GEOLOGIE EN MIJNBOUW,© 198(1 VOLUME 59(2),p. 155-168

MESOZOIC PALAEOCEOGRAPHIC EVOLUTIONOF THE EXTERNAL ZONES OF THE BETIC CORDILLERA'

M. GARCIA-HERNANDEZ2, A. C. LOPEZ-GARRIDO3,P. RIVAS2, C. SANZ DE GALD.EANO2 & J. A. VERA`.3

ABSTRACT

Garcfa-fiernandei, M., A. C. Lopez-Garrido, P. Rivas. C. Sanz de Galdcano & .I. A. Vern 1980Mesozoic palaeogeographac evolution of the, External Zones of the Bctic Cordillera - Geol.Mi,jnhouw 59:1,55-168.

The main events characterizing the Mesozoic palacogcographic evolution of the External Zones of theBetic Cordillera are outlined. The Triassic sediments show a 'germanic' type lacies over the entireregion, ending with Late Triassic evuporites and variegated clays of Keeper facies. At the hcginning ofthe Jurassic a transgression takes place, and a broad shallow-marine carhonatc-platform environmentappears.

During the Carixian (180 Ma) the carbonate platform breaks down leading to the differentiation oftwo large palaeogcographic units: the Prebetic Zone where shallow-water environments prevailedthroughout the Mesozoic, and the Subbctic Zone where the sediments arc clearly pelagic.

Within the Prebetic Zone, two palaeogcographic realms are differentiated: the External Prebetic,showing important stratigraphic gaps in t he .Jurassic and Early Cretaceous sequence, and the InternalPrebetic with a thicker and more continuous stratigraphic sequence. Between the Prebetic andSubbctic Zones, a palaeogeographic realm is distinguished (Intermediate units) where turhiditic andpelagic materials were deposited. This zone corresponds approximately to a slope environment duringmost of Mesozoic times.

In the Subbctic Zone a marked differential subsidence occurs during the Jurassic, leading to trough(Median Subhetic) and swells (External and Internal Subbctic). In the Median Subbctic. the depositsconsist mainly of marls, pelagic limestones, radiolarites and calcareous turbidites. with htafic volcanicand subvolcanic rocks. During the Cretaceous pelagic marls and marty limestones were laid down.

Mesozoic sedimentation took place :`long the southern margin of the European plate, in anAtlantic-type continental margin underlain by continental crust. Three-dimensional schemes. ex-plaining the main palaeogcographic events are included.

INTRODUCTION

The Betic Cordillera forms the westernmost part of the alpineMediterranean chains and occupies a belt in southern Spainabout 600 kin long and 200 km wide. Two main geologicalrealms are distinguished: the Internal and the External Zones.

The Internal Zones consist mainly of overthrust units ofTriassic and Palaeozoic materials,, in some units. Mesozoic,Tertiary and probably Precambrian terraines can also hefound.

The External Zones differ markedly from the InternalZones.' Palaeozoic materials are not exposed. They form the

Manuscript received: 1979-1 I-16.Revised manuscript received and accepted: 1979-12-20.Seccibn de Gcologfa Facultad de Ciencias, Universidad.GRANADA, Spain.Departamento de Investigaciones Geol6gicas C.S.f.C.. Univcr-sidad, GRANADA, Spain.

basement from which the Triassic to Lower Miocene coverwas detached and thrust northwards along Triassic evapo-rites. The cover consists mainly of sediments with local sub-marine volcanic and subvolcanic mafic rocks of Jurassic andEarly Cretaceous ages.

Sedimentation in the External Zones took place on acontinental margin located along the southern border of theSpanish Meseta. During the Mesozoic the position of thismarginal basin, in relation to the Internal Zones. was verydifferent from that of the present. Most authors think that theInternal Zones occupied a position corresponding to the areaof the present western Mediterranean. and that the juxtaposi-tion of Internal and External Zones with the subsequentshortening and deformation of the cover of the ExternalZones, took place from the Eocene onwards. and especiallyduring the Early Miocene.

As well as these two important zones it is possible todistinguish, within the Betic Cordillera, the Campo de Gibral-tar units formed by allochthonous, largely turbiditic and olis-

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Fig. 1

Map showing the distribution of units in the External zones of the 13etic Cordillera. Figure A displays the actual outcrops of thepalaeogeographic units. In some areas (East of Cadiz and South of Caravaca) the interpretation is difficult because of tectonic complicationsand scarcity of Jurassic outcrops. On figure 13 the hypothetical palinspastic position of the palaeogeographic units during the Mesozoic isreconstructed. Shortening of the cover due to folding andovcrthrusting is estimated to ahout 2/3 of the original width. The Internal Zones havebeen separated from their actual position just enough to reconstruct the External Zones: their real position would have been much farther awayduring Mesozoic.Legend. I: Variscan massif of Meseta (Spanish plain); 2: Tabular cover of Meseta (Triassic and .Jurassic): 3: External Prchetic; 4: InternalPrebetic; 5: Intermediate units between Prebetic and Suhbetic; 6: External Subbetic: 7: Median Suhbetic (the asterisks mark the main outcropsof suhmarine volcanic rocks intercalated in Jurassic formations); 8 : Internal Subbetic: 9 : U lira-internal Subbetic; 10: 'Cameo de Gibraltar' units(Numidian flysch and other turbiditic formations forming several nappes): l I : Internal Zones of Retie Cordillera (units arc not separated), 12:Neogene-Quaternary volcanic rocks; 13: Guadalquivir hasin areas, with suhbetic nappes and olisthostrumes (Guadalquivir units and Carmonanappe); 14: Neogene-Quaternary outcrops mainly in postorogcnic basins; 15: Northern limit of Suhbetic during the Mesozoic; 16: Actualposition of Subbetic overthrust: 17: Northern limit of the Guadalquivir units olist[lost romes.x: cross-section of figure 2; y: cross-section of figure 3: Z: cross-section of figure 4.

thostromal formations, which range from Cretaceous to EarlyMiocene.

After the general alpine folding, postorogenic basins werefilled by Neogene and Quaternary materials. Two types ofbasins exist; one marginal and with foredeep characteristics(Guadalquivir Basin) and others intramontaneous (Granada,Guadix-Baza, etc.). During the early Miocene, the Guadal-quivir Basin constituted an important submergent troughwhere, by gravity gliding, some material of Subbetic origin wasinserted between formations of Miocene age, forming olis-thostromes and nappes.

For the reconstruction of the palaeogeographic evolution of

the External Zones we compiled the stratigraphic and tectonicdata of the whole area, especially those of more recent works.Our main sources are included in the list of references. Inthese references we find the description of approximately 800stratigraphic sequences of the Mesozoic formations.Palaeogeographic syntheses are found in: o(NZ,Vez-DONOSO e 1AL. (1970), AZI[MA F; AL. (1970, 1973, 1979) and HLRMES (1978).

The first important subdivision of the External Zones of theBetic Cordillera was given by 111.uMI.N rHAL ( 1927) and I Al LO 1

(1948) both distinguishing the Prebetic Zone to the north ofthe .Subbetic Zone. The first is characterized by shallow-waterfacies as opposed to the second where pelagic facies prevails.

PALE OGEOGRAPHICRECONSTRUCTION

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Section across the External Zones in the Orcera-Ncrpio region.A: Structural cross-section; B: Palinspastic reconstruction (at a minor scale) at end of the Mesozoic; C: Correlation of the Mesozoicstratigraphic sequences located according to palinspastic interpretation.Tr. = Triassic; Ji. = Lower Jurassic; .IM. = Middle Jurassic; Js. = Upper Jurassic; Ki. Lower Cretaceous; Ks. = Upper Cretaceous(Stratigraphic sequences marked by X arc interpreted by extrapolation).Legend of figure A and B'. I: Triassic; 2: External Prebetic (Sierra Cazoi la unit): 3: Internal Prehetic (Sierra Sggura unit): 4: Tertiary sedinrcnisof Prebetic zone, 5: Intermediate units between Subhetic and Prchetie: 6: External Suhbetic: 7: Neooenc and Quaternary.Legend of figure C. 8: Triassic-Liassic boundarv: 9: Lower limit houndarv of Domcriam: 111: Liassic-Middle Jurassic boundary; 11: Middle-Upper Jurassic boundary; 12:.furassic-Cretaceous boundary; 13: Base of Utrillas Formation; 14: Lower-Upper Cretaceous boundarv; 15:Palacogen-Cretaceous boundary; 16: Triassic halal conglomerate: 17: Green and red marls and clays; IS: Sands and sandstones: 19:Muschelkalk facies: 20: Kcuper facies; 21: Dolomites; 22: Marine platform carbonates: 23: Cherty limestones and micritic levels; 24: Nodularlimestones; 25: Filament and radiolarian limestones; 26: Calcareous breccias and turbidites: 27: Tidal flat and lagoonal limestones; 28: Reellimestones; 29: Pelagic facies (marls, marly limestones, micritic limestones with pelagic fauna); 311: Utrillas Formation: 31: Terrigenousturbidites interheddcd in pelagic facies.

The contact between Prebetic and Subhetic Zones correspondto an important thrust. On the palinspastic map of figure IBthe present-day position of this contact and its position priorto the' thrusting are marked.

In the Prebetic,Zone,the External and Internal Prebetic aredifferentiated. Between the Prebetic and Subhetic Zones arethe so-called 'Intermediate units' with nixed stratigraphicfeatures; they are overthrusted on the P.rebetic and underlaythe Suhbetic tectonically. In the Suhbetic, three main realmsare distinguished mainly by their Mesozoic sequences: the

External, the Median and the Internal Suhbetic. The Ultra-internal Subhetic unit is locally differentiated along the south-ernmost areas. In the palaeogeographic reconstructions we donot consider this unit because of its local character and moresouthern origin.

A series of cross-sections, palinspastic reconstructions andstratigraphic correlations through the External Zones situ-ated in the central region of the cordillera is presented in.figures 2, 3 and 4.

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Section across the External Zones in the Granada-Jaen region modified and completed. (after Rivas ct al., 1979)Tr. = Triassic; Ji. = LowcrJurassic; .1n1. = Middle Juraasic: Js. = Uppcr.lurassic. Ki. = LowcrCrctaceous; Ks. = UppcrCrctaccous.Stratigraphic sequences marked by 'x' are deduced by extrapolation.A: structural cross-section; B: palinspastic reconstruction (minor scale) at end of the Mesozoic: C: Stratigraphic sequences correlated andlocated according to palinspastic reconstruction.Legend of figuresA and B. 1: 'Dorsalc hetique'; 2: Malaguide complex; 3: Alpu(arridc complex; 4: Ncvado-Filabride complex; Other signs as infigure 4.Legend of figure C. 5: Keuper faeies; 6: Dolomites; 7: Marine platform limestones: 8: Cherty limestones and micritic levels: 9: Marls, marlylimestones and limestones in general; I1): Nodular limestones: 11: Limestoncs with filaments and radiolarians, locally radiolarites; 12: Volcanicand subvolcanic mafic rocks; 13: Radiolarites and marls with cherty interbcds; 14: Calcareous turbidites and hreccias; 15: Limestones and marlylimestones laterally passing into marls; 16: Detritic limestones; 17: Terrigenous turbidites, intcnccdded in pelagic faeies; 18: Pelagic facies(marls, marly limestoncs, micritic limestones with planktonic and pelagic fauna); 19: Triassic-Liassic boundary; 20: Lower boundary ofDomerian; 21: Liassic-Middle Jurassic hound.uy; 22: Middle-Upper Jurassic boundary: 23:.lurassic-0-etaceous boundary; 24: Lower-UpperCretaceous boundary; 25: Cretaceous-Palaeogene boundary.

STRUCTURE OF THE EXTERNAL ZONES,

The External Zones of the Betic Cordillera show a tectonicstyle typical of sheared-off sedimentary cover. The maindecollement is situated in the Triassic terraines; locally, thereare other decollement levels at a stratigraphically higherposition.

Although the structure of the External Zones differs alongdifferent traverses (compare Figs. 2, 3 and 4). the allochthon-

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The Prehetic zone shows an important shortening of thecover, in some sectors, estimated at 15 km (I)ABRto & toPEZ-GARRtoo, 1970). The general structure of the Prehetic is shownin figure 2A. The tabular cover of the Variscan Meseta at theexternal side of the Prehetic Zone is not affected by Alpinedeformation (Lot't z-GARRtDO. 1971-b). The northern margin of

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Section across the External Zones in the Loja-Cahra region (After RIVAS et al., 1979; modified ;ind completed).Tr. = Triassic; Ji. = Lower Jurassic; Jill. = Middle Jurassic; Js. = Upper.lurassic; Ki. = l owerCretaccous; Ks. = Upper CretaceousStratigraphic sequences marked by 'X' are deduced by extrapolation.A: Structural cross-section; B: Palinspastic reconstruction (at a minor scale) at the end of the Mesozoic; C: Correlation of the Mesozoicstratigraphic sequences located according to palinspastic reconstruction.Legend of tigtues A and B. I: Miocene of Guadalquiv0 hasin (o: olisthostrontes of Suhbetic origin); 2: Prebetic zone: 3: Intermediate unitsbetween Prchetic and Suhbetic; 4: Northern External Suhbetic (Sierra de Cahra unit); 5: Southern External Suhbetic (Sierra de Gacna unit); 6`Mediate Subbetic. with submarine volcanism; 7: Internal Suhbetic (Parapanda-Mpclin unit ); 8: Internal Suhbetic (Sierra Gorda unit); 9: Ultra-internal Suhbetic (Zafarraya and G;tllo-Vilo units); 10: Triassic terraines; 11: 'Campo do Gibraltar units; 12: Internal zones (Alpujarridecomplex).Legend of figure C. 13: l'riassic-Linssic'boundary: 14: Lower houndarv of Domerian; 15: I iassic-Middle ,Jurassic boundary; 16: Middle-UpperJurassic boundary; 17: Jurassic-Cretaceous houndary; 18: Lower-Upper Cretaceous boundary: 19: Cretaceous-Palaeocene boundary; 20:Keuper facies; 2l: Dolomites; 22: Marine platform limcstones; 23: Red marls; 24: Cherty limcstones and micritc levels; 25: Nodular limestones;26: Limestones with filaments and radiolarians, locally radiolaritcs; 27: Mafic volcanic and subvolcanic rocks; 28: Radiolarites and marls withcherts; 29: Calcareous turbidites and breccias; 30. Erosion surfaces with sedimentary infills; 31 Detrital limcstones; 32: Terrigenous turhiditesinterbedded in pelagic facies; 33: Detrital, partially turhiditic facies; 34: Pelagic facies (marls, nearly limestones, nticritic limestones withplanktonic and pelagic fauna).

the Prebetic, zone (External Prebetic) shows a reverse-faultimbricated structure also with narrow overturned folds, bothup dipping toward the Meseta. The Internal Prebetic shows itgentler fold and fault structure. The southern margin of thePrebetic Zone is overthrusted by the Intermediate units,which in their turn are overthrusted by Suhbetic nappes (Figs.3 and 4).

Towards the East (provinces of Morels and Alicante, Fig.1) the structure of the Prebetic Zone is simpler with folds andnormal faults and, occasionally, overthrusts and mushroomfolds, which in many cases are linked to diapiric structures(i ODiuGuez-esrtieLL, , 1977).

An important feature which is not displayed by the cross-sections, but that is common to the entire Prebetic is the

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occurrence of major transcurrent faults, that cut across preex-isting structures and presently have a conspicuous seismicactivity.

The cross-sections of figures 3 and 4 terminate northwardsin the Internal Prebetic and the Intermediate units; the moreexternal units are covered by Neogene sediments of theGuadalquivir Basin. Klippes of Subbetic origin and Prebetictectonic windows are common.

The structure of the Subbetic zone is illustrated in figures 3and 4. Every tectonic unit has been overthrusted to the northand covered to the south by the next higher tectonic unit. Theboundaries of the tectonic units in general coincide with thoseof the Mesozoic palaeogeographic units: in some regions (Fig.3) a transition between two palaeogeographical realms takesplace along continuous outcrops in a single tectonic unit.

During the latest Oligocene and Early Miocene the mainoverthrusts of the Subbetic Zone were thrust over the deepestportions of the submergent trough of the innermost part of therealm of the Prebetic and Intermediate units. West of Cazorlasome of the Subbetic units extend beyond this limit across thePrebetic into the Guadalquivir basin where they form olis-thostromes and gravitational nappes intercalated in Burdiga-lian sediments. This ensemble is called the Guadalquivirallochthonous units (GARCA-KOSS[W.. 1973). The present out-crop position of the olisthostromes is shown in figure IA,whereas their northern extension as inferred from boreholedata is indicated in figure lB (PeacoNING s MARTINEL. 1977).

PALAEOGEOGRAPHIC REALMS

In the map of figure 1 the units of the External Zone areoutlined. Each of the units is defined by its Mesozoic strati-graphic sequence and palaeogeographic evolution.

Prebetic zone

The External Prebetic is characterized by the thinness of theMesozoic cover, important Jurassic outcrops and a general

_stratigraphic gap from the Portlandian4 to the Neocomian.We here refer to the characteristics in the sector situatedbetween the meridians of Cazorla and Cieza.

The Triassic, near the margin of the Meseta, is formedexclusively by classic sediments, but towards the interior ofthe basin carbonate of Muschelkalk facies appears (Fig. 2C).In the Lower Jurassic dolomite predominates with some marland clay interbeds of increasing frequency upwards. TheMiddle Jurassic also consists of dolomites with local lime-stones at the top; the Upper Jurassic presents nodular lime-stones in the Middle-Upper Oxfordian and marls and marlylimestone in the Lower Kimmeridgian; both with abundantammonite fauna. The uppermost Jurassic has only very localoutcrops, in Purbeck facies. The Upper Cretaceous is thin and

4 Portlandian is used instead of Tithonian because of the occurrenceof shallow-water facies.

consists of Cenomanian dolomites and of lagoonal deposits ofthe Senonian. During the Palaeogene the External Prebeticemerged; the Lower Miocene is transgressive and directlyoverlies the Mesozoic rocks.

The Mesozoic cover of the Internal Prebetic is thicker thanthat of the External Prebetic, with fewer stratigraphic gaps,which are located along the marginal areas of the zone orassociated with diapiric structures of Triassic rocks.

The Early and Middle Jurassic sediments appear only insmall outcrops and have characters similar to those of theExternal Prebetic; on the other hand the Upper Jurassic(Upper Kimmeridgian and Portlandian) is well developed andmainly in Purbeck facies. The Early Cretaceous sedimentsshow a variety of facies becoming increasingly pelagic basininwards. The Urgonian facies is developed in the Aptian-Albian (GARCIA-HERNANUEZ. 1979) and is overlain by sands andclays with strong continental influence, belonging to the Utril-las Formation. Below this there occur stratigraphical gapswith different and increasing range increasing towards theexternal border of the Prebetic basin. The Upper Cretaceous,mainly carbonates (dolomites and limestones), is clearlypelagic. The Palaeogene is well developed in the southern-most areas of this realm. It is mainly of shallow-marine facieswith continental and coastal episodes. The Lower Miocene isrepresented by calcarenites and marls with Globigerina.

Intermediate units

Between the Subbetic and Prehetic Zones a palaeogeographi-cal realm with peculiar features is individualized (see Figs. 2, 3and 4). During the Mesozoic and Tertiary it formed a subsid-ing trough, in which a sequence was deposited with charac-teristics `intermediate' between the Subbetic and the Prebe-tic. In the South of Jaen (Jabalcuz-Los Villares unit) theMesozoic cover is exceptionally thick (Fig. 3).

The Jurassic sequence is thick and presents similar featuresto those of the more subsident parts of the Subbetic zone, withradiolaritic levels at the boundary Middle/Upper Jurassic, andturbidites in the Upper Jurassic.

The very thick Lower Cretaceous presents turbiditic levelsof Barremian-Albian ages. The upper Cretaceous andPalaeogene are pelagic, with gravitational slumps, olistho-stromes and turbidites (noi_uEVMAeKLR. 1973) that reach theirgreatest development during the Early Miocene.

Subbetic zone

In the central sector of the Betic Cordillera, three sedimentaryrealms have been distinguished based on facies and thicknessof the Jurassic. They are: External Subbetic, Median Subbe ticand Internal Subbetic (oAKCA-OULNAS, 1967; roN raorr. 1970).The Cretaceous is very uniformly developed. The LowerCretaceous is formed by light-coloured marls and marly lime-stones with abundant ammonites. The Upper Cretaceous ispresent in `couches rouges' facies with planktonic foraminif-

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era similar to that of other Alpine Mediterranean regions(e.g. 'Scaglia rossa' in the Apennines). The Palaeogene pre-sents very scarce outcrops of pelagic facies with interbeddedturbidites and olisthostromes (11OEDEMAEKER. 1973; COMAS.1978).

The sequence of the External Subbetic (Figs. 2, 3 and 4C) ischaracterized in the Upper Jurassic by nodular limestones oflimited thickness and by the absence of radiolaritic facies inthe Jurassic. In the region between the transversals ofGranada-Jaen (Fig. 3) and Loja-Cabra (Fig. 4) two palaeo-graphic realms can be distinguished, according to the facies ofthe Middle Jurassic; the northern one is thick and formed byoolithic limestones, the southern one consists of thin nodularlimestones (Fig. 5C). This differentiation is of local charactersince eastwards (Fig. 2) and westwards the facies are the sameall over the region, consisting mainly of nodular limestones inthe Upper and of varying lithologies in, the Middle Jurassic(marls, limestones, etc).

The Median Subbetic is the most subsiding realm in thesubbetic and shows pelagic marls and nearly limestones in theupper Liassic, with intercalated' volcanic and subvolcanicmafic rocks (VERA. 1966).' During the Middle Jurassic marlylimestones very rich in radiolarians and Bositra 'Filaments'were deposited. Within them abundant intercalations of vol-canic and subvolcanic rocks occur (e.g. FONTBOTE & OUINTURO.

1960; GARCIA-YEBRA ET AL. 1972; PAOULT. 1967). In the lowerpart of the upper Jurassic, radiolarites (in part Middle Juras-sic) and marls rich in radiolarians appear. The uppermostJurassic presents breccias and carbonate turbidites interlay-ered with marly and micritic limestones. In the Upper Jurassicinterbedded volcanic rocks are locally abundant (GARCIA-ROS-SELI., 1973; COMAS, 1978).

The Jurassic sequences of the Internal Subbetic are entirelyformed by carbonate sediments, with stratigraphic gaps thatinclude the late Liassic and, more locally, the Middle .Jurassic.The Malm, as the External Subbetic, consists of thin nodularlimestones with abundant ammonites, that permit accuratedating (LINARES & VERA. 1965; SEGUIIROS. 1974; OLORIZ. 1976).

In the southern parts of the Subbetic, allochthonous ter-raines appear that are interpreted as of still more southerlyorigin than, the Internal Subbetic. They correspond to severalunits that can be included in the Ultra-internal Subbetic (cRUZ-SAN.IUI.IAN. 1974) formed in a subsiding trough similar to that ofthe Median Subbetic which developed radiolaritic facies in thelate Jurassic.

MESOZOIC PALAEOGEOGRAPHIC EVOLUTION

The palaeogeographical features of the External Zones dur-ing Jurassic and Cretaceous times are summarised in figure 5.Figures 6, 7 and 8 show a three-dimensional interpretation ofthree characteristic stages and the corresponding sedimentaryenvironments, facies and thickness-distribution patterns. Thereconstructions are valuable mainly for the central part of the

Betic Cordillera, between the meridians of Caravaca andAntequera.

The Variscan craton of the Spanish Meseta was it continen-tal area continuously eroded during the Mesozoic; at someperiods the more external Prebetic areas emerged and wereaffected by erosion (Figs. SD, E, F).

Triassic

In spite of the great extension of Triassic outcrops both`autochthonous' and allochthonous sections for detailedstratigraphic analysis are rare.

The lithofacies are closely similar to those of the 'GermanicTriassic' and the term 'germanic-andalousian facies' is there-fore used. Three main lithological units are recognized: Bunt-sandstein, Muschelkalk and Keuper.

In the tabular cover of the Meseta the Triassic is composedof red fluviatile clastic sediments covered by evaporitic levels,(FERNANDEZ. 1975); to the South at the borders of the Prebeticzone, the marine Muschelkalk facies begins (LOFEZ-GARRIDO.1971-b). Triassic sediments become gradually thicker. Lip to2000 m in some areas of the Subbetic zone (SANZ DFGAI.DFANO.1973) toward the interior of the External Zones.

The Buntsandstein facies has been dated by the bivalvefauna in only one place (HUSNARDO. 1975): as uppermostWerfenian. During the Early Triassic the sedimentation sup-posedly took place in lagoonal and fluvial environments.

The Muschelkalk facies consists of limestones, marly lime-stones and dolomites sedimented in marine or lagoonal envi-,romnents. Its Middle Triassic age is established by ceratites,bivalves and conodont faunas from many places (LOPEZ-GAR-RIDO, 1971-h; RUSNARDO. 1975; I IIRSCI I & PARNES. 1977). The Mus-

chelkalk facies disappears gradually towards the Meseta (Fig.2C) by an irregular decrease in thickness. The maximumthickness including clastic intercalations is 200-300 In. Thisfacies change is the main palaeogeographic feature recordedin the External Zones during Triassic tines.

The Keuper facies basically consists of red and green va-riegated clays with subordinated interbedded sands, sand-stones, and carbonate rocks of variable thickness and exten-sion. Important amounts of gypsum up to 300 In thick inoutcrop and salt more than 100 In in the subsurface arerecorded. Fossils are rare. mainly because of the preserva-tional conditions, and consist of Estheridae of the Late Triassic. The sedimentary environment is comparable to that of theBuntsandstein, however, with larger marine influence andwith minor detrital influx.

An interesting feature is the presence of important doleriticand. other mafic intrusions, specially in the Subbetic zone.

Pre-Domerian, Liassic

The beginning of the Jurassic coincides with an importanttransgression which affects the entire area including the tabu-lar cover of the Meseta. A" shallow carbonate platform is

PREBETIC ZONE

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Fig. 5

,Palaeogeographic evolution,A: Palaeogeographic reconstruction (P.r.) for Carixian times and facics distribution (f.d.) of pre-domerian Liassic; B: P.r. for latest Liassictimes and Ed. of Liassic: C: P.r. for Middle-Late Jurassic boundary and Ed. of Middle Jurassic.: D: P.r. for Jurassic-Cretaceous boundary andf.ii; of the Late Jurassic: E: P.r. for Hauterivian and Ld, of Neocomian; F: P.r. for early Aptianllate Aptian boundary and f.d. of f arremian-early Aptian: G: P.r. for late Alhian and f.d. of late Aptian-Albi:ln: H: P.r. for latest Turonian and f.d. of Cenomanian-Turonian: L P.r. forMaestrichtian and U. of Senonian. .

l: Fluviatile-influenced sands and lutites (Utrillas Formation); 2: Tidal-flat and lagoonal carbonate rocks; 3: Idem, dolomitized: 4: Open-marine carbonate-platform facies: 5: Idem, dolomitized: 6: Rcefs: 7: Oofite hors; 8: Limestones with chert and pelagic marls with calcareousturbidite interheds; 9: Marls and marly limestones of pelagic facics: 10: Terrigenous turhidites: 11: Nodular limestones: 12: Marly limestoneswith radiolarians, and radiolarites; 13: Pelagic marls with ahundant planktonic Foraminilera: 14: Tidal-flat carbonated rocks with red clayinterheds; 15: Erosion surfaces; 16: Submarine volcanism: 17: Synsedimentarv slumps and hreccias:'18: Calcareous breccia: 19: Localolisthostromes; 20: ;Triassic diapirs rising from the sea floor.,. '

*

162

3

4 mmm m

65

E

G

I

L

-12 ® ® ® ®.13

163

5 M 9

A: Palaeogeographic reconstruction for pre-domerian Liassic.B: Palaeogeographic reconstruction for late Liassic.1: Palaeozoic basement; 2: Triassic; 3: Predomerian dolomites and limestones; 4: Supratidal environments; 5: Intertidal environments;Subtidal environments: 7: Areas of pelagic sedimentation within platform: 8: Carbonate sand bars 9: Rosso Ammonitico facies: lo: Volcanicand subvd1canic rocks; 11: Pelagic facies.

developed with episodes of tidal-flat deposition and locallywith an open-sea-influenced facies, suggesting the presence ofchannels, gulfs and embayments (Figs. 5A and 6A).

The hulk of the sediments is a thick sequence of limestonesof Hettangian-Sinemurian age, more or less dolomitized. Thisdolomitization usually affects only the lower part of theformation, but sometimes also the entire pile of shallow-watercarbonates. The study of the microfacies reveals diversetextures: oosparites, biosparites, intrasparites and biomicriteswith abundant algal debris (Codiaceae, Dasycladaceae,Cyanophythae, etc.) and with agglutinated Foraminifera(Lituolidae), other calcareous Fornianifera and invertebrateremains (Bivalvia., Gastropoda, Ostracoda, Echinodermata,Brachiopoda, etc.). In the upper part of the sequence,Lithiothis and Opisoma limestones may occur. The environ-,ment is interpreted as avery shallow carbonate platform, withthe different textures reflecting various energy regimesaccording to the relative position to the tidal level (GARCIA-

HERNANDEZ. ET At... 1976). The oolitic and intraclastic lime-stones with abundant algal remains reflect intertidal bars,while micfitic sediments with larger Foraminifera (Orbitop-sella, Haurania) are assumed to be from subtidal or lagoonalenvironments.

The Carixian is represented by a thin sequence of crinoidaland oncolitic limestones. Carixian (mostly' middle Carixian)and, locally, lower Domerian ammonites are frequently found(RrvAs. 1972). The Lower part of this formation shows similar,characteristics to those described from Sicily by .ILNKNNS(1971). However, the upper part of some sequences containsstratigraphic features (mud-cracks; herringbone crosshed-ding) indicative of a very shallow depositional environment'(intertidal and even supratidal).

On top of these limestones a `hard-ground' occurs, coincid-ing with a stratigraphical gap, preceeding partial break downof the carbonate platform:

Figure 6A shows a model for the environment and facies

1r7AFig. 6

RSV

6:

164

pattern for Pre-Domerian Liassic times. It comprises a shal-low carbonate platform with intertidal and emerged (supra-tidal) areas, the latter mainly during Carixian times. Figure 6B displays the equivalent model for the time after the break-down of the carbonate platform.

Post-Domerian Jurassic

During the late Liassic (Figs. 5B and 6B) the Prebetic andSubbetic Zones were clearly differentiated. In the PrebeticZone sedimentation of platform carbonates continued,,whereas in the Subbetic pelagic conditions were established.

Within the Subbetic zone, pronounced changes occur infacies and thickness due to differential sinking of the basinfloor. Thick marly basinal deposits with submarine volcanicrocks interbedded laterally changing to reduced and con-densed sequences of deposits `Rosso ammonitico' facies canbe found. The extent of the area with little or no sedimenta-tion varied in time (RIVAS. 1972; SEYFRIED. 1978).

During the Middle Jurassic, the southern border of thecarbonate platform occupied a more southerly position than itdid in the late Liassic (Fig. 5C.) In the Prebetic Zone, Inter-mediate units and part of the External Subbetic (Cabra andPandera units) formed part of this platform (Figs. 4 and 3respectively) The main deposits consist of oolitic limestones,locally passing into bioclastic or cherty micritic limestones,suggesting the existence of areas protected from waves andcurrents. In the rest of the Subbetic zone, troughs and swellswere differentiated in the basin, as a consequence of differen-tial subsidence. It caused frequent changes of facies andthickness. The volcanic activity still went on and reached itsmaximum in the Aalenian and Bajocian.

The differentiation into troughs and swells of the basin'persisted throughout the Late Jurassic, resulting in a mostcharacteristic constant palaeogeographic pattern.

In the Prebetic zone, after the Oxfordian, a sedimentationbegan of more or less pelagic type almost to the shoreline.This led to the deposition of nodular limestones during themiddle and late Oxfordian and of marls and marly limestonesduring the Kimmeridgian. Thick Portlandian formations formtheir cover, composed of carbonates laid down in a tidal-flat.The limit between the External and the Internal Prebeticcorresponds to the northern shore-line during this time.

In the Intermediate units, a strongly subsiding trough isdeveloped in which radiolaritic sediments overlain by calcare-ous turbidites are deposited with a maximum thickness to thesouth of Jaen.

The differential sinking in the Subbetic zone led to differentsedimentary areas by which the External, Median and Inter-nal Subbetic realms are defined (Fig. 7A). The thicker se-quence corresponds to the Median Subbetic and containsradiolarites as well as calcareous turbidite facies with sub-marine volcanic rocks. To the North and South (External andInternal Subbetic), the Late Jurassic formations consist ofnodular limestones ('Rosso Ammonitico' facies) of much

more reduced thickness.

Lower Cretaceous

The Lower Cretaceous in the Prebetic zone is continuous withthe uppermost Jurassic and consists, in the Berriasian, oflimestones with marls, deposited in a fluctuating environ-ment, which repeatedly evolves from supratidal (laminatedlimestones with mudcracks) to subtidal limestones and marlswith Clypeina jurassica FAVRE. Eastwards, the presence ofsome calpionellids denotes an open marine influence. Nodu-lar limestones with ammonites and calpionellids in the basalBerriasian and white marly limestones throughout the rest ofthe Lower Cretaceous are the predominant lithologies in theIntermediate units and the Subbetic zone. In the latter, thesefacies persist in the entire Lower Cretaceous. while in theformer they only extend up to the Hauterivian. In someregions of the Internal Subbetic (Ronda-Torcal unit) theLower Cretaceous is absent (Fig. 7B) due to a submarineerosion documented by a non-depositional surface betweenthe Upper Jurassic and the Upper Cretaceous (HOPPE. 1968;PEYRE. 1974; ROURGOIS. 1978).

In the Prebetic zone the shore-line kept approximately to itsuppermost Jurassic position, with emersion and erosion in theExternal Prebetic. The Internal Prebetic now presents verydiverse facies. The Lower Valanginian facies, for instance,change from West to East from tidal-flat, to lagoonal, reef andeven to pelagic (Fig. 5E). In the eastern region the Valangi-nian-Hauterivian boundary is characterized by sandy marlswith ammonites and Exogyra remains, while in the west-unfossiliferous lutites and sands denote a strong fluviatileinfluence (Weald facies).

An important palaeogeographic change took place in theBarremian; the Internal and' part of the External Prebeticwere occupied by marshes and lagoons where rich organicmaterials, intraclastic limestones and limestones with abun-dant Charophyte, were deposited (FOURCADE. 1970; reREz.1973; AZEMA. 1977; GARCIA-HERNANDEZ. 1978; RODRIGIJEZ-

ESTRELLA, 1978). These sediments record the beginning of acycle that becomes gradually more marine during the EarlyAptian (Bedoulian) ending with subtidal facies at the Bedou-lian-Gargasian boundary (GARCIA-HERNANDEZ. 1978, 1979).

The maximum transgression occurred in the late Bedulianwith coral reef facies and sandy calcarenite bars with Palor-bitoiina.

By Gargasian times the Prebetic zone was almost com-pletely invaded by continental terrigenous materials. In theExternal Prebetic these sediments rest unconformably ondifferent Jurassic formations (FOURCADE. 1970; AZI;MA 1977;GARCIA-HERNAN)EZ. 1978; RODRIGIJEZ-ESTRELLA. 1978). Later,

predominantly in the Internal Prebetic, marine environmentsare recorded, mostly of restricted marine; but also of openmarine character (limestones with Mesorbitolina andPsetldotoucasia). Renewed fluviatile sedimentation occurredin the late Albian with the deposition of clays and sands rich in

165

1 5 12MFig. 7

A: Palaeogeographic reconstruction for the Jurassic-Cretaceous boundary.B: Palaeogeographic reconstruction for the early Valanginian.1: Palaeozoic basement: 2: Triassic; 3: Jurassic: 4: Supratidal environment: 5: Intertidal environment: 6: Subtidal environment: 7: Restrictedplatform environment (lagoon); 8: Reefs; 9: Rosso Ammonitico facies; lo: Volcanic and subvolcanic rocks:. 11: Pelagic facies; 12: Calcareousturbidites.

quartzite pebbles (Utrillas facies). Another unconformity liesat the base of this formation (LOPEZ-GARRIno. 1971-a).

Throughout Barremian, Aptian and Albian times, turbidi-tic terrigenous sediments were deposited in the basin 'of theIntermediate units where they became interbedded withpelagic material (Fig. 8A). These turbiditic levels containwood debris and displaced Orbitolina, suggesting that theirsources received sediments from rivers in the north. Some-times during Aptian-Albian times the submarine fans movedto the South, causing the arrival of detritic sediments in theMedian Subbetic'(sANZ DE GAL.I)EANO. 1973; GONZALEZ-DONOSO

et al, 1974). In several areas of the Intermediate units, diapiri-cally rising Triassic material became, intercalated in the se-quence (FOUCAUL.T, 1971; GARCIA-HF.RNANDEZETAL.1973: SANZDE

GALDEANO.1973).

Upper Cretaceous

Figure 8B displays a reconstruction of the sedimentary basinat the beginning of the Late Cretaceous. It shows veryuniform conditions in contrast to those reconstructed for theAlbian (Fig. 8A).

The northward extension of the Cenomanian is rathersimilar to that of the Albian; however, dolornitized open-marine platform carbonates extend over nearly the entirePrebetic zone. The subsiding trough of the Intermediate unitsis filled up during this time and marls and marly limestoneswith planktonic Foraminifera cover the submarine topogra-phy from the Intermediate units to the Subbetic. Also in theCenomanian some Triassic masses were emplaced as olistho-stromes (COMAS, 1978).

M

166

M 5 IFig. 8

A: Palaeogeographic reconstruction for late Aptian-Alhian.1: Palaeogeographic reconstruction for Cenomanian.1: Palaeozoic basement; 2: Triassic; 3: Jurassic and Cretaceous (up to early Aptian); 4: Sands and lutites (Utrillas Formation); 5: Restrictedplatform environment (lagoon): 6: Carbonate sand bars; 7: Carbonate platform; 8: Turhiditic facies. 9: Pelagic facies,

An important palaeogeographic change in the PrebeticZone during the Senonian is the eastwards retreat of theshore-line. The lower Senonian limestones with Charophyteremains and with laminated intercalations are deposited ontidal flats and swamp regions. From the West to the East thereexist facies of Discorbis limestones, rudist limestones (both ofthem of lagoonal environment), reefal calcarenites, andpelagic marls with planktonic Foraminifera,

In the late Senonian the facies, changes seawards fromlacustrine and lagoonal, to marine carbonate platform.

Throughout the Intermediate units and the Subbetic,pelagic sedimentation prevailed with. pink and white marlsand marly limestones containing abundant Globohvncanaand nannofossils.

CONCLUSIONS

The palaeogeographic evolution of the External Zones of theBetic Cordillera is closely .parallelled by that of other AlpineMediterranean Mesozoic basins. BERNOULLI & JENKYNS (1974)described the Mesozoic facies of these basins with brief refer-ence to the Betic Cordillera, emphasizing the palaeogeo-graphical events noticed in this paper.

The beginning of the Jurassic is accompanied by the instal-lation of a carbonate platform over the germanic andalousianTriassic; GARCIA-HERNANDEZ ETAi.. (1976) compared these sedi-

ments to analogous ones found in N. Africa, the Apennines.Sicily, the Alps, the Carpathians, and the Jonian zone of theI lellenides; the sedimentation rate is equivalent to those of

t s

167

the recent Bahamas. The prevailing facies are of shallow-marine carbonate platform with episodes of tidal-flat andsupratidal deposition as described from the Calcare Massiccioformation of the Apennines (BERNOULLI & WAGNER 1971: COL-

ACCICHI ET AL.. 1975).

In the Subbetic zone the uppermost levels of this calcareoussequence are composed of Carixian crinoidal limestoneswhich are also present, with similar age and facies, in otheralpine basins (i.e. Sicily, JENKYNS. 1971; CATALANO & D'ARGENIO.

1978).Between the middle Carixian and early Domerian ages (180

Ma) the change from shallow water to pelagic facies occurred.an event which coincides with a breakdown of the maincarbonate platform all over the Mediterranean domain andwith early stages of opening of the Central Atlantic (BERNOULLI& JENKYNS, 1974; SCANDONE, 1975; BIJU-DUVAL ET At, 1976; TAP-

PONIER. 1977).

After this event in the External Zones of the Betic Cordill-era two main realms are differentiated: the Prebetic andSubbetic Zones.

The Prebetic Zone constitutes, throughout Mesozoic times,a border zone of a geosynclinal area, linked to the NW toemerged areas, and characterized by marginal facies compris-ing tidal-flats, lagoonal and open-marine platform carbonate,with frequent clastic episodes of fluvial or coastal sedimenta-tion; many facies associations are in fact similar in lithology tocoeval ones described from elsewhere not only in the Mediter-ranean area but also in the North of Europe. The Purberckfacies, Weald facies and Urgon facies have been recognized.

In the Subbetic zone, sedimentation was pelagic from themiddle Liassic onwards. Troughs and swells are related todifferential subsidence of a fractured and thinned continentalcrust. In some of the troughs, interbedded with pelagic sedi-ments, subvolcanic and submarine volcanic rocks appear.Overall, Mesozoic sedimentation, occurred in a continentalmargin of the Atlantic type, analogous to other alpine regions,e.g. the Apennines 1976).

The main pelagic facies, which have their equivalents inother Alpine regions are:, (1) Grey limestone-marls interbeds(biomicrites); (2) Rosso Ammonftico and red nodular limes-tones; (3) Radiolarites and marl with radiolarians; (4) Cal-careous turbidites; and (5) red to white biomicrites containingplanktonic foraminifera.

ACKNOWLEDGEMENTS

The authors are very grateful to D. Bernoulli (Basel), J. M.Fon.tbot6 (Barcelona), J. J. Hermes (Amsterdam), P. Scan-done (Pisa), R. 'Grumpy (Zurich) and G. Westerniann(Ontario) for the comments and suggestions regarding themanuscript. They wish to express their sincere thanks toJ. Westermann (Ontario) and M. Orozco (Granada) for thecorrection of the English text.

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