Regional correlations across the Internides-Externides front (northwestern Rif Belt, Morocco) during the Late Cretaceous-Early Burdigalian times: palaeogeographical and palaeotectonic implications

KH. EL KADIRI 1, R. HLILA 1, C. SANZ DE GALDEANO 2, A. C. LOPEZ-GARRIDO 2, A. CHALOUAN 3, F. SERRANO 4, A. BAHMAD 5, A. GUERRA-MERCH~,N 4 & H. LIEMLAHI 1 1University Abdelmalek Essaadi, Facultd des Sciences, Dep. Geology, BP 2121, 93003 Tetuan, Morocco (e-mail: khkadiri@fst, ac. ma) 2University of Granada, Facultad de Ciencias, Dep. Geodinamica, Av. Fuente Nueva, 18002 Granada, Spain 3Universitd Mohammed V-Agdal, Facultd des Sciences, Dep. Geology, BP 1014, 10000 Rabat, Morocco 4University of Malaga, Dep. Ecologia & Geologia, Teatinos, Malaga, Spain 5Socidtd Nationale d'Etudes du Ddtroit de Gibraltar (SNED), 31 r. Al Alaouyines, Rabat, Morocco

Abstract: New insights into the palaeogeographical evolution of the Rifian Internides and their external surroundings are inferred from six key stratigraphic successions selected across the Internides-Externidesfront. These successions span a time interval ranging from the late Cretaceous to the early Burdigalian. The main results are: (1) important lost palaeogeographical domains should be located during the late Cretaceous-Eocene between the present-day Ghomarides and the Dorsale Calcaire, on one hand, and between the Predorsalian units and the Flysch Trough as isolated carbon- ate platforms, on the other hand; (2) during the late Eocene-early Oligocene an extensional tectonic event, well marked in the Dorsale Calcaire, caused the collapse of these platforms and resulted in olistostromes and coarse-grained breccias in both the Predorsalian and the Btni Ider areas; (3) by the beginning of mid-Oligocene, an overturning contractional event in the Ghomarides resulted in the regional onset of the siliciclastic depositional regime throughtout these palaeogeographical areas; (4) during the Aquitanian-early Burdigalian, the stepwise return of pelagic deposition in the Ghomarides indicates extensional phases, whereas the homogenization of the same pelagic facies over the Dorsale Calcaire and its external surroundings may indicate that the previously distant palaeogeographical areas were brought nearer (i.e. just before large-scale thrusting).

The Gibraltar arc consists of two juxtaposed struc- that the filling of the main flysch depocentres in the tural domains: (1) the Internal Domain, (Internides) External Domain occurred shortly before the parox- where the orogenic contractions started from Oligo- ysmal nappe emplacement, or even as syntectonic cene time and generally resulted in high-grade deposits, competing hypotheses were presented for metamorphism, particularly in its innermost part; the equivalent strata in the Internal domain. Some (2) the External Domain (Externides), where the workers attempted to link them to post- outward migrating orogenic contractions during orogenic deposits transgressively sealing the parox- Miocene time progressively produced piggy- ysmal structures (e.g. Durand-Delga et al. 1993), back-foredeep basins and ramp-anticline struc- whereas others considered them as recording a tures. The culmination of these phenomena during near-continuous marine regime entirely predating the paroxysmal phase resulted in a high accretion- the main orogenic events (e.g. Maat6 1996). ary prism and successive large-scale gravitational Recently, detailed stratigraphic studies of the processes (Chalouan et al. 2006). Oligo-Miocene cover were carried out in the Mala- The Tertiary sedimentary filling within and/or guides (Guerrera et al. 1993; Martin-Martin et al. close to these forming basins was differently inter- 1997) and the Ghomarides (Feinberg et al. 1990; preted in both domains. Whereas there is acceptance E1 Kadiri et al. 2000, 2001). They showed that the

From: MORATTI, G. & CHALOUAN,A. (eds) 2006. Tectonics of the Western Mediterranean and North Africa. Geological Society, London, Special Publications, 262, 193-215. 0305-8719/06/$15.00 9The Geological Society of London 2006. 194 KH. EL KADIRI ETAL.

Oligo-Miocene sedimentary cycles were episodi- the external zones in deciphering the tectonic cally induced by extension-related marine encroach- and/or eustatic significance of their coeval depos- ments punctuating contractional events during a its. Thus, these two domains can no longer be polyphase tectonic scenario (Comas et al. 1992; taken as two independent geological realms when Garcia-Duefias et al. 1992; Chalouan et al. 1997). reconstructing the tectonosedimentary evolution of The aim of this paper is to extend this approach to the Gibraltar arc evolution. time-equivalent depositional series belonging to both sides of the Internide-Externide front (i.e. the Dorsale Calcaire, Predorsalian and B6ni Ider Geological background series). Some of the studied series are newly dated The Rifian Internal zones (Fig. 1) consist of a and/or described herein. Good examples are pro- complex nappe pile resulting from the westward- vided by: (1) the Dradia-E10nzar and Talembote vergent stacking of three distinct units: the Sebtides, sections in the Ghomaride Domain; (2) the Hafat Ghomarides and the Dorsale Calcaire. Srir section in the Dorsale Calcaire; (3) the well- The Sebtides consist of varied metamorphic exposed Tamezzakht succession (located in the Pre- nappes, including a granulitic-mantle ultramafic dorsalian zone) that belongs to this frontal zone, to unit, which is underlain (Sebta massif) and overlain which special attention will be paid here. Its (B6ni Bousera massif) by gneiss and schists extended time-range (from the late Cretaceous the of upper-crustal affinities. These in turn are overthrust early Burdigalian), gravity-flow events, and well- or are overlapped by detached high-pressure- delineated discontinuities are used to monitor low-temperature metapelitic strata, mainly of regional-scale correlations across the Internal- late Palaeozoic-Triassic age (Federico units; External Domains (see El Kadiri et aI. 2005, for Bouybaou~ne et al. 1995), a fact that supports the detailed sedimentological data). attribution of the Sebtide nappe emplacement to the The general interest of this approach is to Alpine orogeny. The ultramafic rocks of B6ni promote the correlation between the internal and Bousera essentially consist of spinel-bearing

Fig. 1. Geological map of the northwestern Rif belt and location of the study areas (see Fig. 2 for details). REGIONAL CORRELATIONS, RIF INTERNIDES-EXTERNIDES 195 lherzolites. They were interpreted as a hot astheno- palaeogeographically corresponded to the deepest spheric dome (Loomis 1975; Platt & Vissers 1989) part of this palaeomargin (e.g. Chrafate Klippes or conversely as pre-Alpine slivers uprooted from units, Assifane units, E1 Hatimi 1982; El Kadiri Precambrian infracrustal levels and emplaced in the 1984; El Hatimi et al. 1988; Ben Ya'ich et al. upper crest (Kornprobst 1974). Integrated approaches 1988). Triassic-earliest Jurassic, thick-bedded, including detailed structural field-survey (Reubert shallow-water carbonate limestones make up the et al. 1982; Saddiqi et al. 1988) and geochronological main massifs of the Dorsale Calcaire. They may analyses (Sanchez-Rodriguez & Gebauer 2000) be topped with polyphase palaeokarst surfaces in showed that the lower Sebtide lherzolites were the Internal Dorsale (El Kadiri 1991; Maat6 1996) initially derived from a lithospheric mantle, and and with Fe-encrusted hardgrounds in the External were subsequently emplaced as tectonic slivers Dorsale (El Kadiri 2002a,b). within upper crustal levels. This scenario occurred In the Internal Dorsale, reduced pelagic series in two main stages, during Tethyan rifting at about may diachronously onlap the massive carbonate 183-131 Ma, and during Palaeogene subduction- formations. The most noteworthy of these are collision (Chalouan et al. 2001; Michard et al. developed in rosso-ammonitico facies during the 2002). Geochemical data (Targuisti 1994), and even Domerian-Toarcian, and in Saccocoma- and/or the stratigraphic record (El Kadiri et al. 1992, 1995), Calpionella-rich mudstones during the Tithonian- support the idea that the B~ni Bousera-Ronda perido- Berriasian. A long-lasting palaeokarst history tites derived from an asthenospheric dome, the ascent occurred in the intervening time span (El Kadiri of which started as early as Mesozoic time (Sanchez- 1991; E1 Kadiri et al. 1992), a feature that recalls Rodriguez & Gebauer 2000). The conditions and kin- the Mid-Late Jurassic 'Main Gap' found by ematics of their final exhumation as well as of that of Farinacci (1996, 2002) and Farinacci et al. (1997) the surrounding metamorphic rocks are still a matter in the Central Mediterranean Apennine areas. The of debate (see, for example, the discussion by most distinctive features of the External Dorsale Balanya & Garcia-Duefias 1987; Lonergan & White are: (1) the rosso-ammonitico facies and cherty 1997; Azafion et al. 1998; Morales et al. 1999; limestones, which can start as early as the Sinemur- Azafion & Crespo-Blanc 2000; Calvert et al. 2000). ian (e.g. Arnioceras-rich strata, Fallot 1937; Griffon The Ghomaride nappes (Kornprobst 1974; 1966); (2) the red and/or green radiolarites, the Chalouan 1986) generally thrust the Sebtides. onset of which occurred as early as the Liassic- They mainly consist of Palaeozoic schists, which Dogger transition (El Kadiri 1984, 1991). For this compositionally resemble their Hercynian homo- reason, they were considered as being amongst logues known at present in the eastern Moroccan the earliest continental-margin-related Jurassic, Meseta (Chalouan 1986), a fact that supports a biosiliceous deposits in the Tethyan realm (De palaeogeographical reconstruction in which they Wever et al. 1985). They continued until early originally derived from an eastern domain, where Tithonian time (El Kadiri 1991). they formed the westernmost part of the 'A1Ka- In both Dorsale units, Cretaceous succes- PeCa' palaeoplate (Bouillin et al. 1986; Chalouan sions recorded important hiatuses during the & Michard 1990; Guerrera et al. 1993). Lithofacies, Hauterivian-Albian pro parte and the early Seno- metamorphism and the position within the nappe nian, the best characterized ones being the Campa- pile allow four main nappes to be distinguished nian and Maastrichtian Globotruncana-rich (Chalouan 1986; Chalouan & Michard 1990). marly mudstones referred to as 'Capas Rojas' and The Dorsale Calcaire was first interpreted as cor- 'Capas Blancas', respectively (El Kadiri 1991). responding to the Alpine Ghomaride cover (Durand Palaeogene successions consist of: (1) thin Delga et al. 1962; Kornprobst 1974) detached from nodular black shales of Paleocene age; (2) varie- its Palaeozoic basement during Tertiary thrusting. gated marl-nummulitic sand alternations of However, characterization of an independent Meso- Eocene-mid-Oligocene age (Griffon 1966; Raoult zoic Ghomaride cover with respect to the carbonate 1966; Nold et al. 1981; Maat4 et al. 1993; Hlila Jurassic strata of the Dorsale Calcaire, on one hand 1994, 2005; Maat6 1996); (3) micaceous rust- (Maat6 1984, 1996; E1 Kadiri 1991; E1 Kadiri et al. coloured sandstones, during the late Oligocene- 1992), and detailed stratigraphic analyses of the (?)early Aquitanian. entire Mesozoic successions of both the Internal Tectonically, the fact that the latter deposits are and the External Dorsale, on the other hand (Nold considered as being the youngest strata trapped et al. 1981; E1 Kadiri 1984, 1991; Olivier 1984; between different slices (Nold et al. 1981) E1 Hatimi 1991; Maat6 1996), led to the two latter suggested a first phase of thrusting during the Aqui- being assigned to the palaeomargin bordering west- tanian. Later, characterization of early Burdigalian wards and/or southwards the Rif 'Internal zones'. marine strata involved in both the internal and This result appears in accordance with the concept external fronts of the Dorsale Calcaire (Feinberg of a 'Predorsalian zone' (Didon et al. 1973) that & Olivier 1983; Ben Ya'ich et al. 1986; Feinberg 196 KH. EL KADIRI ET AL.

Fig. 2. Geological-structural setting of the areas including the investigated successions. (a) Jbel Moussa Group (modified from Komprobst & Durand Delga 1985); (b) northern part of the Tamezzakht sector (this work); (c) main lithological components of the Mauretanian series cropping out the vicinity of the Oued-E1-K6bir in the B~ni Ider area (simplified from Didon 2006); (d) example of a residue of the karstified Ghomaride carbonate cover close to the Internal Dorsale (El Onzar succession, simplified from Raoult 1966); (e) Ghomaride siliciclastic cover in the Talembote area (simplified from E1 Kadiri et al. 2001), (f) western Chrafate Klippes, a good example of the Predorsalian olistostromes REGIONAL CORRELATIONS, RIF INTERNIDES-EXTERNIDES 197 et al. 1990; E1 Kadiri et al. 2001) led researchers to Predorsalian zone and an external ridge. The 'Tar- envisage a second phase, during which the whole iquide Ridge' is herein used in the strict sense of a Dorsale nappe pile underwent large-scale thrusting high palaeogeographical zone delivering shallow- before being trapped between the Ghomaride ter- water carbonate material (calciturbidites) to both ranes and the flysch-nappe domain. In some seg- the Predorsalian and the Mauretanian trough ments (Haouz chain), the latter event resulted in a during the late Cretaceous-early Oligocene. double 'encapuchonnement' process (e.g. Raoult The External zones are dominated by large-scale 1966; Hlila 1994, 2005), a kinematic scenario that 'parautochthonous' terranes (the Tangiers, Ketama explains the backthrusting and related fan-shaped and Loukous units, mainly), and their overriding structures. sandstone-flysch nappes. These in turn may thrust The northern part of the Rif calcareous each other along well-delineated parallel structures, chain (Dorsale Calcaire) is occupied by the Jbel which act as the topographical lines of the Gibraltar Moussa Group, which is dominated by four arc. Although palaeogeographical reconstructions kilometre-scale juxtaposed tilted blocks (J. of the External zones still remain a subject of Moussa, J. Juimaa and Ras Leona and Leila) of a debate, especially for the Mesozoic, there is agree- Jurassic continental passive palaeomargin (El ment that their tectonosedimentary evolution Kadiri et al. 1990; E1 Hatimi 1991). All these during the Tertiary was primarily conditioned by blocks exhibit Triassic-early Cretaceous succes- piggy-back basins and ramp-anticline structures, sions that strongly recall the Spanish Penibetics both generated by deep detachment planes (e.g. (Fallot 1937; E1 Hatimi 1991), the Gibraltar and Morley 1987, 1988, 1992; Ben Yai'ch 1991). Los Pastores massifs (Durand Delga & Villiaumey Close to the internal border, the External 1963), and/or the Southern Middle Subbetics (El Domain (the so-called Intrarif) was strongly Kadiri et al. 1990). The fact that the J. Moussa deformed so that its parautochthonous units Group is thrust directly over the Tangiers units locally show schistosity (Andrieux 1971; Frizon and its Spanish equivalents (Gibraltar and Pas- de Lamotte 1985) and the flysch successions tores, both occurring in the external Campo de were totally uprooted. The deformation style is Gibraltar area), led Durand-Delga (1972, p. 274) predominantly characterized by duplex structures to assign all these calcareous blocks to an external and imbricate slices. 'Cretaceous cordillera' separating the Mauretanian Stratigraphic reconstructions carried out mainly and the Massylian basins. This palaeogeographical by Durand-Delga (1972) and Durand Delga & setting proved to be identical to that proposed by Didon (1984a,b) led researchers to recognize the Raoult (1974) for the Algerian 'Prekabyle base- two main flysch successions previously defined ment'. Concurrently, Didon et al. (1973) defined in the Kabylian domains (Bouillin et al. 1970): the Predorsalian units as corresponding to a (1) the Mauretanian series, which includes in its narrow basin externally bordering the Dorsale Cal- lower half the Tisir~ne early Cretaceous calciturbi- caire units. It is noteworthy that the Predorsalian dites and holoquartzous sandstones, and in its upper zone was characterized by the Aquitanian Numi- half the B6ni Ider late Cretaceous-Aquitanian cal- dian-like sandstones (the so-called 'Beliounis citurbidites and micaceous sandstones; (2) the sandstones'), which were fundamentally defined Massylian series, which may encompass in a in the J. Moussa Group itself. Thus, this Group single stratigraphic column the Barremian-Albian implicitly bears the double definition of a olive-green sandstone flysch (Massylian sensu

Fig. 2. Continued. (simplifiedfrom E1 Kadiri 1984). 1, low-grade-metamorphosed Triassic strata (Federico units, upper Sebtides); 2, Palaeozoic schists; 3, Verrucano-type Triassic red sandstones; 4, late Triassic dolomites; 5, earliest Liassic massive limestones; 6, mid- to late Liassic pelagic successions (cherty limestones and/or rosso-ammonitico facies); 7, mid- to late Jurassic red radiolarites; 8, latest Tithonian-Berriasian Aptychus-bearing calciturbidites; 9, Aptian-Albian, thick-bedded, fine-grained sandstones (Tisirene flysch); 10, carbonate-poor, green pelites (Tangiers units, Campanian-Maastrichtian mainly); 11, Campanian-Maastrichtian (mainly) calciturbidites of the Mauretanian series and the Chrafate Klippes; 12, Microcodium-bearing Paleocene calcarenites; 13, Nummulite-rich, white massive grainstones (El Onzar succession, (d)) and calciturbidites (Tamezzakht and Oued-E1-K6bir areas; (b) and (c), respectively); 14; late Oligocene chaotic mixture of the Talembote area, reworking Triassic strata, with a basal coarse- grained conglomerate rich in granite and basalt pebbles; 15, latest Eocene-mid-Oligocene variegated marls with large- scale olistoliths, particularly in the Predorsalian zone; 16, late Oligocene-Aquitanian yellow soft marls with large- scale olistoliths inherited from Triassic and Eocene massive carbonates (Tamezzakht and Talembote successions, (b) and (e), respectively); 17, early Burdigalian Vifiuela-type green pelagic marlstones with similar large-scale olistoliths (in Tamezzakht and Talembote areas); 18, late Oligocene-early Burdigalian micaceous sandstones (the so-called 'B6ni Ider' Flysch); 19, late Oligocene-Aquitanian holoquartzose yellow sandstones (the so-called 'Beliounis' sandstones); 20, early Burdigalian, carbonate-poor, tobacco brown pelites and holoquartzose tobacco brown channelized sandstones (Talembote and Chrafate Klippes). 198 KH. EL KADIRI ETAL. stricto) and the late Oligocene-Aquitanian Numi- In both outcrops, white nummulitic sandstones and dian sandstones. However, in the latter case upper Nummulite-rich massive grainstones rest on early Cretaceous transitional strata are not yet clearly Liassic white massive limestones after a conspicuous characterized. palaeokarst discontinuity (palaeokarst surface 1, Figs On the whole, these flysch series were used to 2 and 3). This may indicate that the Ghomaride ter- define the Maghi'ebian 'Flysch Trough' (Didon ranes experienced a protracted emersion history et al. 1973; Bourgois 1978; Durand-Delga 1980; during the Mesozoic-Paleocene, resulting in the Martin-Algarra 1987), along which the Maureta- near-complete removal of their carbonate cover. nian flyschs were located, close to the A1KaPeCa The stratigraphic top of the nummulitic white palaeomargin (Bouillin et al. 1986). In contrast, limestone bar (10-30 m) in turn shows an import- the Massylian flyschs were located close to the ant palaeokarst surface (palaeokarst surface 2, African palaeomargin (e.g. Raoult 1974). In the Rif Fig. 3). In some cases (El Onzar succession), domain the latter palaeomargin is represented by karstic relief (small-scale kamenitzas and palaeo- the Jurassic terrigenous series (mainly 'Ferrysch' sinkholes) is filled with red to brown sandstones successions, Wildi 1981) known in the M6sorif and made up of the 'en-echarde'-type quartz, which Pr~rif zones (e.g. compiled data of Ben Yai'ch originated from pedological processes (Meyer 1991; Benzaggagh 1996). 1987). An algal-Discocyclina-rich grainstone bed On the basis of the stratigraphic data given (0.10-1 m) transgressively rests on the palaeokarst below, we shall see that the Flysch Trough can no surface. It is generally capped with a remarkable longer be considered to be formed by a single, Fe-crust (Fe-HG, Fig. 3), from which bacteria- large-scale homogeneous basin, as the existence produced Fe-epigenesis processes (e.g. Prdat of external isolated platform(s) subdivided it into et al. 2000; E1 Kadiri 2002a) may extend several at least two elementary basins (see also E1 Kadiri decametres downwards into the host rock, which et al. 2003). becomes rust coloured. Outcrop survey shows that this Fe-crust also may directly cap the under- lying nummulitic bar when the transgressive Stratigraphic framework of the selected Discocyclina-rich deposition is laterally lacking, successions as occurs in many transgressive deposits (e.g. lag gravel of Plint (1988), transgressive lag deposit Six study areas (Fig. 2) have been selected from the of Ftirsich et al. (1991), transgressive lags of principal domains known in the Internal zones and Burkhalter (1995) and hiatal shell concentrations the surrounding External ones, namely the Ghomar- of Rivas et al. (1997), among others). Thus, ides, the Dorsale Calcaire, the 'Tariquide Ridge' the double discontinuity (palaeokarst+HG) at and the Flysch Trough. Their stratigraphic succes- the top of the nummulitic bar may best be classi- sions are thoroughly reassessed (Fig. 3) and their fied as a rock-ground surface in the sense of possible juxtaposition during the early Burdigalian Clari et al. (1995). is outlined to better assess the sources of the carbon- Dating controls based on benthic Foraminifera ate clastic material. The Tamezzakht succession lead us to assign the stratigraphic top of the nummu- appears to be the most complete, as it spans a wide litic bar to the late Lutetian (e.g. Raoult 1974; see time-interval ranging from the latest Cretaceous to also Table 1, sample ONZ 5). the early Burdigalian. Thus, it provides a rare oppor- Yellow to rust-coloured marls (20-30 m) sharply tunity to appraise a long-term tectonosedimentary overlie the Fe-hardground surface. In their upper evolution through a single stratigraphic column. half they contain fine-grained sandstone intercala- tions, which progressively dominate the deposi- In the Ghomaride domain tional regime (see the possible interpretation below). They yield planktonic Foraminifera indicat- The El Onzar and Dradia successions (Figs 2d and ing a latest Lutetian-Early Bartonianage (Table 1, 3) crop out close to the Ghomaride-Dorsale bound- sample ONZ 10) ary in the northernmost part of the Ghomaride In the Talembote area (Fig. 2e) located 40 km domain, north of the city of Tetuan. They provide south of the city of Tetuan close to the Internide- some of the best evidence known for the Ghomaride Externide front, decametre-scale sedimentary Eocene cover. In addition to the lithostratigraphic klippes are embedded within an Aquitanian-early description and dating controls given by several Burdigalian siliciclastic matrix (Fig. 3). They workers (e.g. Raoult 1966; E1 Kadiri et al. 1992; exhibit an identical Liassic-Eocene stratigraphic Maat~ 1996) and completed herein, we have succession with the same discontinuities and litho- found two complex discontinuity surfaces in these logical components, and their presence here may successions, at the very base of the Eocene strata have an important bearing on the palaeogeographi- and at their top. cal reconstructions (see below). REGIONAL CORRELATIONS, RIF INTERNIDES-EXTERNIDES 199

Fig. 3. Stratigraphic correlation of the studied successions, selected from distinct domains of the northwestern Rif belt: the Ghomaride domain (Dradia-El Onzar units, Talembote succession), the (Calcareous) Dorsale Calcaire (Hafat Srir succession) of the Internal zones; the Predorsalian fringe (B6ni Imrane succession), and the B6ni Ider area (Oued-El-K6bir section) of the External zones (see text for details). The upper part of the figure tentatively proposes a possible reconstruction of this scenario during the early Burdigalian, i.e. just before the orogenic paroxysm (the shortening distance D? remains uncertain). Grey shading indicates the sampling levels from which new biostratigraphic dates are given in Tables 1 and 2. 200 KH. EL KADIRI ET AL.

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The most noteworthy feature of the Talembote pre-altered, rust-coloured Triassic dolomites. This Tertiary succession is the facies contrast, which is basal breccia passes up into a thinning-upward well marked in the field, between its four sedimen- alternation (c. 150 m thick) of pelagic marls and tary formations ranging from the late Oligocene to graded breccias. Well-developed Fe-crusts carpet the early Burdigalian (El Kadiri et al. 2001, and near all the basal breccia beds. Yellowish pelagic Fig. 2e). For regional correlation, it is relevant to marls, between them, yield planktonic Foraminifera note the sharp facies change from the yellow soft indicating a latest Eocene age (Table 1, sample marls of the second formation (latest Oligocene- SAD 1). The overlying marly succession, which Aquitanian pro parte) to the green pelagic marl- spans the early to mid-Oligocene interval (Maat~ stones of the overlying third formation (earliest et al. 1993; Table 1, samples SAD 2, 7 and 10), Burdigalian). The former facies is particularly rich comprises a rhythmic metre-scale alternation of in planktonic Foraminifera (El Kadiri et al. 2001) carbonate-rich green marls and carbonate-poor and contains in its upper half spaced intercalations pink marls, a fact that may be ascribed to cycles of yellow Alozaina-type sandstones, a facies wide- related to the calcite compensation depth (CCD) spread in the Aquitanian Malaguide cover and that fluctuation, redox and/or productivity (Eicher & of the northern part of the Ghomaride terranes. Diner 1991; Einsele & Ricken 1991). The Hafat The second contains siliceous horizons and strongly Stir marly alternation may satisfactorily be used recalls the Vifiuela-type pelagic deposition to interpret the origin of the widespread early to (El Kadiri et al. 2001). mid-Oligocene 'variegated marls' as the result of Various coarse-grained breccia flows are interca- reworking and mixing by slope processes of the lated within the Talembote pelagic successions. All same kind of cyclic deposits. exhibit the same mixture of carbonate and meta- These marly deposits are sharply overlain, after an morphic clastic material, with the ubiquitous erosive surface, by micaceous, wood-debris-beating, Nummulite-rich and reefal boundstone blocks rust-coloured sandstones, probably of late Oligo- derived from a lost Palaeogene carbonate platform. cene-Aquitanian age (Hlila 2005). The onset of this Also ubiquitous are granitic and alkaline-basalt siliciclastic depositional regime may be ascribed to pebbles. The former were discovered in situ a second extensional event, as shown by numerous within the Carboniferous Marbella conglomerates, synsedimentary normal faults. In thin section the from which they are presumed to have been rust colour is proved to be due to the presence of a derived. In contrast, the origin of the alkaline large amount of pre-rubefaction, palaeosoil-derived basalts still remains unclear. carbonate clasts together with white and black In the Internal zones of the Betic Cordillera, the quartz grains. coeval early Burdigalian Las Millanas-Vifiuela Formation contains a basal conglomerate exhibiting In the Predorsalian zone the same clastic mixture. This may indicate that the source of supply was the same and had a wide The most representative successions of the Predor- palaeogeographical extent. Otherwise, it is relevant salian zone crop out in the well-studied Chrafate to note the presence, within the Spanish early klippe area (Didon et al. 1973; Lespinasse 1975; Burdigalian conglomerates, of almost unaltered Nold et al. 1981; E1 Kadiri 1984, 1991; Olivier blocks and pebbles of the usual Alpujarride- 1984; Ben Yai'ch et al. 1988) where the early Oligo- Sebtide facies, namely peridotites and garnet cene 'variegated marls' (Fig. 2f) form decametre- gneiss. Such pebbles have not yet been discovered to hectometre-scale sedimentary klippes, inherited in the Ghomaride cover. from Dorsale-type lost units, and pass upward into late Oligocene-Aquitanian Numidian-like In the Dorsale Calcaire sandstones (i.e. Beliounis sandstones, Didon et al. 1973). These two stratigraphic components (olisto- In the Dorsale Calcaire the most pronounced dis- stromes and sandstones) are separately known in continuity is delineated by the widespread late the Internal domain and the External one, respect- Eocene-early Oligocene Breccias Nummuliticas ively. As part of this peculiar zone we would (Nold et al. 1981) that independently rest on like to consider the Tamezzakht stratigraphic normal-fault-denuded Triassic or Jurassic strata, succession (Figs 1, 2b and 3), which also combines which pinpoint a regional extensional event. The features separately known in the Internal domain Hafat Srir section, cropping out in the northern and the External one. This succession displays in part of the Internal Dorsale (south of the city of its lower half a late Cretaceous-early Oligocene Tetuan), provides a good example of this: it starts calciturbidite-shale alternation, similar to that of with a 5 m thick, ungraded, coarse-grained nummu- the external B~ni Ider series. In contrast, its upper litic breccia bed (facies R1 of Lowe 1982; facies F3 half is chiefly made up of early to mid-Oligocene of Mutti 1992) that directly reworks pedologically variegated pelagic marls and rust-coloured 202 KH. EL KADIRI ET AL. sandstones. The latter are developed in the same half of the B6ni Imrane succession (c. 30 m). Dorsale-type facies (see Table 2 for dating con- They can be accompanied by a channelized, trols). They pass upward into late Oligocene-early coarse-grained basal division, which reveals that Burdigalian pelagic deposits made up of yellow the black mudstones came from up-slope pelagic marls-green marlstone couplets identical to those muds. They are sharply overlain by c. 5 m thick, previously described in the early Miocene Ghomar- thin-bedded calciturbidites with the sandy fraction ide cover. In addition, the intercalation within the being rich in penecontemporaneous Nummulites late Oligocene-Aquitanian levels of the Beliounis- of Eocene age. Hence, there has been an important type sandstone facies supports the attribution of the environmental change affecting the source area Tamezzakht succession to the Predorsalian zone. across the Paleocene-Eocene boundary, from In thin section, the calciturbidite flows com- exporting plankton-dominated muds into producing monly reveal the presence of carbonate clasts, and shedding shallow-water-rich bioclastic sands whose facies strongly recalls the Internal together with an important lithoclastic fraction Dorsale Jurassic series, namely the shallow-water deriving from its carbonate substratum. A channe- white massive grainstones (earliest Liassic) lized white, Nummulite-bearing sandstone bed and the Calpionella-Saccocoma-rich mudstones (WNS, Fig. 3) occurs in the intervening the strati- (Tithonian-Berriasian). However, the interposition graphic levels. The latter facies also appears at the of the External Dorsale between the Internal one very base of both the Eocene deep-sea calciturbi- and the Predorsalian zone, on the one hand, and dites of the Tamezzakht succession and the the proximal character of the calciturbidite dis- Eocene shallow-water, limestone bar of the Gho- charges, on the other, lead us to suggest a distinct maride cover, a result that suggests key strata of carbonate source with respect to the Internal regional correlation potential (WNS, Figs 3 and 4). domain. Palaeocurrent directions that we have A 3-5 m thick, coarse-grained, poorly graded measured on the bed surfaces of the calciturbidite conglomerate bed sharply overlies the calciturbidite interval are N70~ ~ with the current flowing interval. It is covered with an Fe-crust and probably towards the internal zones (from WSW to ENE, pinpoints the same extensional event that resulted in i.e. from an external source). In the overlying silici- the latest Eocene-early Oligocene chaotic breccias clastic interval the current direction is N20~ ~ in the Internal Dorsale and the Tamezzakht succes- mainly N30~ ~ flowing from SW to NE. Thus, sion. The B6ni Imrane Palaeogene series ends with the clastic material of the Tamezzakht succession a shaly interval (most probably of early to mid- could be sourced from an external lost terrane, a Oligocene age, by comparison with dating controls result that fits well with the 'Tariquide Ridge' obtained from Tamezzakht similar levels), made up hypothesis (Durand-Delga 1972) and recalls the in its lower half of ochre-red, lime-poor shales with Penibetic and/or Ultra-Internal Subbetic seamounts thin intercalations of calciturbidites, and in its upper of the southern Betic Cordillera. half of variegated marls. The most noteworthy feature of the Tamezzakht The Oued-E1-K6bir section exhibits the same pelagic marly deposits (late Oligocene-early lithostratigraphical features, particularly: (1) the Burdigalian) is the rhythmic alternation of yellow WNS key strata; (2) the Fe-crust-capped, chaotic soft marls and green marlstones. In the Ghomaride breccia overlying the Eocene calciturbidites; (3) cover, both facies are strictly limited to the latest the early to mid-Oligocene ochre-red shales, a Oligocene-Aquitanian and the early Burdigalian, facies well known in the remainder of the external respectively. B~ni Ider area (the so-called 'flysch color6'). Regardless of the relative palaeogeographical Surrounding External Domain position of the Oued-El-K6bir section, the entire Palaeogene stratigraphic evolution outlined in the Two Paleocene-mid-Oligocene successions with Internal domain and close to its border seems to stratigraphic features similar to those previously have been strongly influenced by a neighbouring described can be selected from the surrounding carbonate platform. By the beginning of the late External Domain: the B6ni Imrane succession, Oiigocene, the total disappearance of the clastic which crops out north of the city of Tetuan carbonate material was combined with the onset between the Predorsalian zone and the Tangiers of the siliciclastic depositional regime. Thus, at unit, and the Oued-E1-Kebir succession cropping that time, the supplying carbonate platform(s) was out along the main river crossing the B6ni Ider (were) probably destroyed and/or drowned under area, 25-30 km SW of the city of Tetuan (Fig. 2c). the siliciclastic accumulations. In both cases, the Black, thick-bedded cherty mudstones rich in sharp contact between the early-mid-Oligocene small planktonic Foraminifera (Subbotina pseudo- calciturbidite-intercalated red shales and the late bulloides (Plummer) and Planorotalites compressa Oligocene sandstone-intercalated yellow marls (Plummer)) of Paleocene age make up the lower may be regarded as a depth-equivalent of the REGIONAL CORRELATIONS, RIF INTERNIDES-EXTERNIDES 203

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~ q'3 204 KH. EL KADIRI ET AL. drowning-suffocation discontinuity in the sense of cases dating controls do not allow us to distinguish Schlager (1989, p. 7). them from the underlying condensed late Cre- Petrographical evidence from the very base of taceous pelagic deposits or the overlying Eocene the graded sandstone beds shows a mixture of marly strata (Nold et al. 1981, p. 134). In its north- basement-derived detrital fragments, namely, ern part, near the Kobat Sidi Kmim slice, a filonian-type quartz, schist, feldspar and micas. coarse-grained chaotic breccia (c. 15-20 m thick, They are probably sourced from a tectonically facies 9) unconformably overlies a Campanian- raised, new source area(s). Regional correlations Maastrichtian Capas Rojas-Capas Blancas pelagic with both the External domain and the Internal series (facies 1 and 3). Dark-coloured marls interca- one support such an assumption (see below). lated between the basal breccia flows contain plank- tonic Foraminifera of late Paleocene age (El Kadiri et al. 2003). The most conspicuous example of Discussion: regional correlations Paleocene gravity-flow events was found in the J. Moussa Group: as noted by E1 Hatimi (1991) Figure 4 summarizes the facies contents of the and E1 Kadiri (1991), its largest elements, of up palaeogeographical domains outlined in Figure 3, 1 km in length (Ras Leona and J. Moussa Blocks), and highlights the recognized discontinuities (ero- are partly embedded within ochre-red and black sional, palaeokarstic and Fe-hardground-type shales of Late Maastrichtian-Paleocene age surfaces) and the main calciturbidite and tectono- (facies 12). All these Paleocene chaotic breccia sedimentary events. It should be noted that the were probably linked to regional tectonic pulses, Tamezzakht succession appears to be the most com- as they form also a widespread key stratum in the plete, with its facies being more clearly contrasted Kabylian domain (e.g. Raoult 1974). In many in the field (El Kadiri et al. 2005). Its position in places throughout the northern Dorsale Calcaire a transitional area between the Internal domain (Haouz Belt), Raoult (1966) noted a Paleocene and the External one makes it a useful starting age for the Microcodium-bearing calcareous sand- point for regional correlations. From the latest Cre- stones (facies 10, Fig. 4), which transgressively taceous onwards the main lines of comparison are overlie the massive carbonate formations. Ben described below (see also Fig. 3). Yaich et al. (1986) and Hlila (2005) described and The latest Maastrichtian-early Paleocene dated in the Oued El Gharraq section an interesting pelagic-dominated strata (black shales and dark-coloured glaucony-rich, bioclastic level (c. reduced ochre-red shales, facies 5 and 6, respect- 30 cm, facies 8), which transgressively erodes late ively, Fig. 4) at the base of the Tamezzakht succes- Cretaceous 'Capas Blancas'-type strata, and lies at sion strongly recall their time-equivalent strata the very base of the white massive Nummulite- known in (1) the Dorsale Calcaire as Capas rich grainstones (facies 14b). Similarly, Microco- Blancas (facies 3, Fig. 4), made up of dark-coloured dium-bearing calciturbidites characterize the late marl-limestone alternations (of Maastrichtian- Paleocene calciturbidites in the Flysch Trough (?)Paleocene pro parte age, Griffon 1966; E1 (facies 13). Kadiri 1991); (2) the Jbel Moussa Group in the Petrographical evidence from the Maastrichtian- facies of ochre-red and black, lime-poor shales of Eocene Tamezzakht calciturbidites (facies 6-11) lower Paleocene age (facies 6b, Ras Leona and and from the Brni Ider Flysch Trough (facies 2, 7 Taoura sections, E1 Kadiri et al. 1990); (3) the and 13), show that the reworked lithoclasts were southernmost External Dorsale ('Col de l'Abri' inherited from Triassic-early Jurassic, massive car- section, Nold et al. 1981; E1 Kadiri 1984) in the bonate formations, mainly dolomites and white facies of variegated to ochre-red lime-poor shales massive limestones, as well as from latest of Maastrichtian-(?)Paleocene pro parte age (facies Jurassic-earliest Cretaceous pelagic series, namely 4). In contrast, the Maastrichtian-Paleocene strata Calpionella- and/or Saccocoma-rich mudstones. in the BEni Ider area are represented by thick packages Complementary results have been obtained from of mixed carbonate-siliciclastic turbidites (facies 7, equivalent late Cretaceous-early Oligocene calcitur- E1 Kadiri et al. 2003), but within which intercalations bidite strata of the Brni Ider area by Blumenthal of ochre-red lime-poor shales are a very common et al. (1958), and recently by E1 Kadiri et al. component. (2003, 2006). Interestingly, such facies make up pre- The thick-bedded late Paleocene dark-coloured cisely the successions known in the Internal Dorsale calciturbidites (facies 11) present a striking lithofa- units (e.g. Griffon 1966; Raoult 1966; Nold et al. cies analogue in the Brni Imrane area located 5 km 1981; E1 Kadiri et al. 1989; Maat6 1996) and NW of Tetuan, which may correspond to a lateral the Jbel Moussa Group (El Kadiri et al. 1990). equivalent of the Tamezzakht succession. In the In contrast, lithoclasts derived from key facies of southern Dorsale Calcaire units Paleocene strata the External Dorsale (red radiolarites, Aptychus- are generally poorly characterized and in most rich mudstones) are lacking despite the fact that the REGIONAL CORRELATIONS, RIF INTERNIDES-EXTERNIDES 205

Fig. 4. Facies correlation and the tectonosedimentary events in the southwesternmost A1KaPeCa palaeomargin, the Tariquide Ridge and the Flysch Trough, based on selected data from: the Talembote area (Ghomaride terranes), Oued E1 Gharraq and Hafat Stir sections (Internal Dorsale), J. Lakraa, Hafat Nator, Saaden and Ametrasse-Bettara units (External Dorsale), Chrafate Klippes (Predorsalian domain), Beliounis and Ras Leona Klippes of the eastern part of the J. Moussa Group (Tariquide Ridge) and the Oued-E1-Kdbir successions (Bdni Ider trough). 1, 'Capas Rojas'-type marlstones; 2, thick-bedded calciturbidites; 3, 'Capas Blancas'-type marlstones; 4, variegated marls (scaglia rossa facies); 5, black shales and resedimented blocks; 6, ochre-red marlstones and slope calcarenites in Tamezzakht (6a) and the eastern J. Moussa Group (6b); 7, calciturbidite-black shale alternation; 8, glaucony-rich bioclastic wackestones of the Oued E1 Gharraq section); 9, chaotic megabreccias and black shales (Kobat Sidi Kmim section); 10, black-shale pelagic limestone alternation (10a) and Microcodium-bearing turbidites and pelagic mudstone (10b); 11, Microcodium-rich, thick-bedded calciturbidites; 12, hectometre-scale olistoliths, i.e. eastern elements of the J. Moussa Group; 13, medium- to thick-bedded Microcodium-rich calciturbidites (late Paleocene); 14a, early Eocene, Nummulite-bearing white sandstones; 14b, Nummulite-rich massive white limestones; 15, latest Eocene-earliest Oligocene coarse-grained conglomerates (the so-called Breccias Nummuliticas); 16, variegated marls; 17, large-scale olistoliths embedded within the latest Eocene-early Oligocene variegated marls (i.e. Chrafate Klippes, Assifane blocks, etc.); 18a, 18b, coarse-grained c alciturbidites and olistoliths; 19, ochre-red lime-poor shales (RSF); 20, yellow soft marls with thin intercalations of sandstones (Bartonian); 21a, micaceous, wood-debris-bearing, carbonate sandstones, i.e. the so-called 'Grbs Roux' (late Oligocene-(?)early Aquitanian); 21b, 'Grbs Roux'-micaceous sandstones alternation and yellow soft pelagic marls (mid- to late Oligocene); 22, green and yellow pelagic marls underlying the Beliounis sandstones; 23, thin-bedded micaceous sandstones and yellow marls; 24, holoquartzose puddingstones, with scarce granite pebbles (basal conglomerate of the Alozaina-type formation): latest Oligocene- early Aquitanian; 25a, yellow sandstone-marl alternation; 25b, yellow soft pelagic marls (late Aquitanian pro paste); 26, fine-grained yellow sandstones (Aquitanian); 27, channelized Beliounis-type sandstones (late Oligocene- Aquitanian); 28, Aquitanian Beliounis sandstones (cropping out in the village of Beliounis); 29, thick-bedded micaceous sandstones; 30, chaotic basal breccias and olistoliths containing a mixture of carbonate clasts as well as granite and basalt pebbles; 31, early Burdigalian Vifiuela-type marlstones with thin chert levels, cropping out in the Talembote area (31 a) and in the Predorsalian Chrafate Klippe zone (3 lb); 32, 'Gr~s Roux'-micaceous sandstones alternation and Vifiuela-type marlstones (early Burdigalian); 33, tobacco brown pelites and Numidian-type sandstones (early to mid-Burdigalian) with resedimented blocks inherited from lost Ghomaride terranes; 34, chaotic complex reworking a mixture of blocks inherited from the Internal Dorsale and the Ghomaride cover; 35, chaotic complex reworking blocks from both the Internal and the External Dorsale; 36, nappe emplacement, probably triggered from late Burdigalian time. 206 KH. EL KADIRI ET AL. latter domain was palaeogeographically placed differs from the initial Predorsalian scheme of between the Internal Dorsale and the Tamezzakht Didon et al. (1973) and Olivier (1984) who recon- area. Thus, calciturbidites of the Tamezzakht succes- structed the Predorsalian as a narrow transitory sion (and those of the B~ni Ider succession) are likely palaeogeographical zone directly connected to the to have been derived from an external shallow-water external Flysch Trough. The scheme proposed high area and not from the neighbouring Dorsale here may explain why the Predorsalian zone did Calcaire. Support is given to this assumption by not receive the widespread early Cretaceous sand- the following three criteria. (1) Both the Internal stone flysch (i.e. Tisirene flysch). Interestingly, Dorsale and the external Dorsale during this time the fact that the Predorsalian series received interca- interval were completely drowned, as is clearly lations of Numidian-like sandstone flysch during shown by the three ubiquitous pelagic facies: latest Oligocene-Aquitanian times may indicate 'Capas Rojas' (Campanian), 'Capas Blancas' that an important tectonic event occurred during (Maastrichtian) and black shales (mainly of late the mid- to late Oligocene and resulted in the disap- Paleocene age). In contrast, the petrographical evi- pearance of the so-called 'Tariquide Ridge'. We dence shows the abundance of rust-coloured, shall see below that this turning event: (1) was palaeo-altered clasts in the B6ni Ider and Tamez- immediately preceded by large-scale resedimentation zakht Paleocene calciturbidites, which indicates phenomena (latest Eocene-early Oligocene), partly that this clastic material was reworked from an adja- reworking the material of the above-mentioned cent emerged area. (2) The east-moving slump struc- ridge itself; (2) was coeval with the onset of the wide- tures in the late Cretaceous-Paleocene calcarenites spread micaceous sandstone flysch (i.e. B6ni Ider point to east-dipping (towards the internal zone) flysch), which indicates a tectonically raised new palaeoslopes. (3) The palaeocurrent directions indi- clastic source. cate currents flowing towards the internal domain At present, late Cretaceous-Paleocene marine and directed N70~176 mainly N80~ strata are unknown in the Ghomaride domain In contrast to the late Paleocene black shales and (Maat6 1984, 1996; E1 Kadiri 1991). In almost all Microcodium-bearing pelagic black mudstones of the patched outcrops of the carbonate cover, dis- the Dorsale Calcaire (facies 9 and 10a) the coeval covered in this domain, white Nummulite-bearing thick-bedded black calciturbidites of the carbonate sandstones (WNS, Fig. 3) of earliest Predorsalian (facies 10b), Tamezzakht (facies 11) Eocene (Illerdian) age (facies 14a, Fig. 4) directly and B~ni Ider series (facies 13) are almost exclu- fill the karstic cavities developed in the Liassic car- sively made up of Microcodium crystal grains. bonate successions (e.g. E10nzar unit, E1 Kadiri The Microcodium colonies (originally defined by et al. 1992). It is noteworthy that all the early Gltick 1912) are known to correspond to microbial Eocene transgressive shallow-water limestones at mats 'decaying' limestones on palaeosoils (Freytet present known in the Ghomaride domain are 1970; Bodergat 1974) and palaeokarst surfaces never found directly discordant on the Palaeozoic (Meyer 1987; E1 Kadiri et al. 1992). Thus, the latter schists. The fact that they are fundamentally Microcodium-rich calciturbidites were sourced from linked to early Jurassic strata (e.g. E10nzar and large-scale emerged karstic areas, which cannot be Talembote sections, Fig. 3) and frequently occur envisaged in the Dorsale Calcaire, as the latter was as olistolithes within the Alozaina- and Vifiuela- totally drowned during Campanian-Paleocene type Tertiary formations (e.g. Talembote section, times (El Kadiri et al. 1989, 1992). It is noteworthy Fig. 3), strongly suggests that these fragments of that the basinward export of the greatest volume of the assumed early Eocene 'Ghomaride cover' Microcodium material was mostly triggered during were originally derived from Ghomaride-like lost the late Paleocene transgressive regime (compare terranes and not from the at present defined Gho- the. 'transgressive washing' process described by E1 maride units. A similar conclusion may be inferred Kadiri et al. 2006). from the basal conglomerates of these two Tertiary These important results are in accordance with formations (El Kadiri et al. 2001; Hlila 2005) and the 'Tariquide Ridge' hypothesis of Durand-Delga from coeval conglomerates overtopping the Ter- (1972), which postulates that an isolated pelagic tiary Ametrasse unit (southern external Dorsale, platform should be reconstructed in the northern- Nold et al. 1981; Hlila 2005), which are, in both most part of the External zones (i.e. Jbel Moussa cases, rich in granite, basalt pebbles and reefal Group). The above-mentioned petrographical data blocks of unknown origin. The fact that these strongly suggest that the 'Tariquide Ridge' would conglomerates preferentially occur close to the have had an important southward prolongation in Ghomaride-Dorsale contact (e.g. Talembote, B6ni the external zones and therefore would have separ- Maaden) and within the Dorsale Calcaire itself, ated the Predorsalian zone from the Mauretanian strongly suggests that their source was located Flysch Trough during Jurassic-early Oligocene between the Ghomaride terranes and the Dorsale times. Thus, the Predorsalian zone significantly Calcaire. REGIONAL CORRELATIONS, RIF INTERNIDES-EXTERNIDES 207

Regarding the successive transgressive peaks 1979). In the second, chaotic breccias cap the shown in the long- and short-term eustatic curves Eocene calciturbidites before being buried under an by Haq et al. (1987) and Hardenbol et al. (1998, ochre-red shale-dominated succession (facies 18b). charts 1 and 2), the late Cretaceous-Paleocene In addition, E1 Kadiri (1984), De Wever et al. transgressive peaks were markedly higher than (1985) and Ben Ya'/ch et al. (1988) showed that the those of Eocene times. This leads us to suggest sedimentary Chrafate Klippes (facies 17), which rep- that: (1) the Ghomaride realm (sensu lato) experi- resent the southernmost part of the Predorsalian enced a long-term Mesozoic karstic regime (El domain, were embedded within variegated marls Kadiri et al. 1992); (2) the onset of the Tertiary of latest Eocene-early Oligocene age (facies 16). marine regime from the beginning of the Eocene Concurrently, the absence of coeval marine strata in was driven by a regional-scale tectonic collapse. the Ghomaride domain is noteworthy. Marine sedi- Interestingly, equivalent transgressive Nummulite- mentation seems not have returned before the onset bearing sandstones that developed in a strikingly of the widespread latest Oligocene transgressive holo- identical lithofacies make up a metre-scale interval quartzose puddingstones (facies 24), which lie at the at the base of the Eocene calciturbidites in many base of the Aquitanian yellow marl-sandstone alter- sections throughout the Btni Ider area (Fig. 3). nation (facies 25, i.e. Ciudad-Granada-Fnideq They can serve as key strata not only because of Formation). their high correlation potential, but also as they In the northernmost part of the Ghomaride domain, allow the onset of a transgressive regime to be deli- the Fnideq sandstones commonly seal normal faults at neated even within near-homogenous base-of-slope different scales, which points to a regional extensional calciturbidite packages. In the Oued-E1-Ktbir event. In the Dorsale-Predorsalian couplet, the rust- section (Fig. 3) a conspicuous Thallassinoides- coloured sandstones (facies 21a) that start shortly burrowed firmground surface (i.e. Glossifungites- before, during the late Oligocene, also seal normal type surface; e.g. Savrda 1995; MacEachern & faults at different scales. A more comprehensive Burton 2000; Savrda et al. 2001a,b) immediately assessment of the regional-scale tectonic controls follows the WNS facies, and probably marks the that might be proposed for the whole late Oligocene related transgressive peak. history needs to account for other time-equivalent Importantly, the same light-coloured carbonate events known throughout the whole Betic-Rif sandstones exist in the Tamezzakht section. They Internal zones, which is beyond the scope of this clearly erode the lime-free siliceous green shales paper. It should be noted, for instance, that this exten- of the underlying facies (facies 11), upon which sional event in both the Ghomarides and Dorsale Cal- they unconformably rest along a low-angle hidden caire occurred just after the mid- to late Oligocene discontinuity (in the sense of Clari et al. 1995). paroxysmal phase that is well documented in the Two Fe-encrusted surfaces cap the immediately Ghomaride units (e.g. Chalouan 1986; Durand- overlying beds and may be regarded, in the same Delga et al. 1993). way, as corresponding to the consequent transgres- The abrupt facies change that is well delineated sive peak. Hence, the following thin-calciturbidite- in the field between the 'oligotrophic' ochre-red intercalated ochre-red shales could normally shales (facies 19 in the Tamezzakht, J. Moussa correspond to the late highstand-lowstand regime, and Bgni Ider areas) and the 'eutrophic' green during which terrigenous-nmd-dominated packages pelagic marls (oligotrophy-eutrophy boundary, are the most common components (e.g. Savrda Ol/Eu B, Fig. 4) is seemingly linked to the well- et al. 2001a). documented global-scale climatic change that Within the Tamezzakht succession, conspicuous occurred close to the Eocene-Oligocene boundary. grain-flow events occur in the upper part of the It is evidenced by the turnover of planktonic Fora- ochre-red shales of Eocene-early Oligocene age minifera (see examples by Molina et al. 1986, (facies 18a), probably close to the Eocene- 1988, 1996, amongst others) as a result of a Oligocene boundary. They laterally evolve into a dis- sudden global cooling event paired with enhanced continuous olistostrome-like formation, which can ocean circulation (e.g. Pomerol 1985; Marry et al. rest uncomfortably on the underlying strata of late 1988; Zachos et al. 1993, 1995; Diester-Haass & Cretaceous-Paleocene age (facies 5 and 6). This col- Zahn 1996; Barnes 1999). These climatic events lapse event may correlate with the regional-scale were essentially induced by the immediately pre- onset of chaotic breccias in both the Dorsale Calcaire ceding tectonic collapses, which resulted in the (facies 15, Breccias Nummuliticas, Nold et al. 1981) opening and/or rearrangement of intercontinental and the Flysch Trough. In the former (e.g. Hafat seaways (e.g. between Antarctica and South Stir section, Fig. 3) they unconformably rest on the America, Pomerol 1985; Wilson et al. 1998). Triassic-Liassic massive carbonate formations Thus, the successions selected in this study and seal large-scale extensional structures (see also provide an interesting record of such a twofold the geological maps of Kornprobst et al. 1975, tectonic and climatic event: the coarse-grained 208 KH. EL KADIRI ETAL. conglomerates (facies 15, 17 and 18)and olistos- careful regional-scale correlations (partly involving tromes (facies 17) fit well with this, scenario. sedimentological and environmental data as a com- We would like to compare this Oligocene scen- parison tool) throughout both the Internal and ario with two strikingly near-identical events, External zones. For instance, it is noteworthy that: which occurred close to the Jurassic-Cretaceous (1) a tectonic event (i.e. the mid- to late Oligocene boundary and at the Turonian-~-early Senonian paroxysmal phase in the Ghomaride domain) could boundary, respectively. The former was recorded be responsible for the emplacement (and/or emer- similarly by an abrupt facies change between the gence) of new supplying terranes close to or 'oligotrophic' ochre-red radiolafitic shales (late partly on the previous nummulitic carbonate Jurassic) and the coccolith-formed yellow hemi- source, which resulted in its complete and irrevers- pelagic marls (late Tithonian-e~/rly, Cretaceous). ible drowning under the siliciclastic accumulations; This is the Kuenen event (Roth 1989), which is (2) the whole palaeogeographical setting was likely known throughout the Tethyan realm to be similarly to undergo significant modifications (i.e. in placing induced by a tectonic-mediated ocean-circulation together previously distant areas). Concurrently intensification (De Wever et al. 1986; E1 Kadiri with the rust-coloured sandstones, this result may 2002b). In the latter case the early Senonian additionally be supported by the interlayered eutrophic green pelites sharply seal normal faults metre-scale micaceous sandstones, which undoubt- affecting the immediately underlying ochre-red edly reflect the rise of another juxtaposed terrige- Turonian shales and calciturbidites (El Kadiri nous source. et al. 2003). These examples support the causal In the Ghomaride domain, the chaotic, coarse- link proposed above between tectonics and abrupt grained conglomerate lying at the very base of the facies change. In the case of the onset of the early early Burdigalian marlstones (i.e. Vifiuela For- to mid-Oligocene eutrophic shales (Dorsale mation) is well documented in the Betic Internal calcaire; Tamezzakht, B6ni Ider), the related zones as transgressively onlapping the Palaeozoic tectonic event may obviously be linked to the terranes (Sanz de Galdeano et al. 1993; Serrano Ghomaride paroxysmal phase. et al. 1995; L6pez-Garrido & Sanz de Galdeano The rust-coloured sandstones (the so-called 'Gr~s 1999). These rocks erode the Aquitanian yellow Roux'; Fallot 1937; Griffon 1966) typify the late pelagic marls of the underlying formation (Alozaina Oligocene siliclastic regime in all the stratigraphic Formation) and could indicate a tectonically con- series known in the Dorsale Calcaire (facies 21a) trolled collapse. This large-scale event resulted in and last until the early Burdigalian in the Tamez- the generalization of the siliceous marlstones of zakht succession (facies 21b and 32). Petrographi- hemipelagic signature throughout the Betic-Rif cal evidence shows that this regime reworks a Internal zones. The fact that this facies of high cor- mixture of metamorphic-rock-derived, immature relation potential makes up decametre-thick inter- lithoclasts that do not seem to be sourced from the vals in the upper third of the Tamezzakht Rifian Sebtide-Ghomaride terranes or from their succession (facies 32) and the Predorsalian units Betic counterparts. Their petrographical features (facies 31b) leads us to the conclusion that the seem to us similar to those described by Puglisi palaeogeographical setting of the latter external et al. (2001) in both the Tertiary Ghomaride cover units became relatively close to the structuring of and the time-equivalent strata in the B4ni Ider the Internal zones during the late Aquitanian- flysch successions. About 10 palaeocurrent direc- early Burdigalian. tions measured on the sole of the sandstone beds With regard to the pelagic sedimentation regime, it indicate currents directed N20~ ~ mainly seems possible that there are three lines of comparison N30~ ~ and flowing from the SW to the NE between the Tamezzakht succession and that of the (i.e. towards the internal domain from an external Talembote area recently described by E1 Kadiri source). Thus, like the underlying calciturbidites, et al. (2001) close to the Internide-Externide front these sandstone flows could be sourced from (an) (Fig. 3). (1) In the Tamezzakht area, the entire mid- external lost terrane(s). Seemingly, the same may Oligocene-early Burdigalian pelagic marly depo- be true for the Dorsale-Calcaire 'Gr6s Roux', the sition develops in a rhythmic alternation of centimetre sole of which gives evidence of north-flowing cur- to decimetre intervals of yellow marls and 'early' rents (our measurements were taken in the Tamez- Vifiuela-type green marlstones, with the latter cyclic zakht area, i.e. in the Hafat Stir section along the component being dominant in early Burdigalian road to the television mast). In the latter domain time. In the Talembote area, these two facies are the current directions were probably modified by a clearly separated in time as two contrasted lithologi- near north-south-directed half-graben physiogra- cal intervals, with an erosional discontinuity phy. However, reconstruction of the late Oligo- between them close to the Aquitanian-Burdigalian cene-Aquitanian sandstone source(s) remains a transition (see Fig. 3). Thus, the difference between hard task and requires more dating controls and the Tamezzakht pelagic deposition (i.e. close to the REGIONAL CORRELATIONS, RIF INTERNIDES-EXTERNIDES 209

External Domain) and the Talembote one (Internal regional or global scale. The above interpretation Domain) may basically be related to the diachronism provides the three following results. of the Vifiuela-type marlstones. (2) Lithofacies and biostratigraphic dating allow us to distinguish in the (1) Apart from certain widespread facies of high Predorsalian domain two types of early Miocene correlation potential, the late Cretaceous-early holoquartzose sandstones: the first corresponds to Oligocene strata studied above exhibit important the classical Numidian-like, yellow to rust-coloured differences, so that their respective depocentres sandstones (facies 27 and 28, Fig. 4) defined by should be located in distant palaeogeographical areas. We can retain the possibility that: (a) important Durand-Delga (1972) and Didon et al. (1973) in the village of Beliounis (J. Moussa Group) as charac- Ghomaride-like lost terranes could be located terizing the depositional regime of the Predorsalian between the present-day defined Ghomaride units zone during the late Oligocene-Aquitanian, (i.e. and the Internal Dorsale; (b) symmetrically, one or synchronously with the external Numidian flysch several isolated carbonate platforms could be deposition). This facies, sometimes poorly consoli- located within the external zones, i.e. 'Tariquide'- dated, is generally poorly graded and all the quartz like ridge(s), which have played a major role as the grains are rounded and may be white, red or black. source delivering, at a large scale, calciturbidites to Very similar yellow sandstones coevally spread the Predorsalian and Flysch basins. over the Ghomaride-Malaguide domains (Fnideq (2) The relationship between the internal and the and Alozaina Formations, respectively, facies 25a, external zone, which has long been considered as Fig. 4). We have found identical facies within the being marked by a narrow transitional zone (the late Oligocene-Aquitanian levels of the Tamezzakht classical Predorsale concept), was likely to have succession, a result that lends additional support to involved more than a simple palaeogeographical ascribing the Tamezzakht area to the Predorsalian area, as shown by the Chrafate klippes and the zone. The second type of sandstone facies corre- J. Moussa Group, which are remains of a wider sponds to tobacco brown holoquartzose sandstones, and more complex area. The latter probably under- in which the quartz grains may be rounded or went successive palaeogeographical modifications not and are predominantly glass-green coloured. Indi- with time. For instance, it should be noted that vidual beds may show graded bedding into during late Cretaceous-Eocene times, the Predor- fine pelites. This second sandstone facies strictly salian zone(s) were separated from the Flysch occurs within the tobacco brown pelites of early to Trough by the above-mentioned 'Tariquide'-like mid-Burdigalianage (El Hatimi 1982; E1 Kadiri ridge(s). The collapse and final disappearance of the latter occurred during the latest Eocene-early et al. 2001; Hlila 2005) and its distinction fits well with the early 'Neonumidian'-sandstone concept Oligocene, i.e. concurrently with (a) the disappear- defined by Bourgois (1978) in the Internal zones of ance of the external prolongation of the external the Betic Cordilleras. Dorsale units (i.e. Chrafate Klippe olistostromes), The upper levels of early Burdigalian tobacco (b) the onset of the Dorsale calcaire megabreccias brown pelites receive increasing gravity-flow dis- (Breccias Nummuliticas) and (c) other large-scale charges that evolve into huge olistostrome com- gravity events (e.g. Talembote olistostromes). plexes carrying large olistoliths. These derived (3) The major discontinuities, coarse-grained dis- from either the Ghomaride-Internal Dorsale charges and facies changes (e.g. newly raised sources) couplet (facies 34, example in the Talembote may be ascribed to distal reverberations of the con- area) or the External Dorsale (facies 35; for the tractional phases that occurred in the old Ghomaride examples occur in Tamezzakht, Chrafate Klippes realm during the early to mid-Oligocene-early and Kobat E1 Kesskasse olistostrome) with Palaeo- Burdigalian time interval. The progressive homogen- gene variegated marly strata being trapped ization of some key facies (rust-coloured sandstones, between them. The immediately superimposed Beliounis and Neo-Numidian ones as well as the Dorsale nappe pile may tentatively be considered Vifiuela-type marlstones) to previously distant as resulting from the culmination of the same palaeogeographical zones during Aquitanian-early phenomenon. B urdigalian times may be paralleled by the shortening processes that resulted in a new palaeogeographical setting.

Conclusion However, reconstructing a reliable tectonosedi- mentary evolution requires new insights into the The aim of this paper was to provide a basis for following issues. synthesizing the more significant facies, discontinu- ities and gravity-flow discharges from the Rif (1) What was the triggering mechanism(s) of the Internal Domain and its surroundings. It seems chaotic, coarse-grained gravity flows? Despite these that almost all the data point to tectonic events of commonly occuring as deposits that transgressively 210 KH. EL KADIRI ETAL. overlie previous emerged areas, their intercalation AZANON, J. M., GARCIA-DUENAS, V. & GOFFg, within and/or at the top of pelagic marly succes- B. 1998. Exhumation of high-pressure metapelites sions leads us to raise the question of contractional and coeval crustal extension in the Alpujarride (nappe front) versus extensional (normal fault) tec- complex (Betic Cordillera). Tectonophysics, 285, 231-252. tonic controls. A eustatic signature cannot be BALANYA, J. C. ~% GARCIA-DUENAS, V. 1987. Les excluded, as megabreccias are generally ascribed directions structurales darts le domaine d'Alboran to lowstand phases (e.g. Haas 1999; Ineson & de part et d'autre du D~troit de Gibraltar. Surlyk 2000). Comptes Rendus de l'AcadEmie des Sciences, (2) What is the significance of the four Sdrie II, 304(15), 929-932. Palaeogene-early Miocene formations (with discon- BARNES, C. R. 1999. Palaeoceanography and palaeo- tinuities between them), well documented in the climatology: an Earth system perspective. Chemi- Malaguide-Ghomaride domain, in terms of eustatic cal Geology, 161, 17-35. controls (i.e. Exxon sequence) versus a tectonic one? BEN YA~CH, A. 1991. Evolution tectono-sEdimentaire (3) What is the extent of the entirely disappeared du Rif externe centre occidental (rEgions de M'Sila et Ouezzane, Maroc). Doctorat d'Etat palaeogeographical zones? Indeed, the clastic Thesis, University of Pau, France. mixture reworked in the Alozaina and Vifiuela for- BEN YAICH, A., MAATt~, A., FEINBERG, H., MAGNI2, mations (Betic Cordillera) and in their Rif counter- J. & DURAND-DELGA, M. 1986. Implications de parts, points to very extensive lost source areas. niveaux du Miocene inf6rieur dans les retro- This leads us to question how far we can still maintain chevauchements de la Dorsale calcaire rifaine the classical scheme that immediately juxtaposes (Maroc): signification ~ l'~chelle de l'Arc de the Sebtides, Ghomarides, Dorsale, Predorsale and Gibraltar. Comptes Rendus de l'AcadEmie des Mauretanian flysch? Sciences, SErie 11, 302(8), 587-592. (4) Was the kinematics of nappe emplacement BEN YA~CH, A., DUI~E, G., EL HATIMI, N. & EL KADIRI, KH. 1988. La formation it klippes sEdi- determined by tectonic driving forces (subduction mentaires d'fge oligo-burdigalien du Rif septen- et al. phases, Lonergan & White 1997; Chalouan trional (Maroc): signification gEodynamique. 2001) or by gravitational ones (Weijermars 1987; Notes et M6moires du Service G6ologique du Doblas & Oyarzun 1989; El Kadiri et al. 1995)? Maroc, 334, 99-126. A possible continuum process and/or causal link BENZAGGAGtt, M. 1996. Le Maim supErieur et le Ber- between them may tentatively be suggested in the riasien dans le PrErif interne et le MEsorif (Rif case of the large-scale gravity flows proved to Maroc): stratigraphie, sEdimentologie, palEogEo- immediately precede the nappe-pile emplacement. graphie et Evolution tectono-sddimentaire. Doc- torat d'Etat Thesis, University of Rabat. Integrated approaches involving sedimentology, BLUMENTHAL, M., DURAND DELGA, M. & FALLOT, sequence-stratigraphic interpretation, comprehen- P. 1958. DonnEes nouvelles sur le Tithonique, le sive inventory of sedimentary discontinuities, CrEtacd et I'Eocbne de la zone marno-schisteuse close biostratigraphic dating and detailed du Rif septentrional (Maroc). Notes et M6moires mapping, as well as more extended regional corre- du Service Gdologique du Maroc, 16(143), 35-58. lations, are expected to shed additional light on BODERGAT, A. M. 1974. Les Microcodium, milieux et modes de ddveloppement. Docmnents du Labora- these issues, and are in progress. toire de G4ologie de la Facult4 des Sciences de Lyon, 62, 137-235. The authors express their sincere thanks to A. Michard BOU[LLIN, J. P., DURAND-DELGA, M., GI~LARD, J. P., (University of Paris) and W. Wildi (University of Zfirich) ET aL. 1970. D~finition d'un flysch Massylien et for their thorough reviews and constructive remarks. This d'un flysch Maur~tanien au sein des flyschs alloch- work was financially supported by both the Soci6t6 tones de I' Alg~rie. 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