Devonian to Lower Carboniferous Stratigraphy and Facies of the Moroccan Meseta: Implications for Palaeogeography and Structural Interpretation – a Project Outline

Becker & El Hassani A project outline

Devonian to Lower Carboniferous stratigraphy and facies of the Moroccan Meseta: implications for palaeogeography and structural interpretation – a project outline

R. Thomas BECKER & Ahmed EL HASSANI

1. Introduction al., Eds., 2013; HARTENFELS et al., Eds., 2018). The eastern Anti-Atlas is famous for its 1.1. Devonian stratigraphy internationally celebrated geological heritage The Devonian was the first system in which (e.g., EL HASSANI et al. 2017), but, as presented all chronostratigraphic units (series and stages) in this volume, there are equally important and were formally defined, producing a stable time fossil-rich localities in the Western Meseta and frame work for detailed international and Middle Atlas basement. interdisciplinary correlation (e.g., BECKER et al. 2012, 2020). This also applies to the main 1.2. Devonian plate tectonics part (Tournaisian, Viséan) of the Lower The Devonian plate tectonic configuration Carboniferous (e.g., DAVYDOV et al. 2012). has been controversial for a long time and this The most significant fossil groups that provide applies especially to the latitudinal position of an international high-resolution subdivision of Gondwana and Laurussia (= Laurentia + time are conodonts and ammonoids for the Baltica + Avalonia) and to the width of the pelagic facies realm, conodonts, brachiopods oceanic system between both supercontinents, and trilobites for the neritic realm, and variably named as western part of the miospores for terrestrial settings and for Prototethys, Palaeotethys, or the Variscan nearshore clastic sediments with high Oceans (FRANKE et al. 2017). The widely used terrigeneous influx. There are both regional term Rheic Ocean applies only to a specific and global zonation schemes, which part within the dynamic system; it closed supplement each other. Together with other during the Emsian, which was followed by the modern stratigraphic techniques, such as opening of the Rhenohercynian Ocean (e.g., Devonian global event, isotope, and sequence FRANKE 2000). Whilst palaeomagnetic data stratigraphy, it is now possible to establish and reconstructions (e.g., VAN DER VOO 1990; precise time frameworks for fossiliferous BACHTADSE et al. 1987; TAIT et al. 2000; sedimentary successions, which lie far beyond NANCE et al. 2012) postulated a very wide the past research (Fig. 1). This can now be Devonian ocean, palaeobiogeographic applied to regions with difficult outcrop comparisons between cratonic Gondwana and conditions and strong tectonic overprinting, Laurussia (e.g., ROBARDET et al. 1990; where stratigraphic progress has been slow. MCKERROW et al. 2000; GOLONKA 2007; One such example is the Moroccan Meseta, NAZIK & GROOS-UFFENORDE 2016), suggest a which, in terms of Devonian-Carboniferous narrow ocean, as depicted first in the Devonian stratigraphy, has long remained in the shadow continent distribution of HECKEL & WITZKE of the Anti-Atlas (e.g., EL HASSANI & TAHIRI, (1979). Occurrences of calcareous contourite Eds., 1999; EL HASSANI, Ed., 2004; BECKER et deposits in strongly condensed deeper-water

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settings (HÜNEKE 2006, 2007) agree with the Mrirt sucession (see BECKER et al. 1997; close-fit palaeogeographic reconstructions. BECKER & HOUSE 2000a). Based on the close similarity of German and Meseta Givetian reefs, EICHHOLT & BECKER 1.3. Prototethys palaeogeography (2016) suggested a ca. 3.000 km wide (N-S) A better understanding of the western “Variscan Sea”. It had no oceanic crust in a Prototethys evolution can be reached by a wide archipelago of crustal blocks and islands much finer (in terms of time resolution) and (BECKER et al. 2016d) ranging from the dynamic comparison of facies, faunal, floral, Moroccan Meseta in the South to a ribbon of and palaeogeographic characteristics of its southern European microplates. These were southern and northern shelf areas. These are represented, for example, by the Betic preserved in the moderately deformed, Cordillera and Catalonia of Spain, Menorca, fossiliferous, southern (= Meseta, SE Portugal) Sardinia, Sicily, and Calabria, as well as the Rif and northern external Variscides. An improved and Kabylie areas, which were then situated understanding of the varied and complex more easterly than today (“Palaeo-Adria” belt sedimentary and faunal successions of the of FRANKE et al. 2017). Clearly, the Meseta Meseta is the key to understand the dynamics faunas and facies developments play a of a seaway, which controlled the East-West significant role in this plate tectonic debate. moving oceanic water masses and, in the form The Devonian plate configuration is not of stepping stones, the North-South migration only crucial for the geodynamic understanding of biota. Rather enigmatic and incompatible of the Variscan Oceans and later orogeny, but with the sedimentary and palaeobiogeographic critical for the reconstruction of global record (e.g., ROBARDET et al. 1990; ROBARDET palaeoclimate, oceanic currents (e.g., BALBUS 2003; ERNST & RODRÍGUEZ 2010) are 2015), and paleobiogeography, including, for Devonian maps with a position of Morocco far example, the early dispersal of tetrapods and to the east and completely outside of the freshwater biota (e.g., YOUNG 1981, 2003 southern European/Variscan realm (e.g. BLIECK et al. 2007). Both equivocal and crucial DALZIEL et al. 1994, COCKS & TORSVIK 2002). is the Devonian plate tectonic position of Morocco. Many reconstructions (e.g., HOUSE 1.4. Devonian synsedimentary tectonics 1975; NEUGEBAUER 1988, SIMANCAS et al. The Middle Devonian to Lower 2006; GOLONKA 2007, VON RAUMER et al. Carboniferous was the time when Eovariscan 2009; PÉREZ-CACÉRES et al. 2017) place it tectonic events occurred throughout the slightly or far to the west of Iberia, directly Variscan oceans. This led to distinctively facing the Appalachian belt. Other authors different sedimentary and palaeoecological (e.g., HECKEL & WITZKE 1979; ZIEGLER 1989; patterns on separate, often closely adjacent MCKERROW et al. 2000; MATTE 2001) place crustal blocks, microplates, and on the the Moroccan Meseta just to the south of the marginal shelf sees. However, the lack of southern European Variscides. The latter view precise biostratigraphic dating for such is strongly supported by palaeobiogeographic movements and re-sedimentation events similarities (e.g. ROBARDET et al. 2000; hampered palaeogeographic and structural EICHHOLT & BECKER 2016) and the trans- reconstructions. Even further, it has been Variscan tracing of thin marker units from the claimed (TRIBOVILLARD et al. 2004; Meseta Devonian to southern France. An AVERBUCH et al. 2005) that Eovarican important example is given in our chapter on tectonics played a major role as a trigger mechanism for major marine eutrophication

10 Hassan II Academy of Science and Technology Frontiers in Science and Engineering - Vol. 10 - n° 1 - 2020 2 Becker & El Hassani A project outline events, such as the Kellwasser Events near the complex framework of structural units (e.g., Frasnian-Famennian boundary. This can be PIQUE & MICHARD 1981; PIQUE 1994; tested (and rejected) based on the precise MICHARD et al. 2010), each with a distinctive dating of Eovariscan uplift and erosion faunal and synsedimentary tectonic history. episodes and their relationships in time and There are both autochthonous and space with the Kellwasser Beds, which are allochthonous units, including nappes and partly well-developed in the Meseta. large olistostromes, that experienced There are links between synsedimentary significant westward displacement and re- tectonics and palaeobiogeography. More equal embedding during the “middle” Carboniferous facies and biota across the ocean system can be peak of deformation. The Western Meseta expected in times of tectonic quiescence, when clearly belong to an extensional tectonic similar depositional conditions could spread regime, from the basal Devonian well into the over large areas and when faunal exchanges Carboniferous (e.g., PIQUE 1975; BEAUCHAMP were not limited by deep and wide troughs or & IZART 1987; OUANAIMI et al. 2019). subaerial arc barriers. Fluctuating biodiversity However, Famennian metamorphism and gradients and peaks of endemism, for example compression has been suggested for the Midelt of (sub)tropical shallow-water corals, area (Middle Atlas; e.g., PIQUE & MICHARD ammonoids, and conodonts, are good 1981). Towards the Anti-Atlas in the South, indicators of stable or changing latitudinal and there is no evidence for a significant terrane or climatic differences. The Meseta localities facies boundary at the tectonically complex provide insights into latitudinally intermediate southern Variscan Front (e.g., JEANETTE & but tectonically influenced ecosystems at the PIQUE 1981; BAIDDER et al. 2008; FERONI et al. southern margin of the palaeotropics. 2010; RYTINA et al. 2013; Sub-Meseta Zone of MICHARD et al. 2010). 1.5. The Meseta Variscides A wide range of previous research dealt As part of the southern Variscides, with post-sedimentary tectonic styles, the main Hercynian Morocco includes the strongly structural framework, and tectonic models tectonized Palaeozoic successions north of the (summaries in PIQUE & MICHARD 1981, 1989; more or less stable cratonic part of NW PIQUE 1994, 2001; EL HASSANI & TAHIRI, Gondwana, the Anti-Atlas, which experienced Eds., 1994; EL HASSANI et al. 2003; MICHARD only moderate Upper Carboniferous folding et al. 2008, 2010). However, former attempts and faulting (e.g., BURKHARD et al 2006; TOTO to reconstruct the Devonian to Tournaisian et al. 2007). Sedimentary successions of the palaeogeographic evolution suffered badly Moroccan Meseta and of small tectonic from the lack of adequate biostratigraphic data windows within the Atlas Mountains or at its and poor international correlation of southern margin (Skoura region) are overlain successions. Examples are the rough by flat lying Mesozoic and Cenozoic strata. stratigraphic columns in HOEPFFNER et al. Widespread granites are related to post- (2005; subsequently recycled in other Variscan (Cenozoic) volcanism (MICHARD summary papers) and the many uncertainties 1976). There was considerable post-Variscan recognized in stratigraphic reviews, such as EL crustal shortening in the High Atlas since the HASSANI & BENFRIKA (1995, 2000) and Miocene (GOMEZ et al. 2000). Syn- and KAISER et al. (2007). A few modern (bed-by- postsedimentary tectonic movements (e.g., bed) studies and high-resolution PIQUE & MICHARD 1989; EL HASSANI & biostratigraphic data are available for some TAHIRI, Eds., 1994, 2000) resulted in a very sections and restricted time intervals.

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Fig. 1: Devonian chrono-, bio- (conodonts, ammonoid zonal key), and event stratigraphy.

But for the majority of successions, a revision of taxonomy and zonal assignments previous biostratigraphic data were according to the current state of the art. Our imprecise, poorly documented, based on studies intended to overcome these incipient, widely spaced sampling, or require shortcomings, involving also specialists for

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other fossil groups, and by concentrating on The Palaeozoic basement of the Middle key sections for individual structural units. Atlas is poorly exposed in small tectonic The applied schemes for chrono-, bio- windows, for example at Immouzer-du- (conodonts, ammonoids), and event Kandar S of Fez (e.g., CHARRIÈRE & stratigraphy are shown in Fig. 1. A wealth of RÉGNAULT 1989; our new chapter). new stratigraphic and biofacies results is Reworked Neoproterozoic and Lower presented in chapters that include as many Palaeozoic rocks, especially magmatic details as possible, such as bed-by-beds pebbles and the Devonian facies section logs, abundant outcrop photos, range development, differ significantly from other charts, fossil and microfacies plates. A refined Meseta regions but there are some similarities picture of palaeogeography and of Eovariscan with the nappes of the eastern Central Meseta. movements in time and space will emerge The principle palaeogeographic when the data from all individual successions configuration of the Meseta began in the are combined and correlated. upper Silurian, followed by the earliest Hercynian tectonic movements. Early 2. Structural units of the Meseta Palaeozoic Devonian sedimentation continued in most regions conformably from the Silurian 2.1. Main tectonic and palaeogeographic (Pridoli). The transition is characterized by a zones strong increase of calcareous deposition The Moroccan Meseta is constituted by the related to a decreasing amount of terrigenous Palaeozoic Plateau and its flat lying cover supply from the West African Craton in the between the Atlas system and Rif mountains South. This was accompanied by climatic (Figs. 2-3). The Middle Atlas divides this warming due to the motion of northeast domain into two areas: Gondwana into a warmer, southern subtropic The Western Meseta is located position. approximately between the cities of Rabat, Three palaeogeographic zones are Taza, Marrakesh and Essaouira. There are distinguished in the Moroccan Meseta. A three major Palaeozoic zones (massifs), the western carbonate platform zone (Western Massif Central, Rehamna, and Jebilet, and Meseta) was subdivided during the Lower some outcrops in the small valleys of the and Middle Devonian into several calcareous Atlantic coastal rivers (e.g., at the Oued Oum- ridges and adjacent, deeper-water troughs er-Rbia). These massifs are separated by with shales and rare calcareous intercalations. Mesozoic and Cenozoic areas, the Khouribga Biostromes and bioherms grew the and Gantour Phosphate plateau, Doukkala, borders of tectonically uplifted and emerged along and Chaouïa. Despite this cover, it is possible areas. A second, transitional zone, to establish stratigraphic and structural corresponding to eastern parts of the Central correlations and to reconstruct a common Moroccan Massif, is characterized by Palaeozoic history. differentiated facies in allochthonous and The Eastern Meseta consists also of autochthonous series. Reef growth was rather Palaeozoic regions and a Mesozoic-Cenozoic localized. The third zone, the Eastern Meseta, cover, but outcrops are smaller than those of shows turbiditic and pelagic sedimentation the western part. It is composed of the Midelt with siliciclastics derived both from distant area, and the areas of Zekkara, Jorf Ouezzène, African shields and from emerged areas (e.g., Jerada Debdou, and Mekkam. The small ACOTTO et al. 2018). outcrop make correlations more difficult.

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Fig. 2: The Meseta Domain and adjacent Anti-Atlas foreland; structural map of the Variscan Meseta Domain, from MICHARD et al. (2008, fig. 3.16), modified after PIQUE & MICHARD (1989), OUANAIMI & PETIT (1992), HOEPFFNER et al. (2005), BAIDDER et al. (2008), SOULAIMANI & BURKHARD (2008), MICHARD et al. (2010), and TAHIRI et al. (2010). White: Mesozoic–Cenozoic cover.

2.2. Investigated sedimentary-tectonic affected by Famennian (367 ma), not Silurian units of the Western Meseta magmatism (TAHIRI et al. 2010). It does not The Western Meseta is characterized by include Devonian sediments and, therefore, folding and metamorphic events of the Upper was not re-studied during our project. Carboniferous main Hercynian/Variscan Various authors, who have worked in the orogeny. However, Eovariscan folding Palaeozoic of the Meseta, agreed to divide it (Upper Tournaisian, “Eovariscan 2 Events of into distinctive sedimentary-structural units. MICHARD et al. 2008) is observed in the Their Devonian and Lower Carboniferous eastern Azrou–Khenifra Basin and affected stratigraphy has been reviewed by ZAHRAOUI Cambrian–Ordovician formations. This (1994), FADLI (1994a, 1994b), EL HASSANI & suggests an initial continuity with the Eastern BENFRIKA (1995, 2000). The following Meseta (MICHARD et al. 2010). In the northern regions were part of our project (Figs. 2-5): part, the Sehoul Block is regarded as a Caledonian block (e.g., PIQUÉ, 1979; EL 2.2.1. Coastal block (“Môle côtier”) HASSANI, 1991) but the re-dating of its It is located in the western part of the granitoids showed that this terrane was western Meseta and includes Palaeozoic

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outcrops W of the Western Meseta Shear region large open folds (at kilometer scale), Zone (PIQUE et al. 1980), such as the coastal with locally low cleavage development in the plateau and western parts of the Rehamna and fold-axis. This moderately deformed zone Jebilet massifs. The successions consist extends southward up to the westernmost mainly of Cambrian to Upper Devonian High Atlas Palaeozoic Massif (CORNÉE, sediments. Carboniferous outcrops were 1989). We logged and re-sampled the Oulad discovered only in boreholes of the Doukkala Abbou (Douar Zrahna) section (EL KAMEL Basin, which is a Silurian–Devonian basin 2004), concentrating on the dating of Middle beneath the Mesozoic cover (ECHARFAOUI et Devonian reef drowning phases and overlying al. 2002). Deformation occurred during the deeper-water Upper Devonian strata. Main Variscan-Phase, which gives in this

Fig. 3: Hercynian Geological map of Central Morocco (FADLI et al., 2008): 1. Cambrian (a: grauwackes, siltstones and quartzites; b: trachyandesites and rhyolites); 2. Cambrian-Ordovician (Zain quartzites and Phyllades of Sehoul Block); 3. Lower Ordovician; 4. Upper Ordovician; 5. Silurian; 6. Lower-Middle Devonian; 7. Undifferentiated Devonian; 8. Upper Devonian and Tournaisian; 9. Lower Visean ; 10. Middle, Upper Visean and lower Namurian; 11. upper Namurian – lower Westphalian ; 12. upper Westphalian ; 13. Stephanian – Permian ; 14. Triassic.

2.2.2. Rabat-Tiflet Zone recalculated the age of this supposed The Rabat-Tiflet Zone is a narrow band in Caledonian granite as 609 ± 4 Ma in age, and, tectonic contact with the Sehoul block (Fig. consequently, re-interpreted it as Precambrian 6). It includes the so-called “Taicha Granite”, basement. The Devonian is represented in which was attributed to the Ordovician by western part of the Rabat-Tiflet Zone by CHARLOT et al. (1973). TAHIRI et al. (2010) fossiliferous Lochkovian to Emsian strata of

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the Oued Bou Regreg region, which have bearing limestones at Sidi Jilali and Sidi Radi been studied by numerous authors (last (see IZART & VIESLET 1988). review and detailed conodont biostratigraphy by BENFRIKA et al. 2007). We concentrated in 2.2.4. Oued Cherrat Zone our project on the Devonian and Lower The Oued Cherrat is a narrow, ca. N-S Carboniferous of Chabat-el-Harcha (EL running Devonian outcrop band that forms HASSANI 1991) and on the Tiflet region (Oued the western border of the Sidi-Bettache Basin Tiflet and the reefal limestones of the Tiflet (Fig. 7). It follows a palaeogeographical ridge Quarry). and is best characterized by its Emsian and Givetian, economically important reef 2.2.3. Sidi Bettache Basin limestones. Eovariscan reworking, reef This basin was defined by PIQUÉ (1979, destruction, and re-deposition were very 1981). It stretches SSE of the Rabat-Tiflet prominent. The first chapter of this volume Zone (Fig. 4) and comprises a thick, partly deals with a detailed review and many new flyschoid, siliciclastic Famennian to data concerning its biostratigraphy and Tournaisian succession. Only some intervals synsedimentary tectonic movements. We are rich in fossils. We concentrated on these, concentrated, from North to South, on four for example on the goniatite-rich Tournaisian successions: Aïn Khira, Aïn-ad-Dakhla to of Aïn Hallaouf/Aïn Aouda (S of Rabat; Cakhrat-ach-Chleh, Aïn-Al-Aliliga to BOLLELI et al. 1953) and on the conodont- Cakhrat Mohammed ben Brahim, and Aïn-as- Seffah.

Fig. 4: General structural map of Central Morocco (in FADLI et al. 2008): 1. Variscan granites, 2. Cambrian to Middle Devonian, 3. Carboniferous basins (Upper Devonian to lower Westphalian), 4. Continental sediments (upper Westphalian to Permian), 5. Axial direction of major folds, 6. Thrust contacts, 7. Main Faults.

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Fig. 5: Geographic position of sampled Meseta/Atlas regions. 1. Rabat-Tiflet Zone, 2. Tiddas region, 3. Oulmes region, 4. El Hammam Block, 5. Immouzer-du-Kandar, 6. Azrou, 7. Jebel ben Arab, 8. Bou Khedra-Bou Trou, 9. Mrirt autochthon at Dechra Ait Abdallah, 10. Mrirt allochthon, 11. Khénifra region, 12. Oued Aricha, 13. Western Mdakra Massif, Benhamed region, 14. Khatouat Massif (Jennabia, Biar Setla), 15. Al Attamna, 16. Ben Slimane Region, 17-18. Oued Cherrat Zone, 19. Western Sidi Bettache Basin (Aïn Aouda), 20. Central Sidi Bettache Basin (Sidi Jilali, Sidi Radi), 21. Coastal Block (Oulad Abbou), 22. Western Rehamna (Mechra-ben-Abbou region), 23. Eastern Rehamna (Foum-el-Mejez), 24. Eastern Jebilet, 25. Western Jebilet (Jebel Ardouz), 26. Mzoudia (El Moussira), 27. Western High Atlas (Talmakent), 28. Skoura region just S of High Atlas, 29. Tinerhir region, Southern Variscan Front, 30. Tinejdad allochthon (Bou Tisdafine SW, Oued Ferkla).

2.2.5. Ben Slimane region 2.2.6. Al Attamna Devonian outcrops are more restricted in The Al Attamna region lies just S of the the basin of Ben Slimane, which lies just W Oued Cherrat (Figs. 3, 7) and is characterized of the Oued Cherrat (Fig. 7). We re-studied by a continuation of its general facies and by two areas, the Lower Devonian and the re-appearance of thick Emsian and ammonoid-rich uppermost Famennian just Givetian reefs. We re-sampled two sections: South of Ben Slimane (near Aous bel of BENFRIKA & BULTYNCK (2003), Sidi Fassi/Chaabat Hamira), and, to the North, the Ahmed Lemdoun and Sidi Mohammed Lower Devonian limestones of Bled Besbass Smaine (see EICHHOLT & BECKER 2016), with (ZAHRAOUI 1991). a second focus on Eovariscan breccia beds.

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Fig. 6: The Sehoul Block and Rabat–Tiflet Fault Zone (RTFZ) in the eponymous regions, after EL HASSANI (1994a, 1994b), modified after TAHIRI et al. (2010) who use the name of “Bou Regreg Corridor” for the RTFZ. A. Sketch map with location of B–C cross-sections. B. Cross-section within the Sehoul Block. C. Cross-section of the RTFZ. S1: metamorphic foliation; or: Ordovician; s: Silurian; di, dm, ds: Lower, Middle, Upper Devonian; hT: Tournaisian; hV: Visean.

2.2.7. Khatouat Massif and olistolites are wide-spread, for example at The tectonically complex Palaeozoic of Chabet-el-Baya S of the Al Attamna reefs the Khatouat Massif lies East of the Al (FADLI 1990, 1994a). Attamna and forms the southern continuation of the Sidi Bettache Basin (FADLI 1990; Figs. 2.2.8. Benhamed region 3, 5). Siliciclastics dominate but there are The Devonian and LowerCarboniferous of strongly tectonized and largely reworked the Benhamed region (Figs. 3-5), the western Middle Devonian reefs, which we studied at and southern parts of the Mdakra Massif Jennabia and Biar Settla (EICHHOLT & (“Chaouï sud”), has somewhat been BECKER 2016). Eovariscan conglomerates neglected since the pioneer monograph by

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TERMIER & TERMIER (1951). We logged and 2.2.9. Zaer Ridge re-sampled the pelagic, ammonoid-rich Devonian is exposed in the northwestern Famennian basin of the Oued Aricha (NE of limb of the Khouribga-Oulmes Benhamed) and the deeper-water Givetian to Anticlinorium, East of the Sidi Bettache Frasnian of Dhar Cheikh el Mfaddel, Zwayir, Basin, along the ENE to NE Zaer fault strip and Boudouda (NNW of Benhamed). In the (ZAHRAOUI, 1991). This zone extends from latter section, neritic limestone with rich Sibara in the Southwest to the South of Tiddas foraminifers overlying Eovariscan breccias (Fig. 8). Lower and Middle Devonian rocks proved to be of Viséan age (det. P. COZAR). appears mostly as tectonic lenses or The Lower Devonian, including thick Emsian redeposited blocks within thick Famennian- reefs, requires more work. Tournaisian breccia and olistolite units (CHAKIRI & TAHIRI 2000). Strata in these outcrops are folded and affected by regional metamorphism, to which a contact metamorphism is superposed on the northwestern side of Zaer Granite (Fig. 8). We conducted some new work on the stratigraphy and microfacies in the most easily accessible outcrops of Sidi Ahroun (= Jebel Hadid, S of Tiddas, e.g., ALBERTI 1969).

2.2.10. Oulmès Zone The Devonian to the NNW of Oulmès belongs to the northern part of the Khourigba- Oulmès Anticline (Fig. 8). It is characterized by alternating neritic and fully pelagic sediments, with an important Givetian-lower Frasnian reefal episode (GENDROT 1970). Our detailed logging and sampling concentrated on the Eifelian-Frasnian, on the well-exposed Devonian-Carboniferous transition of Aïn

Jemaa (KAISER et al. 2007), and on the Fig. 7: Geology of the Benahmed, Ben Slimane, Oued adjacent, goniatite-rich Bou Keziam section Cherrat, Al Attamna, and western Sidi Bettache Basin regions (FADLI et al., 2008); 1. Cambrian (a: (COGNEY 1967). Thick, Lower Carboniferous grauwackes, siltstones and quartzites; b: (pre-Viséan) Eovariscan breccias were trachyandesites and rhyolites); 2. Cambrian- studied on the northern slope of Aïn Jemaa Ordovician (Zain quartzites and Phyllades of Sehoul ridge, at Ta´araft. Block); 3. Lower Ordovician; 4. Upper Ordovician; 5.

Silurian; 6. Lower-Middle Devonian; 7. Undifferentiated Devonian; 8. Upper Devonian and 2.2.11. El Hammam Zone Tournaisian; 9. Lower Visean ; 10. Middle, Upper The Devonian exposed around the small Visean and lower Namurian; 11. upper Namurian – track up to Moulay El Hassane sanctuary, NE lower Westphalian ; 12. upper Westphalian ; 13. of Oulmès, was first summarized by COGNEY Stephanian – Permian ; 14. Triassic. (1967). It belongs to a different structural and

facies unit, for example without reefs, the El

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HammanHammanHammanHamman Zone ZoneZone ( T((ZoneTTAHIRIAHIRIAHIRI ( T& &&AHIRI H HHOEPFFNEROEPFFNEROEPFFNER & HOEPFFNER 1988; 1988;1988; 1988;BouBouBou Alzaz AlzazAlzazBou region Alzazregionregion S region SSWWW of ofof SMeknes MeknesMeknesW of Meknes ( T((TTAHIRIAHIRIAHIRI ( T& &&AHIRI & TTTAHIRIAHIRIAHIRI T 1994). AHIRI1994).1994). 1994). We We We logged loggedlogged We logged and and and sampled sampled sampled and sampled the thethe LtheLLAZREQAZREQAZREQ L AZREQ 1988;1988;1988; L1988;LLAZREQAZREQAZREQ L AZREQ 1999).1999).1999). 1999). There,There,There, There, w w wee e we MiddleMiddleMiddle-MiddleUpper--UpperUpper - Upper Devonian Devonian Devonian Devonian pelagic pelagic pelagic pelagic facies facies facies faciesconductedconductedconducted conducted limited limitedlimited limitednew newnew field fieldfield new work, work,work, field with withwork,with some somesome with some (L((LLAZREQAZREQAZREQ(L 1990)AZREQ 1990)1990), , ,which1990) whichwhich ,yielded whichyieldedyielded yielded a a anew, new,new, unique, a unique,unique, new, unique, samplingsamplingsampling sampling forforfor conodont, conodont, conodont,for conodont, microfacies, microfacies, microfacies, microfacies, and and and and smallsmallsmall-sized--sizedsmallsized Frasnian- Frasniansized Frasnian Frasnian ammonoid ammonoid ammonoid ammonoid fauna. fauna. fauna. Thefauna. The The Thebrachiopodsbrachiopodsbrachiopods brachiopods in inin the the the Lower/Middle in Lower/Middle Lower/Middle the Lower/Middle Devonian Devonian Devonian Devonian FrasnianFrasnianFrasnianFrasnian-Famennian--FamennianFamennian-Famennian transition transition transition transition is is is exposed, exposed, exposed, is exposed, ofofof Ayn Ayn Ayn ofAzza AzzaAzza Ayn (= (= (=Azza Bou BouBou (=Alzaz AlzazAlzaz Bou-South). --AlzazSouth).South).- South).We WeWe noted notednoted We noted too.too.too. too. thethethe rare rare rarethe occurrence occurrence occurrence rare occurrence of of of transported transported transported of transported reefal reefal reefal reefal TheTheThe El ElEl TheHamman HammanHamman El Hamman Zone ZoneZone continues continuescontinuesZone continues for forfor quite quitequite for quitecoralscoralscorals in coralsinin the thethe Givetian. Givetian.inGivetian. the Givetian. somesomesome distance distancesome distance distance to to to the the the NNW to NNW NNW the and NNW and and reaches reaches reaches and reaches the the the the

Fig.Fig.Fig. 8: 8: 8: Geological Fig.GeologicalGeological 8: Geological map map map of of of the map the the Zaer Zaer Zaerof the Ridge Ridge Ridge Zaer ( F ( ( RidgeFFADLIADLIADLI et (etetF al.,ADLI al., al., 2008): 2008): 2008):et al., 1. 1. 2008):1. Cambrian Cambrian Cambrian 1. Cambrian (a: (a: (a: grauwackes, grauwackes, grauwackes, (a: grauwackes, siltstones siltstones siltstones siltstones and and and and quartzites;quartzites;quartzites;quartzites; b: b:b: trachyandesites trachyandesitestrachyandesites b: trachyandesites and andand rhyolites); rhyolites);rhyolites); and rhyolites); 2. 2.2. Cambrian CambrianCambrian 2. Cambrian-Ordovician--OrdovicianOrdovician-Ordovician (Zain (Zain(Zain quartzites quartzitesquartzites (Zain quartzites and andand Phyllades PhylladesPhyllades and Phyllades of ofof Sehoul SehoulSehoul of Sehoul Block);Block);Block); 3. Block); 3.3. Lower LowerLower 3. Ordovician; Ordovician;Ordovician;Lower Ordovician; 4. 4.4. Upper UpperUpper 4. Ordovician; Ordovician;Ordovician;Upper Ordovician; 5. 5.5. Silurian; Silurian;Silurian; 5. Silurian;6. 6.6. Lower LowerLower 6.-Middle-- MiddleMiddleLower Devonian;- MiddleDevonian;Devonian; Devonian; 7. 7.7. Undifferen UndifferenUndifferen 7. Undifferentiatedtiatedtiated tiated Devonian;Devonian;Devonian;Devonian; 8. 8.8. Upper UpperUpper 8.Devonian DevonianDevonian Upper Devonian and andand Tournaisian; Tournaisian;Tournaisian; and Tournaisian; 9. 9.9. Lower LowerLower 9. Visean Visean ViseanLower ; ;10.Visean; 10.10. Middle, Middle,Middle, ; 10. UpperMiddle, UpperUpper Visean ViseanVisean Upper and andViseanand lower lowerlower and Namurian; Namurian;Namurian; lower Namurian; 11.11.11. upper upperupper11. Namurian NamurianNamurian upper Namurian – – –lower lowerlower Westphalian – WestphalianWestphalian lower Westphalian ; ;12.; 12.12. upper upperupper ; 12. Westphalian WestphalianWestphalian upper Westphalian ; ;13.; 13.13. Stephanian StephanianStephanian ; 13. Stephanian – – –Permian PermianPermian – Permian; ;14.; 14.14. Triassic. Triassic.Triassic. ; 14. Triassic.

2.2.122.2.122.2.12. .2.2.12.Azro AzroAzrouuu-. Khénifra--AzroKhénifraKhénifrau-Khénifra Basin BasinBasin; ;;AzrouBasin AzrouAzrou; area Azrouareaarea arearelatively relativelyrelativelyrelatively complete completecomplete complete stratigraphic stratigraphicstratigraphic stratigraphic studies studiesstudies .studies ..T TThehehe . The AccordingAccordingAccordingAccording to to to B BBOUABDELLIOUABDELLIOUABDELLI to BOUABDELLI &&& PP PIQUÉIQUÉIQUÉ& PIQUÉfaunalfaunalfaunal faunal content content content content andandand facies facies faciesand facies development development development development (1990)(1990)(1990), (1990),, the the the ""Azrou," AzrouAzrou the -"Khénifra-Azrou-KhénifraKhénifra-Khénifra CarboniferousCarboniferousCarboniferous Carboniferous provideprovideprovide provide important important important important clues clues clues concerningclues concerning concerning concerning the the the the BBBasinasinasin”” ”B ( Fig.((asinFig.Fig. ” 9 9 9)( ))Fig. developed developed developed 9) developed an anan internal internalinternal an internal thrust thrustthrust thrustrelationshiprelationshiprelationship relationship with withwith autochthonous autochthonous autochthonouswith autochthonous Meseta MesetaMeseta Meseta and andand and frontfrontfront thatthatfrontthat overlaps overlapsoverlapsthat overlaps the the the eastern eastern eastern the eastern Meseta Meseta Meseta Meseta of of of Anti AntiAnti of -Atlas--AtlasAtlasAnti regions. -regions.regions.Atlas regions. MoroccoMoroccoMoroccoMorocco, ,,with withwith west ,westwest with verg verg vergwestenceenceence verg. ..At AtAtence the thethe. end At endend the of ofof end ofIn InIn the thethe Azrou AzrouAzrouIn the Nappe, Azrou Nappe,Nappe, Nappe,i niinn the thethe close closeclosein the vicinity vicinityvicinity close vicinity of ofof of thethethe Devonian Devonian Devonianthe Devonian, ,, the the the basin basin basin, the was was basinwas bound boundbound was bybound by by two two two by Azrou, twoAzrou,Azrou, Azrou, faciesfaciesfacies facies changes changes changes changes and and and the the the and conodont conodont conodont the conodont NENENE-SW--SWSWNE running,running,running,-SW running, deepdeepdeep transcurrenttranscurrentdeeptranscurrent transcurrent faults.faults.faults. faults.stratigraphystratigraphystratigraphy stratigraphy of ofof Devonian DevonianDevonian of Devonian outcrops outcropsoutcrops outcrops were werewere first firstfirstwere first TheseTheseThese authors These authors authors authors defined defined defined defined a a a dextral dextral dextral a dextral shear shear shear zone zoneshear zone, ,, zonestudiedstudiedstudied, studied in in in detail detail detail in by detailby by B BBOHRMANNOHRMANN OHRMANN by BOHRMANN & && F FFISCHERISCHERISCHER & F ISCHER wherewherewhere thewhere the the sedimentation sedimentationsedimentation the sedimentation was waswas controlled controlledcontrolled was controlled by by by (1985). (1985).(1985). by (1985). We We We re re re - Wesampled--sampledsampled re-sampled their their their localities localities localities their localities Bou Bou Bou Bou laterallaterallateral movementlateral movementmovement movementss s of ofof synsedimentary synsedimentarysynsedimentarys of synsedimentary faults faultsfaults faultsIghialIghialIghial and andIghialand Bab BabBab and-el--elel- BabAri--AriAri -at elatat even- evenArieven atfiner finerfiner even resolution, resolution,resolution, finer resolution, andandand tiltingtiltingtiltingand tilting blocks blocks blocks . blocks.. T T Thehehe .Upper UpperUpper The Upper DevonianDevonianDevonian Devonian––– withwithwith– some somesomewith focus focusfocussome o oonfocusnn the thethe numerous onumerousnumerousn the numerous Eovariscan EovariscanEovariscan Eovariscan LowerLowerLower CarboniferousLower CarboniferousCarboniferous Carboniferous period periodperiod is period isis characterized characterizedcharacterized is characterized brecciabrecciabreccia brecciabed bedbeds.s.s. beds. bybyby sedimentarysedimentarysedimentaryby sedimentary breaks, breaks, breaks, breaks, olistostromesolistostromesolistostromes olistostromes and and and andFurther FurtherFurtherFurther to to to the the the to SW, SW, SW, the we we weSW, restudied restudied restudied we restudied and and and and gravitygravitygravity gravitynappes nappesnappes nappesthat thatthat were werewere that embedded embeddedembeddedwere embedded in inin upper upperupper in uppersampledsampledsampled sampled the the the Devonian Devonian Devonian the Devonian of of of Bou Bou Bou of Khedra Khedra Khedra Bou Khedra (Bou (Bou (Bou (Bou ViseanViseanVisean-ViseanNamurian--NamurianNamurian-Namurian shales shalesshales. ..shalesEven EvenEven .i fiiEven ffwe wewe are areareif wenot notnot are Khadra,notKhadra,Khadra, Khadra, e.g., e.g.,e.g., B BBOUABDELLI e.g.,OUABDELLIOUABDELLI BOUABDELLI 1994), 1994),1994), which1994), whichwhich ends whichendsends ends yetyetyet sure suresureyet about aboutabout sure the thetheabout origin originorigin the of originofof the thethe gravitational gravitationalofgravitational the gravitationallylyly withwithwithly awith an ann angular angularangular an angular unconformity unconformity unconformity unconformity between between between between transportedtransportedtransportedtransported material, material,material, material, the the the existence existence existence the existence of of of ent ent entire ireire of entEmsianEmsianEmsianire Emsian limestones limestoneslimestones limestones and andand (?Upper) (?Upper)(?Upper) and (?Upper) Tournaisian TournaisianTournaisian Tournaisian seriesseriesseries within serieswithinwithin withinnappes nappes nappes nappes allows allowsallows allows us us us to to to elaborate elaborateus elaborate to elaborate

20 Hassan II Academy of Science and Technology Frontiers in Science and Engineering - Vol. 10 - n° 1 - 2020 121212 12 Becker & El Hassani A project outline

shales. It provides important evidence for the stratigraphic, faunal and microfacies data for Eovariscan 2 Phase of MICHARD et al. (2008). the allochthonous Devonian and basal Carboniferous East and South of Mrirt, with a 2.2.13. Ziar-Mrirt Nappe focus on the sections Anajdam (e.g., LAZREQ The Ziar-Azrou Nappe overlaps in the NW 1999) and Gara de Mrirt (= Bou Ounebdou; the Azrou Nappe (Fig. 9). Our second detailed e.g., LAZREQ 1999; WALLISER et al. 2000; chapter provides a review and many new BECKER & HOUSE 2000a).

Fig. 9: Geological map of the eastern part of Central Morocco (Azrou-Khenifra Basin; FADLI et al., 2008): 1. Cambrian (a: grauwackes, siltstones and quartzites; b: trachyandesites and rhyolites); 2. Cambrian-Ordovician (Zain quartzites and Phyllades of Sehoul Block); 3. Lower Ordovician; 4. Upper Ordovician; 5. Silurian; 6. Lower- Middle Devonian; 7. Undifferentiated Devonian; 8. Upper Devonian and Tournaisian; 9. Lower Visean; 10. Middle, Upper Visean and lower Namurian; 11. upper Namurian – lower Westphalian; 12. upper Westphalian; 13. Stephanian – Permian; 14. Triassic.

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Further to SE, large allochthonous Devonian turbidite basin, overlain by Upper Devonian outcrops re-appear in the Ziar Devonian sandstones, is exposed WNW of (Ziyyar) region (e.g., WALLISER et al. 1995). Azrou, at the Jebel ben Arab (Fig. 9). We We conducted bed-by-bed sampling for logged and sampled the section published by conodonts, foraminifers, and microfacies in LAZREQ (1990) in finer detail. the Emsian to Frasnian and middle-upper Famennian intervals. We dated precisely 2.2.16. Middle Atlas Basement (Immouzer- local unconformities, Eovarican slumping du-Kandar) units, and also focused on global event Our third detailed chapter presented here intervals, such as the Kellwasser Crises, deals with the unique Devonian at Immouzer- Annulata and Dasberg Events. du-Kandar (Figs. 2, 5), a tectonic window into Principally the same Devonian facies and the Middle Palaeozoic of the Middle Atlas faunas re-appear as clasts in massive Upper South of Fes. Our studies built on the previous Viséan olistolites, which belong to the thick research by CHARRIÈRE & RÈGNAULT (1989), flysch succession above the shallow-water CYGAN et al. (1990), and others. limestones of the Jebel Tabainout (e.g., MULLIN et al. 1976). This unit lies outside the 2.2.17. Rehamna Ziar-Azrou Nappe and belongs to the Kasba In the Rehamna, Devonian formations are Tadla-Azrou Anticline. represented by variable facies in distinctive zones. Despite the studies by a range of 2.2.14. Western Azrou-Khénifra Basin geologists (e.g., MICHARD, Ed., 1982; EL There are numerous fossiliferous HASSANI & EL KAMEL 2000; EL KAMEL Devonian outcrops to the W of the Ziar-Mrirt 2004), the age of formations and the dating of Nappe, from the Jebel Bouchot to the Dechra- facies changes and Eovariscan reworking and Aït-Abdallah (or Agarad-n-Azdaїt) region, re-deposition episodes still lacked precision. W/NW of Mrirt (Fig. 9). Pioneer stratigraphic Our work concentrated on Mechra ben work on the Palaeozoic was done by TERMIER Abbou (GIGOUT 1951, 1955) and its fine & TERMIER (1970) and TERMIER et al. (1975). reefs, overlain by Famennian quartzites with The successions are also part of allochthonous brachiopods, and on the supposedly units (nappes) but they reflect a complex contemporaneous non-reefal limestones of palaeogeography in terms of biofacies and Foum-el-Mejez, which are followed by floras (GROBE 1997) that differs significantly brachiopod-rich siltstones. Not very from the Azrou and Ziar-Mrirt sections. For successful spot samples for conodonts and example, there a thick reefs and important microfacies were taken in the Lower plant shales (e.g., PRESTIANNI et al. 2012). So Devonian of Sakhra et Taïra to the SE, which far, we concentrated on sections with reefs is characterized by very early slumping and (Awajgal, Amdawar) and took spot samples re-sedimentation events (EL KAMEL et al. from Famennian strata (e.g., at Titar Oumjel), 1992). In addition, we examined the reworked in order to complement the unpublished Palaeozoic blocks within the thick, M.Sc. Thesis of GROBE (1993). supposedly “Autunian” conglomerates at Koudiat-ed-Diab (HOLLARD et al. 1982). 2.2.15. Jebel ben Arab Another distinctive Devonian succession, 2.2.17. Jebilet: Eastern Jebilet with yet another facies development, from The Jebilet Massif is a tectonically pelagic Lower Devonian shales to a Middle complex Palaeozoic structure, which thick,

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siliciclastic main parts reflect the opening of 2017), somewhat to the South of the main, W- an Upper Devonian-Lower Carboniferous E trending Jebilet outcrop belt basin (DELCHINI et al. 2018). Fossiliferous Devonian strata are mainly exposed in the eastern Jebilet (e.g., Bou Marhara and Smaha). They correspond to Lower Devonian allochthonous or para-autochthonous series (HUVELIN 1977; TAHIRI 1982). The litho- and biofacies shares similarities with the Skoura region, especially in the presence of griotte limestones with rich upper Emsian goniatites (anarcestids), and with East Central Morocco (Azrou-Khenifra zone). We logged and

sampled the Lochkovian to Emsian at Jaidet and examined the conglomeratic Fig. 10: Strongly dolomitized, stromatoporid or unconformity at the base of the overlying stromatolite “ghost” from the top of the Khemis-n´Ga Viséan carbonate platform. Formation (probably lower Emsian).

2.2.18. Mzoudia (Jebel Ardouz) The western Jebilet Formations are exposed in the Skhirat Unit and mainly in Mzoudia (Jebel Ardouz). The Devonian belongs to a large thrust slice, which stratigraphy has been synthesized by TAHIRI (1982). However, our new data led to an important age revision for the reddish conglomerate at the base. The Eifelian- Givetian and Famennian strongly resemble the Mechra ben Abbou succession. However, Fig. 11: Post-sedimentary (?Eovariscan), polymict there is only a relatively thin biostrome that breccia encrusted unconformably and very locally on was truncated by Famennian brachiopod- the Lower Devonian Khemis n`Ga carbonate platform bearing white quartzites. (preserved in a minor depression on the main slope of the outcrop). Most particles are angular clasts of orange 2.2.19. Haouz (El Moussira) to reddish dolomites, partly with preserved crinoid remnants, sitting in a calcarenitic to dark and partly GAILLET (1986) suggested that a Middle laminated limestone matrix (picture width = 25 cm). Devonian to Tournaisian succession, with a reefal interval overlain by a siliclastic basin, 2.2.20. Safi region is developed at El Moussira in the Haouz After an outcrop gap West of the western region S of Marrakesh. Based on rare Jebilet margin, upper Silurian and Devonian conodonts, this claim could be firmly rejected limestones resurface from the post- by ABOUSSALAM et al. (2017), who Palaeozoic cover in the Safi region, at Khemis documented top-Viséan conodonts from the n´Ga (BEUN et al. 1992; BULTYNCK & supposed Middle Devonian. However, SARMIENTO 2003). We re-sampled the rather Famennian strata with conodonts occur thic, mostly coarse crinoidal limestones within the Marrakesh city area (LAZREQ

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(encrinites) but did not succeed to obtain new said above). All sections show Eovariscan faunas and ages. However, we recognized (Middle-Upper Devonian) breccias, as typical domal-shaped, strongly dolomitzed, large (up for Meseta sections. We logged and sampled to 50 cm) stromatoporids or stromatolites at three sections intensively, Taliouine (= the top (Fig. 10). In addition, we found a Tiliouine), Tizi-n-Ourthi, and Asserhmo, coarse, orange-reddish, post-sedimentary partly within the Devonian countourite breccia (?Eovariscan) that truncated the research project of H. HÜNEKE (Greifswald). neritic carbonate platform after it was uplifted. It is only very locally preserved and 2.2.23. Tinerhir region yielded no conodonts. The Sub Meseta Fault Zone continues eastwards to the Tinerhir region (Fig. 5), 2.2.21. Western High Atlas where there was complex transpressional In the western High Atlas, there are several tectonics and nappe stacking (MICHARD et al. tectonic windows which expose Devonian 1982; FERONI et al. 2010) marking the strata, especially the Lower Devonian (e.g., “Southern Variscan Front”. The Devonian CORNÉE 1989; CORNÉE et al. 1990). The age occurs as variably-sized olistolites and more of most stratigraphic units is still only roughly massive, double reworked breccia units established; conodont and microfacies data within the Lower Carboniferous are still lacking. More at an exploration stage, (HINDERMEYER 1954, 1955; GRAHAM & we took some samples from bryozoan-rich, SEVASTOPULO 2008). We sampled many partly biostromal Emsian limestones at Souk individual clasts within the Taourirt n´Khellil Sebt Talmakant. A similar initial survey Formation (RYTINA et al. 2013) as well as concerning allochthonous Devonian blocks at large individual olistolites (within the Aït Ida ou Zal (DE KONINCK 1957) yielded black Yalla Formation) and a breccia succession at orthocerid limestones of unclear age, because Tikkedarine (western end of Tinerhir). This they lack conodonts. will enable a high-resolution reconstruction of Devonian sedimentation at the former 2.2.22. Skoura region Anti-Atlas/Meseta boundary. Clearly, there Since the initial study by ROCH (1939), the was no major facies and faunal break; the well-exposed and partly thick Devonian and tectonic suture did not yet exist in Devonian Lower Carboniferous stratigraphy, faunas, time. and facies succession of the Skoura region (Fig. 5), NNE/NE of Ouarzazate, and at the 2.2.24. Tinejdad region southern foot of the High Atlas, remained Another large isolated Devonian olistolite very poorly studied. LAVILLE (1980) lies close to main road from Tinerhir to concentrated on the tectonics and Tinejdad, but closer to the latter (locality microtectonics. The region belongs to the Sub named as Bou Tisdafine East). It differs Meseta (Fault) Zone of MICHARD et al. (2010: considerably from the large lower Emsian SMZ or SMFZ). It includes along strike olistolites to the West since it preserved consistent sedimentary successions that are internally a non-cleaved (Anti-Atlas-type), non-cleaved and weakly deformed in the fine and fossiliferous Eifelian to Famennian West and strongly tectonized in the East. The succession. Important are trilobite-rich Lower/Middle Devonian facies and faunas limestones, Givetian (Eovariscan) breccias, strongly resemble the Anti-Atlas but there are and a pristine Frasnian-Famennian boundary also relationships with the eastern Jebilet (as sequence.

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Just to the NE of Tinejdad, the Repository allochthonous Devonian of Oued Ferkla The figured and listed fossils, with the became within our project the subject of the exception of specimens shown in field photos, M.Sc. study of P. D. WARD (WARD et al. are deposited in the Geomuseum Münster, 2013). Only preliminary results have been WWU, under the following collection published so far. Further microfacies and numbers: tectonic studies are currently been conducted by A. TALIH (Rabat). The section is Brachiopods: B5B.15… exceptional for its perfect preservation of the Cephalopods: B6C.53… Kačak and pumilio Events and rich in Conodonts: B9A.12… agglutinating foraminifers. Whilst the Emsian Corals: B2C.56… to basal Givetian is weakly deformed and Ostracods: B7B.15… very similar to the Tafilalt, the Upper Shark teeth: A1C.4… Devonian just to the North is very strongly Trilobites: B7A.11… cleaved, unfossiliferous, and was deposited in a turbiditic (flyschoid) basin.

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