Journal of African Earth Sciences 100 (2014) 554–568

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Journal of African Earth Sciences

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Sedimentary evolution of the siliciclastic Aptian–Albian Massylian flyschof the Chouamat Nappe (central Rif, Morocco)

http://dx.doi.org/10.1016/j.jafrearsci.2014.08.0041464-343X/� 2014 Elsevier Ltd. All rights reserved.

⇑ Corresponding author.E-mail address: francesco.perri@unical.it (F. Perri).

Hajar El Talibi a, Mohamed Najib Zaghloul a, Francesco Perri b,⇑, Khadija Aboumaria a, Abdelhamid Rossi a,Said El Moussaoui a

a Department of Earth Sciences Faculty of Sciences and Techniques, University Abdelmalek Essaadi, Postal Box 416, 90000 Tangier, Moroccob Dipartimento di Biologia, Ecologia e Scienze della Terra, Università della Calabria, 87036 Arcavacata di Rende (CS), Italy

a r t i c l e i n f o

Article history:Received 19 May 2014Received in revised form 9 August 2014Accepted 11 August 2014Available online 23 August 2014

Keywords:PetrographyGeochemistryProvenanceWeatheringChouamat nappeMassylian

a b s t r a c t

Sandstone petrography and geochemistry (major, trace and rare earth elements) of the Aptian–Albiansiliciclastic Massylian flysch from the Chouamat Nappe (central Rif Morocco) are used to highlight thechemical weathering conditions in the source area and to infer their provenance. Petrographic studiesshow that the studied samples are mostly quartzarenite, sublitharenite and subarkose generally com-posed of quartz (up to 99%), K-feldspar (less than 5%) and scarce fragments of sedimentary rocks. Thesamples plot in the continental block provenance field of the QtFLt diagram. Thus, the compositionalmaturity of analyzed sandstones is typical of cratonic environments. The sandstone samples shows highSiO2 content (up to 96%) and strong depletion in mobile components such as Na2O, CaO as well as in fer-romagnesian minerals, which are mainly related to intense chemical weathering processes in the sourcearea, as confirmed by high Chemical Index of Alteration values (mean = 79.8). Recycling is shown by theTh/Sc vs. Zr/Sc plot, where the studied sandstones fall along a trend involving zircon addition and thussediment recycling. Several geochemical ratios, such as La/Sc, Th/Sc, Th/Co and Th/Cr, of the studied sam-ples are similar to those of Post-Archean Australian Shales and of the Upper Continental Crust, andsuggest a provenance from source area(s) mainly composed of plutonic and felsic metasedimentaryand sedimentary rocks, which were most probably the basement rocks of the adjacent African plate.These source rocks are related to a large cratonic source region of Eburnean and Pan-African belts, Pre-cambrian (?) and/or Variscan basements of the southeastern margin of the African plate.

� 2014 Elsevier Ltd. All rights reserved.

1. Introduction

The petrography and the geochemistry of siliciclastic sedimentscan reveal the nature of their source regions and the tectonic set-ting of the sedimentary basins where they formed. Several modelsare used to infer provenance parameters (source rock lithology, cli-mate, weathering, transport, and geodynamic setting) from petro-graphic studies on sandstones (Dickinson, 1985; Critelli et al.,2003). Moreover, during the last two decades, geochemical proxiesfor provenance investigation have been significantly developed(Nesbitt and Young, 1996; McLennan, 2001; Roser et al., 2002;Mongelli et al., 2006; Caracciolo et al., 2011; Perri et al., 2008a,2008b, 2011a, 2011b, 2012a, 2012b, 2014). However, some geo-chemical ratios can be altered during weathering and/or diagenesis(Nesbitt and Young, 1989). As long as the bulk composition of arock is not altered, major oxides and trace elements (Nd, Ni, V,

Cr, Yb, La, Th, Sc and Zr) are valuable tools in the study ofmatrix-rich sandstones (Bhatia and Crook, 1986; McLennan et al.,1993) and constitute reliable established provenance and tectonicsetting indicators (Armstrong-Altrin, 2009).

An important feature for palaeogeographical and palaeotectonicreconstructions of the western Mediterranean Alpine belts (Fig. 1)is represented by the Maghrebian Flysch Basin, which is a majorMeso-Cenozoic Domain of the Maghrebian Chains (Durand-Delga,1980; Durand-Delga and Fontboté, 1980; Wildi, 1983; Bouillinet al., 1986). The Mauretanian and Massylian sub-Domains arecharacterized by successions reflecting similar lithological charac-ters and tectonic evolution of their source areas. The clastic supplyof the Mauretanian deposits derived from the erosion of the Mes-omediteranian Terrain sensu Guerrera et al. (1993, 2005), composedof pre-Alpine basements and their Meso-Cenozoic sedimentarycovers locally affected by Alpine metamorphism, whereas the Mas-sylian deposits were fed by the African Craton and it northernpassive margin (Durand-Delga and Fontboté, 1980; Hoyez, 1989).The differences between Mauretanian and Massylian deposits

Fig. 1. Geological sketch map of the alpine chains in the central-western mediterranean region (modified from Perrone et al., 2006; Critelli et al., 2008; Guerrera et al., 2012).

H. El Talibi et al. / Journal of African Earth Sciences 100 (2014) 554–568 555

become particularly evident since the Early Miocene when a thicksedimentation of immature sandstones occurred in the Maureta-nian sub-Domain (Guerrera et al., 1986), while the highly maturequartzarenitic Numidian and like-Numidian successions weredeposited in the Massylian sub-domain (Bouillin et al., 1970;Durand-Delga, 1980; Guerrera et al., 1992; Besson, 1984,Andrieux (1971)).

The studied sandstone suites belong to the Massylian sub-Domain of the Maghrebian Flysch Basin, are located in Jbel Choua-mat area in the central Rif (Figs. 1 and 2). The Chouamat Nappe wasdefined by Andrieux and Mattauer (1963). The age and lithofaciesof the studied Aptian–Albian siliciclastic successions of the Choua-mat Nappe were firstly established by Andrieux (1971) and Gübeli(1982). Previous studies on the Aptian–Albian siliciclastic succes-sions have focused mainly on the sedimentary paleoenvironmentreconstruction and on paleogeographical and structural analyses(Andrieux, 1971; Besson, 1984; Frizon de Lamotte, 1985;Mourabit, 1990). However, there are no studies concerning modalanalysis and geochemical constraints on source area provenance ofthe Chouamat siliciclastic sandstone suites at the scale of the Rifianand Tellian belts. Hence, this paper is aimed to provide new anddetailed data on their petrography and geochemistry (major, trace,and rare earth elements) in order to constraint their provenance,source-area weathering and the related tectonic setting.

2. Geological setting

The Rif chain constitutes the western segment of the AlpineMaghrebide belt (Durand-Delga and Fontboté, 1980), which con-nects with the Betic Cordilleras through the Gibraltar Arc (Fig. 1).The Rif belt (Fig. 2) includes three major paleogeographic Domains,(i) the Internal Domain, or the so-called ‘‘Alboran Domain’’ (Garcia-Duenas et al., 1992); (ii) the Maghrebian Flysch Domain; and (iii)the External Domain.

The Rif Internal Zones include two groups of Nappes showing ametamorphic core complex-like geometry (Garcia-Duenas et al.,1992; Michard et al., 2006). The upper plate corresponds to theGhomaride–Malaguide Nappes, which mainly consist of Palaeozoicrocks affected by low-grade Variscan metamorphism (Chalouanand Michard, 1990). The lower plate corresponds to the Sebtide–Alpujarride units, affected by Alpine low- to high-grade, mediumto high-pressure metamorphism (Bouybaouene et al., 1995;Michard et al., 2006). The Internal Zones include also the DorsaleCalcaire complex (Fallot, 1937; Mattauer, 1960; Wildi et al.,1977; Lallam et al., 1997; El Kadiri et al., 1992; El Kadiri andFauzi, 1996; Hlila, 2005; Chalouan et al., 2008; Zaghloul et al.,2005), which originates from the Mesozoic–Cenozoic sedimentarysuccessions of the southern paleomargin of the Mesomediteraneanmicroplate, located at north of the Ligurian–Maghrebian basin

(Guerrera et al., 2005; El Hatimi et al., 1991; El Kadiri et al.,1992). The latter overthrust the Predorsalian Unit mainly madeof silisiclastic successions and some carbonatoclastic conglomer-ates, macro-breccias and olistoliths related to slope to basin sedi-mentary environments and indicating a proximal paleogeographic location in the Maghrebian Flysch Basin close to thefrontal Dorsale Calcaire Domain (Olivier, 1984; Guerrera et al.,1993).

The External Zones, derived from the north African paleomargin,consist of Mesozoic–Cenozoic successions mainly made of pelagicsediments and of siliciclastic turbidites, which were deposited ontothinned and partially oceanized continental crust of the Africanmargin or (Benzaggagh et al., 2013) and which were stacked duringthe late Serravallian-late Tortonian to form cover nappes (de Capoaet al., 2004; Di Staso et al., 2010). In the Rif belt, the External Zonesare divided, from NE to SW and from top to bottom, into Intrarif,Mesorif and Prerif Zones (Suter, 1980a and Suter, 1980b). The Intra-rif Zone includes the Ketama Unit (Triassic to Albo-Cenomanian),the Tanger Unit, partly detached from the Ketama Unit, and theHabt and Aknoul Nappes (Late Cretaceous–Cenozoic), completelydetached from the Ketama Unit. The Mesorif Zone shows allochth-onous units including Palaeozoic–Paleogene successions whichthrust over tectonic windows whose series end with Middle Mio-cene turbidites. The Prerif Zone consists of Jurassic–Miocene unitsdetached on the underlying Triassic evaporites and thrust overthe Upper Miocene foredeep (Gharb Basin, Saiss).

The Maghrebian Flysch nappes are formed by remnants of thesedimentary infill of the Maghrebian Flysch ocean Basin, associatedwith scarce ophiolitic slivers (Durand-Delga et al., 2000). Thesenappes root beneath the Internal Zones and overlie the ExternalZones, except for some back-thrust units in western Betics, north-ern Rif and Kabylias. Thus, the highly dilacerated contact at thebottom of the Alboran Domain represents the main suture zoneof the Maghrebide orogen.

The Maghrebian Flysch Nappes are mainly made of pelagic fine-grained sediments and of carbonatoclastic and siliciclastic turbi-dites spanning from the Middle Jurassic up to the Late Burdigalian(Durand-Delga, 1980; Suter, 1980; Wildi, 1983; de Capoa et al.,2007, 2013; Zaghloul et al., 2007). The sedimentary successionsof these Flysch Nappes were deposited in a very deep marine basinknown as Maghrebian Flysch Basin (MFB). These terrains extendover more than 2000 km (Fig. 1) from the western Betic Cordillerathrough the Rif Chain to the eastern Sicilian Maghrebides and upsouthern and northern Appenines (Guerrera et al., 2005; deCapoa et al., 2013; Perrone et al., 2014) (Fig. 1).

The MFB has been considered as a southern branch of thewestern Tethys, separated by means of a Mesomediterraneanmicroplate from the Nevado–Filabride–Piedmont northern branch(Bonardi et al., 2001, 2003; Chalouan et al., 2001; Chalouan and

Fig. 2. Geological sketch maps of the Rif Chain and of the Jbel Chouamat, showing a detailed location of the sampling areas.

556 H. El Talibi et al. / Journal of African Earth Sciences 100 (2014) 554–568

Michard, 2004; de Capoa et al., 2003, 2013; Guerrera et al., 1993,2005, 2012; Belayouni et al., 2010, 2012, 2013; Alcalá et al.,2013). Other authors, however, interpreted this basin as a singleextension toward the west of the Piedmont–Ligurian Oceanic belt(Dercourt et al., 1985; Bouillin et al., 1986) through related ter-rains in southern Apenines, which have been interpreted asdeposited in an oceanic belt (Lucanian Ocean) representing, inany case, the northeastward extension of the MFB (Bonardiet al., 2001; de Capoa et al., 2003; Guerrera et al., 2005;Perrone et al., 2014).

The MFB is a main palinspastic domain involved in the buildingof the Maghrebian Chain (Durand-Delga, 1980; Wildi, 1983;Bouillin et al., 1986). The equivalent Lucanian terrains in the south-ern Apennines display a tectono-sedimentary evolution fairly com-parable to those of the MFB (Bonardi et al., 2001; Guerrera et al.,2005; Vitale et al., 2011) and, at present hypothetically, they alsooccur in the northern Apennines according to de Capoa et al.(2003) and Perrone et al. (2014).

The oceanic nature of the MFB has been debated, however,because outcrops of a magmatic substratum were not observedin the Betic Cordillera and they are generally very scarce through-out the Maghrebian Belt (Gübeli et al., 1984; Durand-Delga et al.,

2000). Nevertheless, the oceanic substratum is well recognizablein the Lucanian Ocean units of the southern Apennines, whereultrabasic and basic rocks are broadly exposed (Bonardi et al.,2001). Biostratigraphic data indicate that the continental collisionalong the Maghrebian Chain, from the Gibraltar Arc to the easternSicily (de Capoa et al., 2004; di Staso et al., 2010; de Capoa et al.,2013), was roughly coeval and resulted in the MFB deformationduring the Middle Miocene due to the accretion of the previouslydeformed Mesomediterranean microplate (Guerrera et al., 2005)against the North African and the Southern Iberian Meso-Cenozoiccontinental paleomargins (Guerrera et al., 1993, 2005; Frizon deLamotte et al., 2000; Zaghloul, 2002; de Capoa et al., 2004; DiStaso et al., 2010; de Capoa et al., 2013).

The MFB Cretaceous successions were deposited between thesouthern margin of the Mesomediterranean microplate and theNorth Africa margin and are usually subdivided in two types ofsuccessions named, respectively, Mauretanian and Massylian; thelater was followed stratigraphically, and before Miocene detach-ment tectonics, by the Numidian Flysch successions (Gelard,1969; Bouillin et al., 1970; Thomas et al., 2010a, and Thomaset al., 2010b; Handy et al., 2010; Lustrino et al., 2011; Guerreraet al., 2012).

H. El Talibi et al. / Journal of African Earth Sciences 100 (2014) 554–568 557

The Massylian-Numidian subdomain is characterized byquartzose and arkosic petrofacies (Guerrera et al., 1992; Fildeset al., 2010; Thomas et al., 2010a, and Thomas et al., 2010b;Belayouni et al., 2010; Belayouni et al., 2012, 2013; Alcalá et al.,2013) derived mainly from basement rocks of the adjacent Africanplate whereas the Mauretanian sub-domain is characterized by lit-arenitic petrofacies (Gelard, 1969; Puglisi and Carmisciano, 1992;Puglisi et al., 2001; Zaghloul, 2002). The immature turbidite sedi-mentation deposited in the Mauretanian Zone, supplied by theInternal Domain, passes laterally to the Massylian Zone, by meansof «mixed successions» that have been recognized during Creta-ceous time (Durand-Delga, 1980) and especially during the EarlyMiocene (Didon and Hoyez, 1978; Guerrera et al., 1986;Carmisciano et al., 1987). The lithofacies and petrofacies of thesesuccessions are well known through the whole Maghrebian beltmainly during the Early Miocene and have been interpreted as amixing of two facies in the foredeep axis (Carmisciano et al.,1987; Hoyez, 1989).

The Massylian succession starts with Middle Jurasic limestonesassociated with Upper Jurassic dolerites and pillow-lavas; never-theless, these rocks have been exclusively found embedded withina Coniacian–Campanian marly matrix (Andrieux and Mattauer,

Fig. 3. Stratigraphic column of the Aptian–Albian successions (Ch

1963; Gübeli et al., 1984; Durand-Delga et al., 2000). The most typ-ical and widest outcropping Massylian flysch beds are constitutedby the so-called Aptian–Albian Flysch, a thick succession ofAptian–Albian pelites (locally marly) and medium- to fine-grainedsiliciclastic turbidite sandstones, which are studied in detail in thepresent paper (Fig. 3). Upwards, the succession evolves to UpperCretaceous claystones and marls with siliceous black shales andblack radiolarites (phtanites), sandstones, pelites and marly lime-stones, followed by Paleocene–Oligocene marls, breccias and num-mulitic-bearing limestones. The sequence is topped byAquitanian–Burdigalian Numidian sandstone suites (Andrieux,1971; Raoult, 1974; Wildi, 1983; Gübeli et al., 1984; Besson,1984; Durand-Delga and Olivier, 1988).

3. Sampling and analytical procedures

Two lithostratigraphic sections were measured and sampled(Fig. 2). Thirty samples were collected. Twenty-seven thin sections(from sample Ch1 to sample Ch27; Fig. 3 and Table 2) were pre-pared and examined under the polarizing microscope. Frameworkmineral composition (modal analysis) was quantified using thepoint-counting method of Gazzi-Dickinson, as described by

ouamat Nappe), with location of the studied samples.

Table 1Framework parameters of detrital modes after Ingersoll and Suczek (1979).

Qmn Non-undulouse monocrystalline quartzQmu Undulouse monocrystalline quartzQp Polycrystalline quartzQp 2–3 Qpq 2–3 crystal units per grainQp > 3 Qpq > 3 crystal units per grainCht ChertQt Total quartzose grains (Qm + Qp)P Plagioclase feldsparK Potassium feldsparF Total feldspar grains (P + K)Lv Volcanic–metavolcanic rock fragmentsLs Sedimentary rock fragmentsLm Metasedimentary rock fragmentsLt Total siliciclastic lithic fragments (L + Qp)RF Total unstable rock fragments and chert used for Folk (1974)

classificationAcc Accessory mineralsCem Cements

558 H. El Talibi et al. / Journal of African Earth Sciences 100 (2014) 554–568

Ingersoll et al. (1984). Framework parameters and detrital modesof sandstones are given in Tables 1 and 2 respectively.

For provenance studies we adopted the same standard methodsfor heavy mineral separation and analysis (Parfenoff et al., 1970).Chemical analyses of selected samples (from sample Th1 to sampleTh8; Fig. 3 and Table 3) were performed at the Platform for Ele-mentary Analysis in the National Center for Scientific and Techni-cal Research, Morocco.

Samples were chosen to cover the variations in color and grainsize among the sandstone beds of the studied stratigraphic sec-tions. Major and trace elements were obtained by X-ray fluores-cence (XRF) spectrometry technique on fused and pressed beads,respectively. Analytical precision is better than 3% for the majorelements and 7% for trace elements; accuracy was controlled byrepetitive measurements of standards, and each sample was mea-sured twice (e.g., Mongelli et al., 2006; Perri et al., 2011a). Trace

Table 2Recalculated detrital modes of 27 selected samples from Chouamat sandstones. X, mean v

Qt F L (%) Qm F Lt (%)

Qt F L Qm F Lt

Ch 1 98.8 1.2 0 96.9 1.2 1.8Ch 2 97.9 1.5 0.6 95.9 1.5 2.6Ch 3 97.1 2.6 0.3 95.9 2.7 1.5Ch 4 98.7 1.3 0 96.8 1.3 1.9Ch 5 99.1 0.9 0 96.5 0.9 2.6Ch 6 98.7 0.9 0.4 96.9 0.9 2.2Ch 7 94.9 4.1 0.9 82.5 4.3 3.2Ch 8 97.4 2.6 0 94.8 2.6 2.6Ch 9 98.5 1.5 0 96.1 1.5 2.4Ch 10 98.2 1.2 0.6 97.2 1.3 1.5Ch 11 99.1 0.6 0.3 98.4 0.6 0.9Ch 12 99.1 0.9 0 96.8 0.9 2.3Ch 13 97.6 1.8 0.6 95.6 1.8 2.7Ch 14 97.6 2.1 0.3 96.2 2.1 1.8Ch 15 98.2 1.5 0.3 97.1 1.5 1.5Ch 16 96.8 2.6 0.6 94.2 2.7 3.2Ch 17 98.3 1.7 0 96 1.8 2.3Ch 18 93.8 5.2 1 77.8 5.6 2.1Ch 19 98.5 1.2 0.3 96.8 1.2 2Ch 20 97.6 1.8 0.6 95.8 1.9 2.4Ch 21 99.4 0.6 0 97 0.6 2.4Ch 22 98.8 1.2 0 97.1 1.2 1.7Ch 23 97.2 2.3 0.6 95.2 2.3 2.5Ch 24 98.3 1.7 0 95.8 1.7 2.5Ch 25 94.4 4.5 1.1 74 4.7 2.2Ch 26 98.2 1.2 0.6 96.4 1.2 2.4Ch 27 99.1 0.9 0 97.9 0.9 1.2

X 97.8 1.9 0.4 94 1.9 2.2SD (±) ±1.4 ±1.1 ±0.4 ±6.7 ±1.2 ±0.6

elements were analyzed by inductively coupled plasma-atomicemission spectrometry (ICP-AES) with a Jobin Yvon Horiba Ultima2 sequential spectrometer. The precision of replicate analysis forICP-AES measurements was better than 3% for all analyzed traceelements. The geochemical results are provided in Table 3. Totaliron was expressed as Fe2O3. Total loss on ignition (L.O.I.) wasdetermined after heating the samples for 3 h at 900 �C.

4. Results

4.1. Lithostratigraphy and sedimentology of the Jbel Chouamatsuccession

The analyzed area is located in the Jbel Chouamat around theAousgane village. The general geological map of the Aptian–Albiansedimentary succession within the Chouamat Nappe (central Rif) ispresented in Fig. 2. In the present work, two lithostratigraphic sec-tions were measured and described (Fig. 3). Generally, the Aptian–Albian succession is mainly composed of mudstones and containsintercalations of thin-bedded well cemented turbiditic sandstones(Andrieux and Mattauer, 1963; Gübeli et al., 1984; Durand-Delgaet al., 2000). The succession is 150–250 m thick and starts withbluish marls and mudstones up to 60 m thick, overlain by thick-bedded quartzarenite stratasets usually amalgamated (Fig. 4A)(Andrieux, 1971; Raoult, 1974; Wildi, 1983; Gübeli et al., 1984;Besson, 1984; Durand-Delga and Olivier, 1988). The mudstonesare massive with sharp planar bases and tops (Fig. 4B). The thin-bedded sandstones are medium to fine grained. They are normallyor inversely graded (Fig. 4C), eventually with irregular bases andtops and with few sedimentary structures such as crude paralleland cross stratification, erosive structures as basal scouring andrelated mud clasts accumulations. Almost all the sandstone bedscan be described using the Bouma sequence (Bouma, 1962) andinclude two main facies: medium to fine-grained sandstones andmudstones associated with thin-bedded sandstones. The sand/

alue; SD, standard deviation.

Q F Lt (%) QmuQmnQp (%)

Q F Lt Qmu Qmn Qp

98.8 1.2 0 24.8 73.3 1.997.9 1.5 0.6 24.9 73.1 2.196.8 2.7 0.6 22.3 76.5 1.298.7 1.3 0 24.7 73.4 1.998.6 0.9 0.6 24.9 72.5 2.698.2 0.9 0.9 40.6 57.6 1.896.1 4.3 0.3 18 79.7 2.397.1 2.6 0.3 21.8 75.6 2.697.9 1.5 0.6 25.2 72.4 2.598.2 1.3 0.6 26.6 72.4 0.999.1 0.6 0.3 25.2 74.2 0.698.8 0.9 0.3 26.5 71.1 2.497.1 1.8 1.2 27.2 70.7 2.197 2.1 0.9 27.6 70.9 1.598.2 1.5 0.3 24.1 74.7 1.296.5 2.7 0.9 22.7 74.6 2.797.7 1.8 0.6 22.9 74.7 2.495 5.6 0.6 16.7 82.2 1.198 1.2 0.9 23 75.2 1.897.6 1.9 0.6 25.2 73 1.998.5 0.6 0.9 27.2 70.4 2.498.3 1.2 0.6 27.1 71.1 1.896.9 2.3 0.8 30 67.9 297.7 1.7 0.6 25 72.4 2.696.2 4.7 0.3 3.1 95.7 1.298.2 1.2 0.6 31.5 66.7 1.999.1 0.9 0 22.3 76.5 1.2

97.7 1.9 0.6 24 74.2 1.8±1 ±1.2 ±0.3 ±6.8 ±6.8 ±0.6

Table 3Major and trace element concentrations and selected elemental ratios in the studied samples.

Chouamat sandstones

Th1 Th2 Th3 Th4 Th5 Th6 Th7 Th8 Mean value

Major oxides (wt.%)SiO2 93.40 94.40 91.70 95.80 94.00 91.80 96.10 94.50 93.96Al2O3 1.77 1.76 4.31 1.37 1.87 5.52 2.15 2.65 2.68K2O 0.20 0.25 0.13 0.12 0.10 0.38 0.15 0.10 0.18Na2O 0.16 0.15 0.19 0.09 0.09 0.68 0.27 0.15 0.22CaO 0.06 0.10 0.05 0.05 0.06 0.01 0.02 0.02 0.05TiO2 0.24 0.30 0.14 0.34 0.17 0.19 0.16 0.22 0.22Fe2O3 0.46 0.46 0.66 0.78 0.73 0.20 0.21 0.46 0.49MgO 0.29 0.26 0.43 0.24 0.26 0.41 0.27 0.23 0.30P2O5 0.03 0.03 0.04 0.03 0.03 0.03 0.02 0.03 0.03LOI 0.83 0.65 0.59 0.53 1.87 0.57 0.63 1.64 0.91Total 96.60 97.70 97.63 98.82 97.31 99.21 99.35 98.34 98.12

Trace elements (ppm)Co 3.03 2.05 0.87 1.85 1.19 1.21 2.21 1.07 1.69Rb 30.78 51.57 43.08 29.31 30.49 55.50 40.70 40.34 40.22Cr 33.24 25.73 17.23 26.74 15.38 20.94 17.12 24.43 22.60Ni 19.41 17.39 19.94 20.25 17.44 19.86 13.32 21.53 18.64V 50.32 33.01 27.45 33.16 22.92 30.41 27.01 30.50 31.85Sc 1.86 1.49 1.89 0.75 1.48 1.82 1.56 1.64 1.56Ba 41.96 51.30 39.57 42.13 35.79 39.70 41.68 80.19 46.54La 9.66 10.86 9.09 11.20 7.84 10.38 9.68 10.82 9.94Ce 20.61 22.90 19.12 24.35 16.27 21.31 20.76 23.29 21.08Th 25.45 10.45 19.89 20.45 25.26 25.21 19.35 25.33 21.42Sr 21.35 23.50 20.45 23.60 19.22 20.58 16.55 28.53 21.72Nd 43.64 38.66 44.30 39.59 35.79 44.43 38.25 39.68 40.54Sm 2.60 2.38 1.89 2.24 2.37 2.00 2.50 1.64 2.20Zr 32.87 23.35 20.83 27.93 20.85 40.79 29.82 29.35 28.22Eu 1.86 1.49 1.89 1.49 1.48 1.82 1.56 1.64 1.65Gd 4.27 3.87 3.79 3.88 3.40 4.19 3.59 3.61 3.82Tb 1.86 1.49 1.89 1.94 1.48 1.82 1.56 1.64 1.71Ho 0.94 1.18 2.44 1.57 1.32 1.01 0.49 1.74 1.34Er 0.74 0.60 0.76 0.60 0.59 0.73 0.62 0.66 0.66Yb 2.04 1.64 1.89 1.49 1.48 1.82 1.56 1.80 1.72Lu 0.93 0.89 0.38 1.05 0.44 0.91 0.94 0.98 0.82

Geochemical ratiosCIA 74.21 70.63 88.94 78.47 83.67 78.04 77.03 87.23 79.78PIA 85.62 83.74 92.93 87.93 89.70 85.15 84.32 92.02 87.68CIW 83.01 80.03 92.60 86.28 88.90 83.67 82.68 91.55 86.09K2O3/Al2O3 0.11 0.14 0.03 0.09 0.05 0.07 0.07 0.04 0.08Th/Sc 13.70 7.03 10.51 27.38 17.08 13.84 12.40 15.45 14.67La/Sc 5.20 7.30 4.80 15.00 5.30 5.70 6.20 6.60 7.01Th/Co 8.40 5.07 22.84 11.02 21.09 20.79 8.72 23.58 15.19Th/Cr 0.77 0.41 1.15 0.76 1.64 1.20 1.13 1.04 0.95

H. El Talibi et al. / Journal of African Earth Sciences 100 (2014) 554–568 559

mud ratio and the sedimentary structures are typical of distalturbidites. The middle and upper part of the sections is character-ized by terrigenous turbidites that become more widespread andthicker upwards: the sandstone beds can be more than 3 m thick,with Tc-e Bouma sequence that are often amalgamated and cutoff at the top. These lithofacies can be interpreted as distal-lobeand lobe-fringe deposits laid down in distal areas of a deep turbi-dite system. The progradational system of the Jbel Chouamat suc-cession produced important vertical facies changes, suggesting adeposition in a linear trough in front of the northern African mar-gin during the Early Cretaceous.

4.2. Sandstone petrography

The Chouamat sandstone suites are medium to fine grainedwell sorted sands; these samples are further sub-mature to maturein composition (Fig. 5A). The cement of subarkose samples is gen-erally composed of argillaceous materials, such as pore-filling kao-linite (Fig. 5B). In contrast, the quartzarenites are mainly cementedby quartz overgrowths with minor grain-coatings formed by argil-laceous cements, thus reflecting their slightly mature mineralogi-cal composition.

Quartz is the most abundant framework grain in the studiedsandstone suites; the average framework composition is Q97.8 F1,9

Lt0,4 (Table 2). Monocrystalline quartz grains are dominant and,generally, they have not undulose extinction. Polycrystallinequartz grains are composed mainly of non-oriented crystalliteswith straight to undulose extinction.

All studied thin sections contain small amounts of potassiumfeldspar and plagioclase. The plagioclase (average value 1.9%) dom-inates over K-feldspar (average value 0.76%) and mostly occurs asfresh to altered grains and exhibits twinning (Fig. 5C). Lithic frag-ments are comparatively less abundant in many samples, do notexceed 1.2%, with an average value of 0.6%, and are mainly of sed-imentary origin. They include hematitic siltstone, hematitic clay-stone and chert (Fig. 5D). Micas form a minor component in theanalyzed samples, and are usually formed by muscovite; they arelocally kaolinitised and display fish-tail splaying and lattice expan-sion (Fig. 5E). Biotite fragments are also recorded (Fig. 5F). Theheavy minerals occur in scattered minor quantities throughoutthe samples; their contents does not exceed 0.3%. Heavy mineralgrains are very fine grained and show moderate abrasion. The lat-ter consist of Fe and Fe–Ti oxides, epidote, kyanite, zircon, tourma-line, hornblende, sphene and minor amounts of corundum (Fig. 6).

The analyzed samples were plotted in QFL ternary diagrams(Dickinson and Suczek, 1979; Dickinson et al., 1983), includingdetrital grains but excluding micas, opaques and heavy minerals.Chert was counted as a sedimentary rock fragment. The studied

Fig. 4. (A) Panoramic view of outcrops and of the amalgamated sandstones beds. (B) Base of the Aptian–Albian siliciclastic succession of the Chouamat Nappe, formed byalternating bluish-colored marls, pelites and siltstones. (C) Sandstone beds with parallel lamination. (For interpretation of the references to colour in this figure legend, thereader is referred to the web version of this article.)

Fig. 5. Photomicrographs of Chouamat sandstones showing: (A) Quartzarenite sample; quartz grains are medium to fine-grained, and sub-rounded to sub-angular. (B)Subarkose with argillaceous pore-filling cement; Quartz (Q), Plagioclase single crystal (Pl), kaolinite cement (K). (C) Quartzarenite showing one plagioclase single crystals (Pl).(D) Subarkose with chert fragment (Cht). (E) Photomicrograph showing mica single crystal, muscovite (Ms). (F) Biotite fragment (Bi).

560 H. El Talibi et al. / Journal of African Earth Sciences 100 (2014) 554–568

Fig. 6. Microphotogaphs of heavy minerals within the Chouamat sandstones. (1) Corundum; (2) Kyanite; (3) Tourmaline; (4) Sphene; (5) Epidote; (6) Zircon.

H. El Talibi et al. / Journal of African Earth Sciences 100 (2014) 554–568 561

sandstones are classified as quartzarenite with subordinate subli-tharenite and subarkose (Fig. 7a).

4.3. Geochemistry

The chemical composition, the weathering indices and someuseful geochemical ratios of the Chouamat sandstones are listedin Table 3.

The analyzed samples are dominated by SiO2 with values rang-ing from 91.7 wt.% to 96.1 wt.%, and have low K2O/Al2O3 ratios,while other major oxides are generally below than 1.0 wt.%(Table 3). The studied samples show a similar elemental composi-tion, as shown in the geochemical classification diagrams of Herron(1988), where the studied sandstones are classified as quartzare-nites with few sublitharenite and subarkose samples (Fig. 8).

The source of silica is mainly related to quartz, chert, feldsparsand clay minerals. Al2O3 and K2O contents are related to the pres-ence of K-feldspars (microcline), illite and mica. The source of Na2Ois principally related to plagioclase feldspar. SiO2 abundance wasused as a normalization factor to make comparisons among the dif-ferent major elements, because of its immobile nature duringweathering, diagenesis, and metamorphism (e.g., Bauluz et al.,2000). Fig. 9 shows the major oxides plotted against SiO2 andshows that silica is negatively correlated with Fe2O3 and withAl2O3.

The studied samples revealed a relative enrichment of some traceelements such as Zr (mean = 28.22 ppm), Cr (me an = 22.60 ppm), V(mean = 31.84 ppm), and Th (me an = 21.42 ppm) (Table 3). Theabundance of high field strength elements (e.g. Cr, Zr, etc.) can be

related to the presence of detrital minerals such as chromite, sphene,and zircon (Huntsman-Mapila et al., 2005).

5. Discussion

5.1. Source area weathering

Chemical composition of detrital sediments is largely depen-dent on the lithological composition and on the weathering condi-tions in the source area (Nesbitt and Young, 1989; Nesbitt et al.,1996).

In this sense, the negative correlation of silica as shown in thecross plots of % SiO2 vs. Fe2O3 and vs. Al2O3 (Fig. 9) indicates influ-ence of weathering processes through enrichment of silica anddepletion of Fe and Mg. The implication of marked negative corre-lation between SiO2 and Al2O3 is probably related to the quartzdilution effect affecting the relative abundance of phyllosilicateand, thus, to the competition between mica-like clay mineralsand quartz (e.g., Mongelli et al., 2006). The low K2O/Al2O3 ratios(Table 3) further suggest recycling processes experienced by thestudied samples. It can be concluded, therefore, that the depletionof all other major elements in the Chouamat sandstone is probablyrelated to the removal of ferromagnesian minerals and feldsparsthrough reworking and transportation of the source materials bysedimentary processes.

As demonstrated by Nesbitt and Young (1982), a measure of thedegree of chemical weathering of the source rocks can be con-strained by calculating the Chemical Index of Alteration (CIA = mo-lar (Al2O3/[Al2O3 + CaO⁄ + Na2O + K2O]) where CaO⁄ represents the

Fig. 7. (a) QmFLt triangular diagram shows the classification of the Chouamat sandstones (modified after Dickinson et al., 1983). (b) QtFLt ternary plot of the sandstonesamples (modified after Dickinson et al., 1983). (c) Quartz grain varieties in the studied sandstones (e.g., Basu et al., 1975). Legend: Qt, total quartz; Qp, polycrystalline quartz;Qm, monocrystalline quartz; Qmu, monocrystalline quartz with undulose extinction; Qmn, monocrystalline quartz with straight extinction; F, feldspars; Lt, total lithicfragments.

Fig. 8. Chemical classification of the Chouamat sandstone based on the log(SiO2/Al2O3) vs. log(Fe2O3/K2O) diagram of Herron (1988).

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amount of CaO in silicate minerals only). The Chemical Index ofWeathering (CIW = molar [Al2O3/(Al2O3 + CaO⁄ + Na2O)]; Harnois,1988), is further used to monitor the weathering conditions ofthe source(s). Usually, the CIA or CIW are interpreted in similarway with values of about 50 for unweathered (fresh) materialsand about 100 for highly weathered residual soils, with completeremoval of alkali and alkaline-earth elements (McLennan et al.,

1983; McLennan et al., 1993; Mongelli et al., 1996). The degreeof the chemical weathering can also be estimated using the Plagio-clase Index of Alteration (PIA = [(Al2O3 � K2O)/(Al2O3 + CaO + Na2O� K2O)]⁄100; Fedo et al., 1995). The high values of CIA(mean = 79.8) and CIW (mean = 86.1) for the samples clearly indi-cate strong weathering conditions for the primary source mate-rial(s). In the A–CN–K ternary diagram (Al2O3 � Ca O + Na2O � K2

O; Nesbitt and Young, 1982) the studied samples fall close to theA apex in the direction of the kaolinite, chlorite and gibbsite com-position indicating high degree of alteration at the source area(s)(Fig. 10).

The Chouamat sandstones show uniform CIW values (Table 3),and fall close to the A apex in the A–C–N plot (Fig. 11). A similartrend is shown in the (A–K)–C–N diagram (Fig. 11), since the PIAvalues (mean = 87.7) are generally high for all the studied sand-stones. Thus, results from both the CIW and PIA indices indicatea probably intense weathering in the source area(s).

The chemical composition of the studied sandstone, the highproportion of quartz (>90%), the few amounts of K-feldspar, andthe absence of the more chemically unstable plagioclase and otherlabile components (see Tables 2 and 3) suggest that the sourcerocks were exposed to prolonged and intense weathering condi-tions probably associated with multiple cycles of sedimentaryrecycling.

Hydraulic sorting and recycling processes can significantlyinfluence the chemical composition of terrigenous sediments(e.g., Garcia et al., 2004; Armstrong-Altrin, 2009) and controlsthe distribution of some trace elements (e.g., Th, Sc, Zr, Hf and

Fig. 9. Harker variation diagrams for major elements in the Chouamat sandstones.

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Nb) (McLennan et al., 1993). The presence of sorting-relatedfractionations is evaluated when the Zr/Sc ratio (a useful indexof sediment recycling) is plotted against the Th/Sc ratio (indicatorof chemical differentiation) (e.g., McLennan et al., 1993; Perriet al., 2011a and references therein). Generally, Th/Sc and Zr/Scratios tend to correlate positively in first cycle sediments,whereas in more mature or recycled sediments Zr/Sc tends tobecome increasingly higher and nearly independent of changesin Th/Sc (McLennan et al., 1993). The studied sandstones arenot clustered along the primary compositional trend but fallalong a trend involving zircon addition and thus sediment recy-cling (Fig. 12).

Sediment recycling could significantly affect the CIW and PIAweathering indices, which likely monitor a cumulative effect,including several cycles of weathering at the source (e.g.,Mongelli et al., 2006; Critelli et al., 2008). The high weathering val-ues of the Early Cretaceous Chouamat sandstones suggest thathumidity increased in the Western Tethys region during late Meso-zoic time. The wet-humid conditions promoted weathering anderosion whereas the dry season favored the sedimentation. Fur-thermore, climate alternation favored the recycling process affect-ing the sediments in the Rif Chain (e.g., Critelli et al., 2008;Zaghloul et al., 2010; Perri et al., 2011a, 2013; Perri, 2014; Perriand Otha, 2014).

Fig. 10. Ternary A–CN–K plot of the sandstone samples. Legend: Ms, muscovite; Ilt,illite; Khl, kaolinite; Chl, chlorite; Gbs, gibbsite; Smt, smectite; Bt, biotite; Kfs, K-feldspar; Pl, plagioclase; A, Al2O3; CN, CaO + Na2O; K, K2O (oxides are plotted asmolar proportions with CaO being CaO content in silicate fraction of the samples);CIA, Chemical Index of Alteration (Nesbitt and Young, 1982).

Fig. 12. Th/Sc vs. Zr/Sc plot (after McLennan et al., 1993). Samples depart from thecompositional trend indicating zircon addition suggestive of a recycling effect.

564 H. El Talibi et al. / Journal of African Earth Sciences 100 (2014) 554–568

5.2. Provenance features

The tectonic setting of the depositional environment is assumedto influence sedimentation, diagenesis and composition of sedi-ments (Pettijohn et al., 1972; Chamley, 1990). Several studies haveused composition of sandstones to infer provenance and tectonicsettings (Basu et al., 1975; Dickinson et al., 1983; Cavazza andIngersoll, 2005). Hence, further evidences for the provenance andtectonic settings can be inferred from the relative depletion in oxi-des as CaO, Na2O (the most mobile phases) and enrichment in SiO2

and TiO2 (the most immobile components).Based on the QtFLt ternary diagram (Fig. 7b), the Chouamat

sandstones can be clearly constrained to mature quartzarenite ofcontinental cratonic block provenance. This implies that sand-stones are derived mainly from exposed shield/platform or fromuplifted areas and deposited in tectonically stable sites (Taylorand McLennan, 1985; Potter, 1978, 1986).

Because of the paucity of feldspars and rock fragments in thestudied samples, parent rock lithology was established mainlyfrom interpretation of quartz grain types. Polycrystalline quartzgrains are plotted vs. undulatory to non-undulatory monocrystal-line quartz grains following the technique of Basu et al. (1975) toevaluate the relative importance of quartz grain types for deter-mining the provenance of the Aptian–Albian Choumate sandstones(Fig. 7c). This plot suggests that quartz grains are mainly of plu-tonic origin. According to Basu et al. (1975), the relatively high

Fig. 11. Ternary A–C–N and (A–K)–C–N plots of the Chouamat sandstones. Legend: A, Al2

CaO content in silicate fraction of the samples); CIW, Chemical Index of Weathering (Ha

proportion of fine- to medium-grained monocrystalline quartz insandstones may be attributed to the disaggregation of originalpolycrystalline quartz during high energy transport from thesource area. Therefore, with Q values higher than 96% and negligi-ble F and L components, the quartzarenite designation for Choua-mat sandstones is consistent with the tectonically stable craton/shield source area connected with a passive continental marginsetting. This is consistent with the classification of Crook (1974),which linked quartz-dominated sandstones (Q > 65%) to passive(Atlantic type) continental margins. The lower amounts of unstablegrains (feldspar and other lithic fragments), suggest that thesesandstones were transported far away along the rift.

Trace elements in clastic sedimentary rocks are generally con-sidered to be immobile under conditions of weathering, diagenesisand moderate levels of metamorphism, and are commonly pre-served in sedimentary rocks (Bhatia and Crook, 1986; McLennanet al., 1993). In particular, mafic to intermediate rocks are charac-terized by abundant Co, Sc, Cu, Ni and Ti, whereas felsic rocks showhigh values of La, Th, Y and Zr (e.g., Taylor and McLennan, 1985;Cullers, 1994). Hence, ratios such as Th/Sc, La/Sc and others and tri-angular relationships of V–Ni–Th⁄10 (e.g., Bracciali et al., 2007)have been also used to discriminate the source area composition.Table 3 shows several geochemical ratios, such as La/Sc, Th/Sc,Th/Co and Th/Cr, of the studied samples that are consistent withvalues commonly recorded for felsic igneous rocks and indicatethe lack of a marked mafic–ultramafic detritus (e.g., Perri et al.,

O3; C, CaO; N, Na2O; K, K2O (oxides are plotted as molar proportions with CaO beingrnois, 1988); PIA, Plagioclase Index of Alteration (Fedo et al., 1995).

Fig. 13. (A) V–Ni–Th⁄10 ternary diagram, showing fields representative of felsic, mafic and ultramafic rocks plot separately (e.g., Bracciali et al., 2007) and (B) TiO2 vs. Nibivariate plot of the Chouamat sandstones (fields after Floyd et al., 1989).

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2011a, 2013 and references therein). Furthermore, in the V–Ni–Th⁄10 ternary diagram (Fig. 13A), showing fields representativeof felsic, mafic and ultramafic rocks plotting separately (e.g.,Bracciali et al., 2007; Perri et al., 2011b), the studied sandstonesplot close to the felsic composition and to the Upper ContinentalCrust composition (McLennan et al., 2006). Thus, this distributionsuggests a provenance from a source-area characterized by domi-nantly felsic source rocks. The latter provenance is further con-firmed by the TiO2 vs. Ni bivariate plot reflecting the negligiblemafic input for the studied samples (Fig. 13B). Hence, all these geo-chemical proxies suggest that the Chouamat samples were mainlyderived from an upper continental crust composed chiefly of felsiccomponents.

According to aforementioned data, we can conclude that theAfrican source of the Massylian Flysch area is beyond evident. Infact, a clastic deposit formed by ultramature petrofacies must befed from a craton (Dickinson, 1985; among others) and not froma young orogenic area such as the Alpine chains. In addition, thepersistent presence along the chains of the mixed successions(Guerrera et al., 1986) since the Early Cretaceous (Durand-Delga,1980; Zaghloul et al., 2003) reflects the lateral relationshipsbetween internal (Mauretanian) and external (Massylian) sub-Domains of the Maghrebian Flysch Basin as a key also to under-standing the palaeogeography of both sub-Domains. In fact, areview of the location of Massylian Flysch nappes within theAlpine thrust belt confirms the Massylian Flysch to have beendeposited in the North African margin and related basin(Durand-Delga, 1980).

6. Conclusions

The Massylian siliciclastic Aptian–Albian Flysch of the Choua-mat Nappe in the central Rif of Morocco consists mainly of mud-stones with interbedded distal turbiditic sandstones forming afacies association belonging to distal-lobe and lobe-fringe deposi-tional environments within a deep sea fan. The petrology of theChouamat sandstones coupled to their chemical analyses, allowsdetermining their provenance, source area weathering and tectonicsetting. The Chouamat sandstones composition is mostly quartzar-enite and subordinate sublitharenite and subarkose. The geochem-ical analysis shows that the studied samples are mainlycharacterized by high SiO2 values and that they are depleted intransitional elements such as Cr, Co, Ni and V. Recycling effectsfrom basement rocks are suggested by the sample distribution onthe Zr/Sc vs. Th/Sc diagram, which also suggests that the Chouamatsandstones are compositionally mature and characterized by zir-con addition due to recycling effects. The high values of weatheringindices (CIA, CIW and PIA) indicate that their source area(s)

underwent more intense chemical weathering processes. Thus,the chemical composition of the studied sandstones, the high pro-portion of quartz (>90%), the few amounts of K-feldspar, and theabsence of the more chemically unstable plagioclase and otherlabile components suggest that the source rocks were exposed toprolonged and intense weathering conditions probably associatedwith multiple cycles of sedimentary recycling. The petrographicstudy associated with geochemical analyses indicate a provenancefor the Chouamat sandstones from a craton interior (i.e continen-tal-block) mainly characterized by felsic rocks. Therefore, this con-tinental-block was possibly consisting of the adjacent NorthAfrican plutonic rocks and/or older metasedimentary covers,weathered and eroded during the Cretaceous. These source rocksare related to a large cratonic source region of probably Eburneanand Pan-African belts, Precambrian? and/or Variscan basementslocated at the southeastern side of the African plate margin.

Acknowledgments

The authors are thankful to Director of Platform for ElementaryAnalysis in the National Center for Scientific and TechnicalResearch, Morocco for providing chemical analysis of the sand-stones samples. The authors are indebted to Manuel Martín Martín,Agustín Martín-Algarra and the Editor Read Mapeo for theirreviews and suggestions on an earlier version of the manuscript.

References

Alcalá, F.J., Guerrera, F., Martín-Martín, M., Raffaelli, G., Serrano, F., 2013.Geodynamic implications derived from Numidian-like distal turbiditesdeposited along the internal–external domain boundary of the BeticCordillera (S Spain). Terra Nova 26, 119–129.

Andrieux, J., Mattauer, M., 1963. Sur la présence de roches vertes a la base desnappes « ultra » du Rif. Comptes Rendus Sommaire de le Société Géologique deFrance 7, 213–215.

Andrieux, J., 1971. La structure du Rif central. Étude des relations entre latectonique de compression et les nappes de glissement dans un tronçon de lachaîne alpine. Notes et Mémoires Service Géologique du Maroc 235.

Armstrong-Altrin, J.S., 2009. Provenance of sands from Cazones, Acapulco, and BahíaKino beaches, México. Revista Mexicana de Ciencias Geológicas 26, 764–782.

Basu, A., Young, S.W., Suttner, L.J., Ames, W.C., Mack, G.H., 1975. Reevaluation of theuse of undulatory extinction and polycrystallinity in detrital quartz forprovenance interpretation. J. Sediment. Petrol. 45, 873–882.

Bauluz, B., Mayayo, M.J., Fernandez-Nieto, C., Gonzalez Lopez, J.M., 2000.Geochemistry of Precambrian and Paleozoic siliciclastic rocks from theIberian Range (NE Spain): implications for source-area weathering, sorting,provenance, and tectonic setting. Chem. Geol. 168, 135–150.

Belayouni, H., Brunelli, D., Clocchiatti, R., Di Staso, A., El Amrani El Hassani, I.,Guerrera, F., Kassaa, S., Laridhiouazaa, N., Martín-Martín, M., Serrano, F.,Tramontana, M., 2010. La Galite Archipelago (Tunisia, North Africa):Stratigraphic and petrographic revision and insights for geodynamic evolutionof the Maghrebian Chain. J. African Earth Sci. 56, 15–28.

Belayouni, H., Guerrera, F., Martín-Martín, M., Serrano, F., 2012. Stratigraphicupdate of the Cenozoic Sub-Numidian formations of the Tunisian Tell (North

566 H. El Talibi et al. / Journal of African Earth Sciences 100 (2014) 554–568

Africa): tectonic/sedimentary evolution and correlations along the MaghrebianChain. J. African Earth Sci. 64, 48–64.

Belayouni, H., Guerrera, F., MartÃ-n-MartÃ-n, M., Serrano, F., 2013. Paleogeographicand geodynamic Miocene evolution of the Tunisian Tell (Numidian and post-Numidian Successions): bearing with the Maghrebian Chains. Int. J. Earth Sci.(Geol. Rundsch.) 102, 831–855.

Benzaggagh, M., Mokhtaria, A., Rossi, P., Michard, A., El Maza, A., Chalouan, A.,Saddiqi, O., Rjimati, E., 2013. Oceanic units in the core of the External Rif(Morocco): Intramargin hiatus or South-Tethyan remnants?. J. Geodynam. (inpress).

Besson, F., 1984. Etude géologique et structurale des Nappes de Flyschs et des ZonesExternes dans la région de l’oued Rhiss (Rif central, Maroc). Orsay, Paris, Ph.D.thesis. pp. 190.

Bhatia, M.R., Crook, K.A.W., 1986. Trace element characteristics of graywackes andtectonic setting discrimination of sedimenatry basins. Contribut. Mineral.Petrol. 92, 181–193.

Bonardi, G., Cavazza, W., Perrone, V., Rossi, S., 2001. Calabria-Peloritani Terrane andNorthern Ionian Sea. In: Vai, G.B., Martini, I.P. (Eds.), Anatomy of an Orogen: TheApennines and Adjacent Mediterranean Basins. Kluwer Academic Publishers,Dordrecht, Boston, London, pp. 287–306.

Bonardi, G., de Capoa, P., Di Staso, A., Estevez, A., Martín-Martín, M., Martín-Rojas, I.,Perrone, V., Tent-Manclus, J.E., 2003. Oligocene to Early Miocene depositionaland structural evolution of the Calabria-Peloritani Arc southern subterrane(Italy) and geodynamic correlations with the Spain Betics and Morocco Rif.Geodin. Acta 16, 149–169.

Bouillin, J.P., Durand Delga, M., Gelard, J.P., Leikine, M., Raoult, J.F., Raymond, D.,Tefiani, M., Et Vila, J.M., 1970. Définition d’un Flysch Massylien et d’un FlyschMaurétanien au sein des Flysch Allochtones de l’Algérie. Comptes Rendus del’Académie des Sciences, Paris 270, 2249–2252.

Bouillin, J.P., Durand Delga, M., Olivier, Ph., 1986. Betic-Rifain and Tyrrhenian arcs:distinctive features, genesis and development stages. In: Wezel, F. (Ed.), TheOrigin of Arcs. Elsevier Science Publishers, Amsterdam, pp. 281–304.

Bouma, A.H., 1962. Sedimentology of some flysch deposits: a graphic approach tofacies interpretation. Elsevier, Amsterdam, 168 p.

Bouybaouene, M.L., Goffé, B., Michard, A., 1995. High-pressure Granulites on Top ofthe Beni Bousera Peridotites, Rif Belt, Morocco: a record of an ancient thickenedcrust in the Alboran domain. Bull. Soc. géol. Fr. 169, 153–162.

Bracciali, L., Marroni, M., Luca, P., Sergio, R., 2007. Geochemistry and petrography ofWestern Tethys Cretaceous sedimentary covers (Corsica and NorthernApennines): From source areas to configuration of margins. GSA Special Paper420, 73–93.

Caracciolo, L., Le Pera, E., Muto, F., Perri, F., 2011. Sandstone petrology andmudstone geochemistry of the Peruc-Korycany Formation (BohemianCretaceous Basin, Czech Republic). Int. Geol. Rev. 53, 1003–1031.

Carmisciano, R., Coccioni, R., Corradini, D., d’Alessandro, A., Guerrera, F., Loiacono, F.,Moretti, E., Puglisi, D., Sabato, L., 1987. New data from the Lower Miocene‘‘mixed successions’’ from Algeria (Great Kabylia) and from Sicily (NebrodiMts.): comparison with similar turbiditic successions from the Gibraltar Arc andlucanian Apennines. Memorie della Società Geologica Italiana 38, 551–576.

Cavazza, W., Ingersoll, R., 2005. Detrital modes of the Ionian forearc basin fill(Oligocene-Quaternary) reflect the tectonic evolution of the Calabria-Peloritaniterrane (southern Italy). J. Sediment. Res. 75, 268–279.

Chalouan, A., Michard, A., 1990. The Ghomarides Nappes, Rif Coastal Range,Morocco: A Variscan Chip in the Alpine Belt. Tectonics 9, 1565–1583.

Chalouan, A., Michard, A., Feinberg, H., Montigny, R., Saddiqui, O., 2001. The RifMountain building (Morocco): a new tectonic scenario. Bulletin de la SociétéGéologique de France 172, 603–616.

Chalouan, A., Michard, A., 2004. The Alpine Rif Belt (Morocco): a case of mountainbuilding in a subduction–subduction–transform fault triple junction. Pure Appl.Geophys. 161, 489–519.

Chalouan, A., Michard, A., El Kadiri, K., Negro, F., Frizon de Lamotte, D., Soto, J.I.,Saddiqi, O., 2008. The Rif. In: Michard, A., Saddiqi, O., Chalouan, A., Frizon deLamotte, D. (Eds.), Continental Evolution: The Geology of Morocco-Structure,Stratigraphy, and Tectonics of the Africa-Atlantic-Mediterranean TripleJunction. Springer, 24p.

Chamley, H., 1990. Clay Sedimentology. Springer-Verlag, Berlin.Critelli, S., Arribas, J., Le Pera, E., Tortosa, A., Marsaglia, K.M., Latter, K., 2003. The

recycled orogenic provenance sand suite from an uplifted thrust-belt, BeticCordillera, southern Spain and the Alboran Basin. J. Sediment. Res. 73, 72–81.

Critelli, S., Mongelli, G., Perri, F., Martin-Algarra, A., Martin-Martin, M., Perrone, V.,Dominici, R., Sonnino, M., Zaghloul, M.N., 2008. Compositional and geochemicalsignatures for the sedimentary evolution of the Middle Triassic-Lower Jurassiccontinental redbeds from western-central Mediterranean Alpine chains. J. Geol.116, 375–386.

Crook, K.A.W., 1974. Lithogenesis and geotectonics: the significance ofcompositional variations in flysch arenites (graywackes). In: Modern andAncient Geosynclinal Sedimentation. In: Dott, R.H., Shaver, R.H. (Eds.), . Societyfor Sedimentary Geology Special Publication, 19, pp. 304–310.

Cullers, R.L., 1994. The controls on the major and trace element variation of shales,siltstones, and sandstones of Pennsylvanian-Permian age from upliftedcontinental blocks in Colorado to platform sediments in Kansas, USA.Geochim. Cosmochim. Acta 58, 4955–4972.

de Capoa, P., Guerrera, F., Perrone, V., Tramontana, M., 2003. The extension of theMaghrebian Flysch Basin in the Apenninic Chain: Palaeogeographic andpalaeotectonic implications. Travaux de l’Institut Scientifique de Rabat 21,77–92.

de Capoa, P., Di Staso, A., Guerrera, F., Perrone, V., Tramontana, M., 2004. The age ofthe oceanic accretionary wedge and the continental collision in the Siciliansector of the Maghrebian Chain. Geodin. Acta 17, 331–348.

de Capoa, P., Di Staso, A., Perrone, V., Zaghloul, M.N., 2007. The age of the foredeepsedimentation in the Betic-Rifian Mauretanian Units: a major constraint for thereconstruction of the tectonic evolution of the Gibraltar Arc. C.R. Geosci. 339,161–170.

de Capoa, P., D’Errico, M., Di Staso, A., Perrone, P., Somma, R., Zaghloul, M.N., 2013.Biostratigraphic constraints for the paleogeographic and tectonic evolution ofthe Alpine Central-Western Mediterranean orogenic belt (Betic, Maghrebianand Apenninic chains). Rendiconti Online della Società Geologica Italiana 25.

Dercourt, J., Zonenshain, L.P., Ricou, L.E., et al., 1985. Présentation de neuf cartespaléogéographiques au 1/ 20.000.000 s’étendant de l’Atlantique au Pamir pourla période du Lias à l’Actuel. Bulletin de la Société Géologique de France 8, 637–652.

Di Staso, A., Perrone, V., Perrotta, S., Zaghloul, M.N., Durand-Delga, M., 2010.Stratigraphy, age and petrography of the Beni Issef successions (External Rif;Morocco): Insights for the evolution of the Maghrebian Chain. C.R. Geosci. 342,718–730.

Dickinson, W.R., Suczek, C.A., 1979. Plate tectonics and sandstone compositions.AAPG Bull. 63, 2164–2182.

Dickinson, W.R., Beard, L.S., Brakenridge, G.R., Erjavek, J.L., Ferguson, R.C., Inman,K.F., Knepp, R.A., Lindberg, F.A., Ryberg, P.T., 1983. Provenance of NorthAmerican Phanerozoic sandstones in relation to tectonic setting. GSA Bull. 94,222–235.

Dickinson, W.R., 1985. Interpreting provenance relation from detrital modes ofsandstones. In: Zuffa, G.G. (Ed), Provenance of Arenites, Reidel PublishingCompany, Dordrecht, NATO ASI Series C148, pp. 333–363.

Didon, J., Hoyez, B., 1978. Les séries à facies mixte, numidien et gréso-micacé, dansle Rif occidental (Maroc). Compte Rendu Sommaire des séances de la SociétéGéologique de France 6, 304–307.

Durand-Delga, M., 1980. Considérations sur les flyschs du Crétacé inférieur dans leschaînes alpines d’Europe. Bulletin de la Société Géologique de France 7, 15–30.

Durand-Delga, M., Fontboté, J.M., 1980. Le cadre structural de la Méditerranéeoccidentale. In: 26th International Geological Congress, Paris 5, pp. 67–85.

Durand-Delga, M., Olivier, P., 1988. Evolution of the Alboran Block margin fromEarly Mesozoic to Early Miocene time. In: Jacobshagen, V.H. (Ed.), The AtlasSystem of Morocco. Springer, Berlin, pp. 465–480.

Durand-Delga, M., Rossi, P., Olivier, P., Puglisi, D., 2000. Situation structurale etnature ophiolitique de roches basiques jurassiques associées aux flyschsMaghrébens du Rif (Maroc) et de Sicile (Italie). Comptes Rendus del’Académie des Sciences 331, 29–38.

El Hatimi, N., Duée, G., Hervouet, Y., 1991. La Dorsale calcaire du Haouz: anciennemarge continentale passive téthysienne (Rif, Maroc). Bull. Soc. Géol. Fr. 162, 79–90.

El Kadiri, K., Linares, A., Oloriz, F., 1992. La Dorsale calcaire rifaine (Marocseptentrional): Evolution stratigraphique et geodynamique durant leJurassique-Cretace. Notes Mem. Serv. Géol. Maroc. 336, 217–265.

El Kadiri, K., Fauzi, M., 1996. Les formations carbonates massives de la DorsaleCalcaire externe (Rif interne, Maroc), un exemple de plate-forme tidale souscontrole géodynamique durant le Trias moyen-Lias inférieur. Mines GéologiqueRabat 55, 79–92.

Fallot, P., 1937. Essai sur la géologie du Rif septentrional. Notes. Mém. Serv. Géol.Maroc. 40, 548.

Fedo, C.M., Nesbitt, H.W., Young, G.M., 1995. Unraveling the effect of potassiummetasomatism in sedimentary rocks and paleosols, with implications forpaleoweathering conditions and provenance. Geology 23, 921–924.

Fildes, C., Stow, D., Riahi, S., Soussi, M., Patel, U., Milton, J.A., Marsh, S., 2010.European provenance of the Numidian Flysch in northern Tunisia. Terra Nova22 (2), 94–102.

Floyd, P.A., Winchester, J.A., Park, R.G., 1989. Geochemistry and tectonic setting ofLewisian clastic metasediments from the Early Proterozoic Loch Maree Group ofGairloch, N.W. Scotland. Precambrian Res. 45, 203–214.

Folk, R.L., 1974. The natural history of crystalline calcium carbonate: Effect ofmagnesium content and salinity. J. Sediment. Petrol. 44, 40–53.

Frizon de Lamotte, D., 1985. La structure du Rif Oriental (Maroc). Rôle de latectonique longitudinale et rôle des fluides. Thèse Doct. Etat, Univ. Pierre etMarie Curie, Paris VI.

Frizon de Lamotte, D., Saint Bezar, B., Bracène, R., 2000. The two main steps of theAtlas building and geodynamics of the Western Mediterranean. Tectonics 19,740–761.

Garcia, D., Ravenne, C., Maréchal, B., Moutte, J., 2004. Geochemical variabilityinduced by entrainment sorting: quantified signals for provenance analysis.Sedimentary Geol. 171, 113–128.

Garcia-Duenas, V., Balanya, J.C., Martinez-Martinez, J.M., 1992. Miocene ExtensionalDetachment in the Outcropping Basement of the Northern Albora Basin (Betics)and their Tectonic Implications. Geo-Mar. Lett. 12, 88–95.

Gelard, J.P., 1969. Le flysch à base schisto-gréseuse de la bordure meridionale etorientale du massif de Chellata (Grande Kabylie, Algérie). Bulletin de la SociétéGéologique de France 7, 676–686.

Gübeli., A., 1982. Stratigraphische und sedimentologische Untersuchung derdetritischen Unterkreide-Serien des zentralen Rif (Marokko). Ph.D. Thesis,Univ. Zurich.

Gübeli, A., Hochuli, P.A., Wildi, W., 1984. Lower Cretaceous turbiditic sediment fromthe Rif chain (northern Morocco), palynology, stratigraphy setting. Geol.Rundsch. 73, 1081–1114.

H. El Talibi et al. / Journal of African Earth Sciences 100 (2014) 554–568 567

Guerrera, F., Loiacono, F., Grasso, M., 1986. Dati preliminari sulle suc-cessioni oligo-mioceniche ‘‘miste’’ affioranti lungo la Catena Betico-Maghrebide-Appenninomeridionale: una famiglia di flysch con evidenti implicazioni paleogeografiche epaleotettoniche. Boll. Soc. Geol. It. 105, 99–110.

Guerrera, F., Loiacono, F., Puglisi, D., Moretti, E., 1992. The Numidian Nappe in theMaghrebian chain: state of the art. Boll. Soc. Geol. It. 111, 217–253.

Guerrera, F., Martín-Algarra, A., Perrone, V., 1993. Late Oligocene-Miocene syn/lateorogenic successions in Western and Central Mediterranean chains from theBetic Cordillera to the southern Apennines. Terra Nova 5, 525–544.

Guerrera, F., Martin-Martin, M., Perrone, V., Tramontana, M., 2005.Tectonosedimentary evolution of the southern branch of western Tethys(Maghrebian Flysch Basin and Lucanian Ocean) on the basis of thestratigraphic record. Terra Nova 17, 358–367.

Guerrera, F., Martín-Algarra, A., Martín-Martín, M., 2012. Tectono-sedimentaryevolution of the ‘‘Numidian Formation’’ and Lateral Facies (southern branch ofthe western Tethys): constraints for central-western Mediterraneangeodynamics. Terra Nova 24, 34–41.

Handy, M.R., Schmid, S.M., Bousquet, R., Kissling, E., Bernoulli, D., 2010. Reconcilingplate-tectonic reconstructions of Alpine Tethys with the geological–geophysicalrecord of spreading and subduction in the Alps. Earth-Sci. Rev. 102, 121–158.

Harnois, L., 1988. The CIW index; a new chemical index of weathering. Sed. Geol. 55,319–322.

Herron, M.M., 1988. Geochemical classification of terrigenous sands and shalesfrom core or log data. J. Sediment. Petrol. 58, 820–829.

Hlila, R., 2005. Evolution tectono-sédimentaire tertiaire au front ouest du domained’Alboran (Ghomarides et Dorsale calcaire). Phd thesis, Univ. de Tétouan, 351pp.

Hoyez, B., 1989. Le Numidien et les flyschs oligo-miocènes de la bordure sud de laMéditerranée occidentale. Univ. Lille (France), Ph.D. thesis, pp 464.

Huntsman-Mapila, P., Kampunzu, A.B., Vink, B., Ringrose, S., 2005. Cryptic indicatorsof provenance from the geochemistry of the Okavango Delta sediments,Bostwana. Sed. Geol. 174, 123–148.

Ingersoll, R.V., Bullard, T.F., Ford, R.L., Grimm, J.P., Pickle, J.D., Sares, S.W., 1984. Theeffect of grain size on detrital modes: a test of the Gazzi-Dickinson point-counting method. J. Sediment. Petrol. 54, 103–116.

Ingersoll, R.V., Suczek, C.A., 1979. Petrology and provenance Neogene sand fromNicobar and Bengal fans. DSDP site 211 and 218. J. Sediment. Petrol. 49, 1217–1228.

Lallam, S., Sahnoun, E., El Hatimi, N., Hervouet, Y., De Leon, J.T., 1997. Mise enévidence de la dynamique de la marge téthysienne de 1’Hettangien à l’Aaléniendans la Dorsale Calcaire (Tetouan, Rif, Maroc). Comptes Rendus de l’Académiedes Sciences de Paris 324 (II), 923–930.

Lustrino, M., Duggen, S., Rosenberg, C., 2011. The Central-Western Mediterranean:Anomalous igneous activityin an anomalous collision tectonic setting. Earth-Sci.Rev. 104, 1–40.

Mattauer, M., 1960. Nouvelles données sur la « Dorsale calcaire » du Rif. ComptesRendus de l’Académie des Sciences de Paris 250, 374–376.

McLennan, S.M., Taylor, S.R., Eriksson, K.A., 1983. Geochemistry of Archean shalesfrom the Pilbara Supergroup, Western Australia. Geochim. Cosmochim. Acta 47,1211–1222.

McLennan, S.M., Hemming, D.K., Hanson, G.N., 1993. Geochimical approaches tosedimentation, provenance and tectonics. GSA Special Papers 284, 21–40.

McLennan, S.M., 2001. Relationships between the trace element composition ofsedimentary rocks and upper continental crust. Geochem. Geophys. Geosyst. 2,10–21.

McLennan, S.M., Taylor, S.R., Hemming, S.R., 2006. Composition, differentiation, andevolution of continental crust: constrains from sedimentary rocks and heatflow. In: Brown, M., Rushmer, T. (Eds.), Evolution and Differentiation of theContinental Crust. Cambridge University Press, pp. 92–134.

Michard, A., Negro, F., Saddiqi, O., Bouybaouene, M.L., Chalouan, A., Montigny, R.,Goffé, B., 2006. Pressure-temperature- time constraints on the Maghrebidemountain building: evidence from the Rif-Betic transect (Morocco, Spain),Algerian correlations, and geodynamic implications. C.R. Geosci. 338, 92–114.

Mongelli, G., Cullers, R.L., Muelheisen, S., 1996. Geochemistry of Late Cretaceous-Oligocenic shales from the Varicolori Formation, southern Apennines, Italy:implications for mineralogical, grain-size control and provenance. Eur. J.Mineral. 8, 733–754.

Mongelli, G., Critelli, S., Perri, F., Sonnino, M., Perrone, V., 2006. Sedimentaryrecycling, provenance and paleoweathering from chemistry and mineralogy ofMesozoic continental redbed mudrocks, Peloritani Mountains, Southern Italy.Geochem. J. 40, 197–209.

Mourabit, T., 1990. Etude des relations paléogéographiques et structurales de lanappe de Chouamat et de son autochtone relatif (unité de Ketama, région deTarguist, Rif central-Maroc). Ph.D. Thesis, Univ. Rabat.

Nesbitt, H.W., Young, G.M., 1982. Early Proterozoic climates and plate motionsinferred from major element chemistry of lutites. Nature 299, 715–717.

Nesbitt, H.W., Young, G.M., 1989. Formation and diagenesis of weathering profiles. J.Geol. 97, 129–147.

Nesbitt, H.W., Young, G.M., 1996. Petrogenesis of sediments in the absence ofchemical weathering: effects of abrasion and sorting on bulk composition andmineralogy. Sedimentology 43, 341–358.

Nesbitt, H.W., Young, G.M., McLennan, S.M., Keays, R.R., 1996. Effects of chemicalweathering and sorting on the petrogenesis of siliciclastic sediments, withimplications for provenance studies. J. Geol. 104, 525–542.

Olivier, P., 1984. Évolution de la limite entre Zones Internes et Zones Externes dansl’Arc de Gibraltar (Maroc-Espagne). Phd thesis, Univ. Paul Sabatier, Toulouse,229 pp.

Parfenoff, A., Pomerol, C., Tourenq, J., 1970. Les minéraux en grains. In: Méthodesd’études et détermination. Masson Ed, Paris, p. 575.

Perri, F., Cirrincione, R., Critelli, S., Mazzoleni, P., Pappalardo, A., 2008a. Clay mineralassemblages and sandstone compositions of the Mesozoic Longobucco Group(north-eastern Calabria): implication for burial history and diageneticevolution. Int. Geol. Rev. 50, 1116–1131.

Perri, F., Rizzo, G., Mongelli, G., Critelli, S., Perrone, V., 2008b. Zircon composition ofLower Mesozoic redbeds of the Tethyan margins in the Central-WesternMediterranean area. Int. Geol. Rev. 50, 1022–1039.

Perri, F., Critelli, S., Mongelli, G., Cullers, R.L., 2011a. Sedimentary evolution of theMesozoic continental redbeds using geochemical and mineralogical tools: thecase of Upper Triassic to Lowermost Jurassic M.te di Gioiosa mudstones (Sicily,Southern Italy). Int. J. Earth Sci. 100, 1569–1587.

Perri, F., Muto, F., Belviso, C., 2011b. Links between composition and provenance ofMesozoic siliciclastic sediments from Western Calabria (Southern Italy). ItalianJ. Geosci. 130, 318–329.

Perri, F., Critelli, S., Cavalcante, F., Mongelli, G., Dominici, R., Sonnino, M., De Rosa, R.,2012a. Provenance signatures for the Miocene volcaniclastic succession of theTufiti di Tusa Formation, southern Apennines, Italy. Geol. Mag. 149, 423–442.

Perri, F., Critelli, S., Dominici, R., Muto, F., Tripodi, V., Ceramicola, S., 2012b.Provenance and accommodation pathways of late Quaternary sediments in thedeep-water northern Ionian Basin, southern Italy. Sedimenatry Geol. 280, 244–259.

Perri, F., Critelli, S., Martìn-Algarra, A., Martìn-Martìn, M., Perrone, V., Mongelli, G.,Zattin, M., 2013. Triassic redbeds in the Malaguide Complex (Betic Cordillera –Spain): petrography, geochemistry, and geodynamic implications. Earth-Sci.Rev. 117, 1–28.

Perri, F., 2014. Composition, provenance and source weathering of Mesozoicsandstones from Western-Central Mediterranean Alpine Chains. J. Afr. Earth Sc.91, 32–43.

Perri, F., Borrelli, L., Critelli, S., Gullà, G., 2014. Chemical and minero-petrographicfeatures of Plio-Pleistocene fine-grained sediments in Calabria (southern Italy).Italian J. Geosci. 133, 101–115.

Perri, F., Otha, T., 2014. Paleoclimatic conditions and paleoweathering processes onMesozoic continental redbeds from Western-Central Mediterranean AlpineChains. Palaeogeogr. Palaeoclimatol. Palaeoecol. 395, 144–157.

Perrone, V., Martin-Algarra, A., Critelli, S., et al., 2006. ’’Verrucano’’ and’’Pseudoverrucano’’ in the central-western Mediterranean Alpine chains:palaegeographic evolution and geodynamic significance. In: Geology andActive Tectonics of the Western Mediterranean Region and North Africa. In:Chalouan, A., Moratti, G. (Eds.), . Geol. Soc. London Spec. Publ., 262, pp. 1–43.

Perrone, V., Perrotta, S., Marsaglia, K., Di Staso, A., Tiber, V., 2014. The oligoceneophiolite-derived breccias and sandstones of the Val Marecchia Nappe: insightsfor paleogeography and evolution of Northern Apennines (Italy). Palaeogeogr.Palaeoclimatol. Palaeoecol. 394, 128–143.

Pettijohn, F.J., Potter, P.E., Siever, R., 1972. Sand and Sandstone. Springer-Verlag,New York.

Potter, P.E., 1978. Significance and origin of big rivers. J. Geol. 86, 13–33.Potter, P.E., 1986. South America and a few grains of sand: Part 1– beach sands. J.

Geol. 94, 301–319.Puglisi, D., Carmisciano, R., 1992. Il Flysch di Algeciras (Oli- gocene-Miocene inf.?,

Cordigliera Betica): studio petrografi co-sedimentologico e confronto con altreunità torbiditiche della catena maghrebide. Boll. Acc. Gioenia Sci. Naturali diCatania 25 (340), 5–23.

Puglisi, D., Zaghloul, M.N., Maate, A., 2001. Evidence of sedimentary supply fromplutonic sources in the oligocene-miocene flyschs of the Rifian chain (Morocco):provenance and paleogeographic implications. Bull. Soc. Geol. It. 120, 55–68.

Raoult, J.F., 1974. Géologie du centre de la chaîne numidique (Nord duconstantinois, Algérie). Mémoires de la Société géologique de France 121, 1–163.

Roser, B.P., Coombs, D.S., Korsch, R.J., Campbell, J.D., 2002. Whole-rock geochemicalvariations and evolution of the arc-derived Murihiku Terrane, New Zealand.Geol. Mag. 139, 665–685.

Suter, G., 1980a. Carte structurale de la Chaîne rifaine au 1:500.000. Notes Mém.Serv. Géol. Maroc. 245b.

Suter, G., 1980b. Carte géologique du Rif au 1/500,000. Notes et Mémoires duService géologique du Maroc 245a.

Taylor, S.R., McLennan, S.M., 1985. The Continental Crust: Its Composition andEvolution. Blackwell Sciences Publication.

Thomas, M.F.H., Bodin, S., Redfern, J., Irving, D.H.B., 2010a. A constrained Africancraton source for the Cenozoic Numidian Flysch: implications for thepaleogeography of the western Mediterranean basin. Earth-Sci. Rev. 101,1–23.

Thomas, M.F.H., Bodin, S., Redfern, J., 2010b. Comment on: ‘‘European provenance ofthe numidian flysch in northern Tunisia’’ (Fildes et al., 2010). Terra 22 (6), 501–505.

Vitale, S., Ciarcia, S., Mazzoli, S., Zaghloul, M.N., 2011. Tectonic evolution of the‘Liguride’ accretionary wedge in the Cilento area, southern Italy: a record ofearly Apennine geodynamics. J. Geodyn. 51, 25–36.

Wildi, W., Nold, M., Uttinger, J., 1977. La Dorsale Calcaire entre Tetouan et Assifane(Rif interne, Maroc). Eclogae geol. Helv. 70, 371–415.

Wildi, W., 1983. La chaîne tello-rifaine (Algérie, Maroc, Tunisie): structure,stratigraphie et évolution du Trias au Miocène. Revue De GeologieDynamique Et De Geographie Physique 24, 201–297.

Zaghloul, M.N., 2002. La sédimentation silicoclastique Oligo-miocène de type«Flysch» dans le Rif, «Bassin des Flyschs» et «Zones Internes» (Rif, Maroc):

568 H. El Talibi et al. / Journal of African Earth Sciences 100 (2014) 554–568

évolution et corrélations à l’échelle de la Chaîne Maghrébide. Univ. Abdel MalekEssaadi, Thèse d’Etat, pp. 316.

Zaghloul, M.N., Guerrera, F., Tucker, M.E., El Moutchoun, B., Ouazani Touhami, A.,Puglisi, D., 2003. New petrographic and sedimentological data from EarlyCretaceous mixed succession (Flysch Basin Domain; Northern Rif, Morocco):provenance and paleogeography of the Mauretanian and Massylian sub-domains. 17 éme Colloque des Bassins Sedimentaires Marocains (CBSM),Rabat 2003, Abstr, pp. 153–155.

Zaghloul, M.N., Di Staso, A., El Moutchou, B., Gigliuto, L.G., Puglisi, D., 2005.Sedimentology, provenance and biostratigraphy of the Upper Oligocene-LowerMiocene terrigenous deposits of the internal «Dorsale Calcaire» (Rif, Morocco):

palaeogeographic and geodynamic implications. Bollettino della SocietàGeologica Italiana 124, 437–454.

Zaghloul, M.N., Di Staso, A., de Capoa, P., Perrone, V., 2007. Occurrence of upperBurdigalian silexite beds within the Beni Ider Flysch Fm. in the Ksar-es-Seghirarea (Maghrebian Flysch Basin, Northern Rif, Morocco): stratigraphiccorrelations and geodynamic implications. Bollettino della Società GeologicaItaliana 126, 223–239.

Zaghloul, M.N., Critelli, S., Perri, F., Mongelli, G., Perrone, V., Sonnino, M., Tucker, M.,Aiello, M., Ventimiglia, C., 2010. Depositional systems, composition andgeochemistry of Triassic rifted continental margin redbeds of Internal RifChain, Morocco. Sedimentology 57, 312–350.