform, upper Aalenian and which developed mainly under open-marine conditions, lower Bajocian condensed sections, give way to expand­ a high-resolution biostratigraphic zonation, based on ed upper Bajocian to lower Callovian sections, being the ammonites, has been achieved. Examples of such ex­ upper Bajocian sections the thickest ones of the entire ternal platforms are the External Castilian, Aragonese Middle Jurassic platform system. and Tortosa platforms. Differential subsidence of these Despite these strong lateral and temporal variations, fa ult-bounded platforms conditioned their development. some fe atures remained common to all platforms. The For example, the Pozuel Depocentre, located on the regionally most extensive fe atures observed on the NW External Castilian Platform, was mainly filled-in Iberian platform system, are the stratigraphical gaps that are recorded in part of the Aalenian Murchisonae '" t- Zone and in the Callovian Lamberti Zone. Moreover, Z :.LLJ the presence of condensed sections at the base of the z a1 Bathonian and Callovian is another stratigraphic fe ature � LLJ � that virtually occurs in the entire area, although the time �D � l D �tJs S �ICl cotJ �D ;: interval covered by them strongly varies between the PE:D • Tarragona 0 OFloE:� �"P}\N High :::J different platforms. Further fe atures that can be traced El Maestrazg � Central External T I High (/J Castilian all over the different platforms are, at a stage-scale, the El Maestrazgo Platform Internal High �����: Idepocenter) timing of maximum relative water depth of the succes­ I sive deepening-shall owing cycles. In external platform Beceite areas, maximum water depths were attained during the Strait Bajocian Humphriesianum and Niortense zones, the Bathonian Progracilis Zone and the Callovian Gracilis Zone, as indicated by the colonization of the platforms by ammonites and the taphonomical fe atures observed in the fo ssil assemblages (Fernandez-L6pez, 1997; Fer­ nandez-L6pez and G6mez, 2004). However, subsidence Fig. 7. Plot of palaeogeographic elements mentioned in this work, in maximums, indicated by the distribution of depocen­ tenns of condensed to expanded sections, restricted to open-marine tres, are markedly diachronous from one platform to environments and deep to shallow environments. during the Bathonian and Callovian by the carbonates palaeogeogmphic elements along the eastern margin of of the Domefio Formation. By contrast, the Casinos the Middle Jurassic Iberian carbonate-platform system. Depocentre, located on the SE External Castilian Plat­ Around the El Maestmzgo High, three main platforms form, was filled-in during the Bajocian by the carbo­ can be recognized, namely the Castilian, Aragonese and nates of El Pedregal Formation. The Tortosa Platform Tortosa platforms. Attached to the Iberian Massif, the represents an example of an extremely rapidly subsid­ Internal Castilian Platform, dominated by restricted fu­ ing external platform that is characterized by highly cies and commonly expanded sections, was bounded by expanded sections. In this area, more than 350 m of the Montes Universales and La Mancha faults. The Middle Jurassic sediments accumulated. Maximum sed­ External Castilian Platform was dominated by open­ imentation rates were recorded during the upper Bajo­ marine facies, locally containing interbedded restricted cian Garantiana Zone, when up to 60 m of alternating facies in some proximal and shallow areas, and com­ pelagic marls and limestones were deposited, although monly normal to expanded sections. The Northwestern, subsidence rates reached a maximum during the Nior­ Central and Southeastern External Castilian platforms tense Zone. Condensed sections, which were deposited are sepamted by a northeast-trending fault system, in­ on external platforms, are represented for example by volving the Noguera-Aguaton, Teruel and Requena­ the less than 40 m thick Middle Jurassic deposits of the Mom faults. The fault-bounded El Maestrazgo High, Beceite Strait that connects the Tortosa and Aragonese that was characterized by condensed to expanded sec­ platforms between the El Maestrazgo High and the tions of restricted environments, separated the Castilian Catalan Massif. Condensed external platform sections and the Aragonese and Tortosa platforms. Open-marine are also present on the Castilian Platform where they environments dominated these external platforms. are associated with volcanic mounds, providing for a 'Whereas expanded sections are common on the Tortosa sea floor relief (Fernandez-L6pez et aI., 1985; Cortes, Platform, the Aragonese Platform contains condensed as 2001). Deposits of restricted environments are well as expanded sections. A connection between the recorded, locally and occasionally, in external platform Aragonese and Tortosa platforms was established via areas. For example, some lower Bajocian deposits of the Beceite Strait, located between the Catalan Massif the El Pedregal Formation, filling the Powel Depocen­ and the El Maestrazgo High. The Tarragona High, char­ tre that is located on the NW External Castilian Plat­ acterized by restricted fades,delimited the Tortosa Plat­ form, are composed of peritidal dolomitic limestones form to the north. Along the eastern margin of the and mudstones showing microbial laminae and mud­ Iberian carbonate-platform system, expanded sections cracks. These restricted facies, and associated open­ were not necessarily associated with open-marine envir­ marine facies, find their lateral time equivalents in onments. On these external and internal platforms, con­ open-marine deposits which grade into the Internal densed and expanded sections developed, even on Castilian Platform facies. palaeogeogmphic highs, such as the El Maestmzgo Based on the above, we conclude that during the High. Open-marine environments dominated external Middle Jurassic syn-depositional extensional faults platforms, whereas restricted environments character­ controlled subsidence patterns of the main palaeogeo­ ized internal platforms and occasionally occur in the graphic elements along the eastern margin of the Iberi­ shallow parts of external platforms. an platform system. The different platforms can be categorized in terms of their sediment thickness (ex­ Acknowledgements panded versus condensed sections) and palaeoenviron­ mental setting (restricted versus open environments). This work is a contribution to the project CGL2004- Open-marine, normal salinity, environments were de­ 02694IBTE (MEC-CSIC). We wish to thank F. Surlyk veloped in external platform areas, whereas restricted (University of Copenhagen, Denmark), P. A. Ziegler environments characterized internal platform areas, al­ (UniversityBasel, Switzerland) and an anonymous ref­ though occasionally they occur in proximal areas on the eree who provided useful criticism and valuable sug­ shallow parts of external platforms. gestions for the improvement of the manuscript.

10. Conclusions References

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