Tafraout Group - Knowledge (XXG)

722:, both showcasing significant evidence of diapirism during the late Lias period in the central Atlas region. Dated back to the Earliest Toarcian epochs, identified by its brachiopod fauna. The Amezraï Formation constitutes the earliest segment of this group, composed of sandstones, sandy marls, green and red marls, and biodetrital and/or oolitic limestones, with the layers ranging in thickness from centimeters to decimeters and limestone layers up to 6 meters thick sporadically within the formation. Horizons of reworking and hardgrounds are typically restricted to the limestone layers, while ripples and cross-bedding are found in the sandstone layers. Its outcrops, such as those in Jbel Azourki, consist of a mix of carbonates, sandstones, and marls, accompanied by conglomeratic facies containing Paleozoic basement elements. The vertical arrangement of these facies indicates a gradational decrease, with conglomerates, sandstones, and clays forming the lower part of the formation, transitioning to limestones, marls, and sandstones towards the top. These variations signify the erosion of sandy layers within a shallow platform environment, as evidenced by multiple criteria. It´s layers are interpreted as deposits formed in an environment ranging from subtidal to supratidal, were monospecific accumulations of organisms, especially Bivalves in individual layers, may indicate restricted lagoonal depositional conditions. It is also marked compared with the older Pliensbachian units with a decreased carbonate content. 763:

content from bottom to top, with gradations, laminations, and ripple marks present. Microscopically, the thin-layered turbidites consist mainly of fine-grained silt, with variations in the percentage of siliciclastics and carbonate detritus over time and place. Siliciclastic portions include quartz grains, feldspar, and often glauconite, with micritic carbonate detritus ranging from 15% to 60% in a micritic matrix, with components indicating a distant source area. Pyrite can be enriched in nests or finely dispersed in individual layers. The siliciclastic turbidites suggest an open marine depositional environment, with interruptions in sedimentation and evidence of carbonate portion supply from neighboring emersion zones. Gravel stratification, lateral variations in siliciclastic grain size, and thickness fluctuations suggest different source areas, likely due to movements along paleostèration zones, reactivated during the Toarcian. The Tagoudite Formation is widespread in the Central High Atlas, wedged against paleorelief slopes or Boutonnières, with a thicknesses range up to 320 m, with variations noted in different areas of the Atlas region, including Tounfite, Rich, and Beni Mellal. In the Central Middle Atlas, sedimentation interruptions indicate emersion area formation preceding the deposition of this formation, with complete wedge-out to the east, approximately in the Midelt-Errachidia strait area.

666:. It was on the so-called Post-rift phase that the local tectonics had a thermal relaxation and allowed the deposition of the Jurassic-Cretaceous carbonate platforms. The structure of the High Atlas can be defined by two main groups of faults, thrust and oblique-slip faults, that occur from W-E to NE-SW. The presence of tectonic inversion in the Atlas Mountains has shown that are an intracontinental mountain belts that appeared from the uplift of pre-existing rift systems, where here is represented by a major rift system (~2000 km) originated on the Mesozoic, that was later uplifted and inverted in the Cenozoic. The impact and convergence movements of the African-Iberian plates after the Mesozoic end with an inversion of the previous deposited strata, transporting the sediments of that and forming new low angle thrusts. Triassic, Jurassic and Cretaceous strata are confined within basins controlled by the extensional structures of the Mesozoic rift. The Jurassic basins can be grouped into two main provinces located on either side of an emerged 750:. These observed sequences, displaying a "coarsening up" pattern, illustrate the advancement of a sandy beach area (sandstone) over a shallow subtidal zone (marls). The gullied limestones at the sequence's base denote phases of flooding preceding the resurgence of subtidal sedimentation. The presence of micritized ooids and terrigenous quartz grains indicates episodic hypersaline conditions, while sandstones and microconglomerates are predominantly quartz with occasional feldspar, carbonate detritus, and malachite flakes. The restricted variety of organisms suggests challenging living conditions, with high subsidence rates in certain regions. Sandstone/marl alternations and limestone/marl sequences are interpreted as proximal turbidites, with shallow water organisms and plant remains likely due to rearrangements in submarine channels. The occurrence of dry cracks indicates periodic emersion phases. 1080:

fossil fauna consisting of abundant algae, benthic foraminifera, common oncoids, gastropods, and bivalve bioclasts. As the Lower Toarcian started, over the region, the carbonate platform was abruptly replaced by siliciclastic deposits fed by a greater surrounding hinterland weathering, measured thanks to increased plant debris and the absence of evaporite-rich intervals and semi-arid paleosols, with alternating shoreline-forest depositional contexts. This initial layers are overlied by storm-dominated deposits, with a depauperate fauna and very common occurrence of plant debris, which with the increase in ooid-rich facies suggest deposition on a warm, wet climate belt. Some of these areas, particularly the more coastal ones located in the Azilal region, have an appearance similar to that of modern

746:). The overall sedimentary trend indicates a progressive filling process. Initially, the presence of foraminifera assemblages, ammonite traces, and turbidite spits within the marls suggests sedimentation in an open marine environment with a circalittoral setting. Sandstone turbidites observed at the basin's northern boundary indicate material transit across the Pliensbachian platform. On the other hand, carbonate turbidites observed farther south in the Taquat N'Agrd area are likely attributed to erosion in high intra-basin regions. Moving towards the upper sections, a vertical arrangement and gradual filling process led to the formation of a supratidal carbonate coastal plain, characterized by tropical conditions akin to those observed on 742:

on a coastal platform. This formation is primarily composed of sandstone marl, silt marl, and ooid limestone, distinctly different from the underlying layers. The most common fossils include Bivalves, which often form lumachellae, large brachiopods, gastropods, solitary corals, and echinoderm remains. Plant remains, some with malachite, are found in the sandstones and microconglomerate lenses. The rocks show various microfacies types formed under supratidal to subtidal conditions, including bio-, oosparites/grainstones, and silt marl with fine-grained terrigen detritus. The upper segment of the Tafraout Formation represents sedimentation resulting from terrigenous dispersal in the former "basin" of the upper Pliensbachian (

710:

patch reefs. Sandstones and oolitic and/or biodetritic limestone are often interposed. Red and green marls occur in numerous decimetre-thick layers. Occasionally there are conglomerate lenses with Liassic elements. Oblique stratification and ooid limestones are predominantly restricted to the area surrounding patch reefs. This formation denotes a transitional environment from supratidal to intertidal, exhibiting facies development similar to the underlying Trafraout Formation. Local tectonic activity, primarily triggered by seismic events in the Tethyan domain, played a pivotal role in the formation process. Consequently, emergent Paleozoic strata underwent erosion owing to prevailing local conditions.

1016:

channels abundant in plant roots (mostly located in fine limestone, probably from the channel margins), developed in the near E-W direction of transit. The channel lithology shows notable enrichment of material from the Paleozoic basement and Triassic cover, with interbedded volcanic material (sand to pebbles), generally constituting more than half of the detrital components, showing clear carbonate recrystallization, suggesting that these fragments were still at high temperature during deposition and, therefore, contemporaneous with the sedimentation. Lithic elements or isolated crystals found locally show no evidence of prolonged transport, probably from relatively nearby

976:, soft pebbles, crisscrossed stratifications and "ripplemarks") reflect a confined to continental/marine deposition environment, with temporary emersions, where conditions met in a deltaic environment with saltwater/brackish influences. This terrigenous deposition can be seen from north to south as a lateral transition from a coastal facies to a fluvial facies (at Adoumaz) to a foreshore facies (Ghnim "fining up" type sequences) to a beach facies (Jbel Taguendouft "coarsening up" type sequences). The relatively small thicknesses found at the Jbel Taguendouft section would testify to the tectonic activity of the 7074: 1068: 1038: 619: 1204: 1269:, showing that sedimentation at this time took place in a distensive tectonic context. Then, towards the Late Toarcian-Aalenian boundary, the series corresponds to detrital deposits with carbonate intercalations with neritic fauna. The structural analysis shows that the sedimentation during the upper Toarcian was controlled by a tectonic game, always distensive, causing the tilting of blocks along the transverse fault of NW-SE direction, which leads to the creation of available space with openings always towards E and NE. 4099: 854:

the Tagoudite & Azilal Formations. Then, with the Middle Toarcian- Aalenian, the Azilal Formation expanded towards the east as the sedimentation resumed throughout the region, where coeval layers in the Amezraï subsiding basin was filled by carbonates from the internal platform of the Tafraout and Aguerd n’Tazoult, being surrounded to the north, east and south by a coastal area with dominant terrigenous sedimentation of the own Azilal Formation. This period is marked by the individualization of the

4725: 924: 469: 6551: 557:("Tafraout Platform"), best assigned to succession W-E of alluvial environment occasionally interrupted by shallow marine incursions (tidal flat setting) and inner platform to open marine settings, and marks a dramatic decrease of the carbonate productivity under increasing terrigenous sedimentation. Fossils include large reef biotas with richness in "lithiotid" bivalves and coral mounts ("Patch reef", Tafraout Formation), but also by remains of vertebrates such as the sauropod 5788: 3463: 3954: 7007: 3765: 1278: 1112:, all places that were subaerially exposed during the Jurassic. Specifically, the Anti-Atlas shows processes of tectonic uplift, overburden erosion, which, combined with the concentration of coarse siliciclastic material in the western part of the central High Atlas (absent in the east), suggest that this area was the source of the altered Lower Toarcian sediments, allowing the tracing of the fluvial channels that developed towards the Azilal Formation. 5733: 1029: 3160: 6724: 6248: 3572: 7270: 772: 3337: 406: 933: 6602: 5999: 2940:. Gastropods have been discovered in several places, but none of the specimens have been studied nor identified. Beds with large accumulations of unidentified Ostracod valves on an endemic thin level of green marl are found at the Beni-Mellal area (Adoumaz & Col de Ghnim outcrops). The tubes of serpulid worms are known from Jbel Toksine, in relation to the bivalve pavements. 128: 964:. It was the emerged part of a Siliciclastic-Carbonate platform and represented a variety of settings, including continental river/palustrine-dominated, paralic-tidal deposits, and tidal mudflat shorelines. The terrigenous-dominated deposits of the Azilal Formation were deposited in a coastal environment with continental influence. On this facies, the fauna (composed of rare 686:, calciturbidites and reefal limestones were accumulated in the E Central High Atlas, while on the west margin around the Massif Ancien terrestrial, specially fluvial sedimentation dominated. The present Red Beds of Azilal and the younger marls of Bin el Ouidane indicate various marine oscillations across the Toarcian-Bajocian boundary, ending its sedimentation with the major 476: 569:, along with several undescribed genera. While there have been attributions of its lowermost layers to the Latest Pliensbachian, the current oldest properly measured are part of the Earliest Toarcian regression ("MRST10"), part of the Lower-Middle Palymorphum biozone. This group is composed of the following units, which extend from west to east: the 3244: 3673: 9355: 6896:

At Jebel Azourki, several marine lithofacies were recorded, from 1 to 5, but with an additional 6th of medium gray to black laminated shales with coal streaks and abundant plant fragments, the attribution of which is n is not clear, since it may be Pliensbachian or Toarcian, as may also belong to the

1319:

Examining local diapirism in the Upper Liassic has provided valuable insights into climate and deposition in the coexisting marine Amellago Formation. Intervals devoid of ooids indicate a wetter climate, supported by an increase in continental particles—a sign of heightened Saharan Craton weathering.

853:

during the Toarcian-Aalenian: during the Lower Toarcian, this sector presented the same paleogeographic characteristics as those seen during the uppermost Pliensbachian, being latter followed by a reduction in the deposition areas and a filling of the Pliensbachian basins by terrigenous material from

841:

to the North and the North-Atlasic accident to the South. At Talmest-Tazoult ridge, the siliclastic-carbonate series of the Toarcian-Aalenian form a clear progressive unconformity above the carbonates of the Sinemurian-Pliensbachian, building an individualized ridge oriented NE-SW, limiting two local

741:

The Tafraout Formation comprises oolitic and biodetrital limestones exhibiting cross-stratifications, arranged in channels and bars ranging from decimetric to metric scale, alongside greenish to variegated silty marls topped with lenticular layers of micro-conglomerates. These deposits were laid down

6829:

of plants associated with heavily bioturbated layers. While there is a great amount of plant remains in the form of coal, foliar debris, cuticles, woody roots, rhizolith and ghost roots, fossil wood and unidentified macrofoliar remains the only flora with some work on it was recovered at Toundoute,

3692:

The platform patch reefs in the Tafraout area are notable for their biodiversity, with some reaching heights of up to 40 m and lengths of up to 80 m, representing massive biostromes with a varied associated fossil assemblage, including bivalves, gastropods, echinoderm fragments, solitary corals, and

1299:

is seen as a weld formed by the closure of the salt wall. This period coincides with the peak of passive diapiric growth, driven by the reactivation of the central High Atlas synrift from the Pliensbachian to the Aalenian, triggering salt withdrawal and swelling of adjacent salt walls, forming the

1194:

The Tagoudite & Tafraout formations recover, as seen on worldwide units an increase of weathering due to the Pl/To and T-OAE events, with increase of the siliciclastic sediment supply and increased dissolved material to the oceans. This occurred along an intensification of tropical storm events

1079:

The environment of the Azilal Formation becomes notorious after the Middle Toarcian, with a clear major regression that ends with a slowdown of the local sedimentary filling. The paralic deposits of this phase contain clay intervals rich in continental organic matter such as wood debris, but a rare

825:

evolved as an isolated lateral equivalent, composed of intertidal to open marine carbonate environments, hosting also layers of the Tagoudite Formation, that end first overlain by the Tafraout Formation, and then in the westernmost sectors by the Azilal Formation while remaining in the central East

820:

as the major structural element in this last sector. While at Demnate, Telouet, Azilal, Skoura or Toundoute the conditions did become fully terrestrial, towards the east at Beni-Mellal the Lower Toarcian the ongoing sea regression happened latter, marked by oscillations between the Azilal Formation

910:

Ouidane transgressive facies, while the lower sequences, with fine conglomerate layers and plant remains indicate a proximal delivery area and the peak of the regression, with many microlagoons that formed between the large coral patch reefs are documented by micrite and partially leached micrite.

1199:

action) on the T-OAE, destroying the older carbonate platform organisms locally. This allowed to set the Azilal Formation environments, that range from a series of continental settings with river influence, increased during the T-AOE with more amounts of flora being washed, to nearshore deposits,

1186:

are found in the subtidal facies, building accumulations. At Jebel Toksine in the Dades Valley, the Tafraout Formation develops a local lagoon-subtidal ecosystem in arid and humid conditions. The Jebel Toksine layers represent one of the most complete records of this type of ecosystem in Morocco,

886:

allow a precise localization of this initial progradation of the terrestrial settings around the Bifrons substage of the Toarcian (that can be either considered the uppermost Lower Toarcian of the lower Middle Toarcian). The layers are, at the oldest sections of this initial phase, represented by

709:

The Aguerd-n'Tazoult formation encompasses the most recent marginal marine strata within the Amezraï minibasin, ranging from the Upper Toarcian to Aalenian periods, marked by lower sequences with great amount of conglometatic lenses and upper limit largely characterized by the occurrence of coral

695:

rifting) occurred towards the end of the Pliensbachian and beginning of the Toarcian. This second major tectonic event developed towards the E-W to NE-SW, reactivating trending normal faults, what led to the drowning of the Lower Liassic carbonate platform and the predominance of marls during the

6892:

At Jebel Toksine, lithiotid biostromes are interbedded by recessive and marly levels with woody charcoal debris (including entire trunks of wood, abundant woody plant debris preserved in the form of jet or charcoal), which suggests the presence of vegetation marginal marine that has developed a

909:

coeval with Ammonites of the same age in the easternmost Azilal formation at the Ikerzi Area confirms the marine delimitation in the last stages of deposition. In the Azilal-Aguerd system, the "Tafraout Platform" saw a deepening towards the uppermost layers, teasing the transition to the Bin el

599:. Overall, this group represents a mixed carbonate-siliciclastic system of several hundred meters thick, dominated by deposits of shallow marine platforms linked to a nearby hinterland dominated by conglomerates. The strata of the group extend towards the central High Atlas, covering different 8431:

Krencker, F. N.; Fantasia, A.; Danisch, J.; Martindale, R.; Kabiri, L.; El Ouali, M.; Bodin, S. (2020). "Two-phased Collapse of the Shallow-water Carbonate Factory during the Late Pliensbachian–Toarcian Driven by Changing Climate and Enhanced Continental Weathering in the Northwestern Gondwana

1015:

levels), intercalated with conglomerate under an arid environment, as marks the development of gypsum. This is recorded specially in the Telouet and Demnate-Wazzant area, but also seen in more detail at Toundoute: the deposits present a channel/floodplain type fluvial system, with sand-filled

762:

with predominantly siliciclastic layers. These layers comprise an irregular alternation of gray and green limestone sandstones with sandy marls and siltstones, forming megasequences with thicknesses of 10–20 m, distinguished by a decrease in siliciclastic aggregate size and an increase in marl

1294:

minibasin to the north. Within the Amezraï minibasin, the Tafraout group, stretching about 1500 m, is exposed. These deposits, interpreted as mixed Toarcian-Aalenian sediments, led to the extrusion of the diapir on its flank and the adjacent seabed, positioning the Alenian facies of the

1135:, towards the Middle Toarcian the carbonate producers recovered locally, with the ooid grainstone replaced by wackestone to packstone beds, where heterotrophic faunal bioclasts increase, such as cephalopods, brachiopods, echinoderms, and gastropods, with occasional coral patch reefs. 846:). The North Altas accident shows variations of thickness and facies, testifying a weak activity of the latter, in particular during the deposition of the Azilal Formation, with the reliefs created during the previous phase covered by the terrigenous layers of this last one. 6624:?) are know from several locations, coming from freshwater/lagoonal layers. Indeterminate dinosaurian & other vertebrates are know from Mizaguène Hill, Taouja Ougourane, Aït Ouaridène, Oued Rzef & Jbel Remuai in the Azilal Province. Some of them are recovered in a " 1254:, and shows that after cold event that affect the local waters, related to the Karoo & the Atlantic Rift volcanism the present Brachiopods, based on their preserved oxygen isotope data show that warm seawater temperatures re-established during the early Late Toarcian. 788:, and developed along a major drowning episode linked with the Toarcian Anoxic event, that led to the eustatic sea–level rise on the Early Toarcian in Europe and Africa. The Azilal Formation was bracketed between several major geologically older hinterlands: the 959:

The Tafraout Group covers most of the W High Atlas, surrounded by highlands that probably hosted dry cool (10.6 °C) to humid climate (12.30 °C), with a succession rain tundra to wet forest environments, as proven by samples from coeval layers in the

775:

Early Jurassic Paleogeography of the Sahara Craton, including source Highlands, Jurassic basins and CAMP outcrops. While the Central High Atlas basin in the N limit is represented as fully marine, it was partially filled by terrestrial sediments towards the

7907:

Bodin, S.; Krencker, F. N.; Kothe, T.; Hoffmann, R.; Mattioli, E.; Heimhofer, U.; Kabiri, L. (2016). "Perturbation of the carbon cycle during the late Pliensbachian–early Toarcian: New insight from high-resolution carbon isotope records in Morocco".

990:

The depositional environment of the Azilal formation was dominantly fluvial or alluvial, with large sandstone channels cutting through detrital conglomerate deposits. The high abundance of plant remains, either as fossil wood, cuticles, charcoal or

887:

marly and silty marls and limestones as well as marginal-littoral sandstones testifying to the siltation of this sector by sandy sheets of deltaic origin. At the same time on the Amezraï basin the fauna is composed by brachiopod fauna such as

8207:

Enregistrement sédimentaire de l'activité diapirique associée à la ride du Jbel Azourki, Haut Atlas central, Maroc : impact sur la géométrie des dépôts et la distribution des faciès des systèmes carbonatés et mixtes du Jurassique

6842:. By quantity of material the vegetation was apparently dominated by ferns, maybe concentrated in punctual wetlands (spring tuffs), followed by cycads and conifers. A possible correlative flora if found in the same age layers of the 1320:

Additionally, the presence of small amounts of charcoal or charred wood remnants suggests the existence of coastal forests or mangroves in the carbonate ramp of the Zaouiat Ahançal group during periods of increased local humidity.

1295:

Aguerd-nˈTazoult Formation in a sub-horizontal orientation beyond the allochthonous body. The sharp transition between the gently SE-dipping Zaouiat Ahançal Group and the steeply NW-dipping Late Aalenian-Bajocian carbonates of the

690:

redbeds. A initial tectonic event on the Triassic-Jurassic boundary led to the formation of the Tigrinine-Taabast pull-apart basin, for example. Following this event a major extensional tectonic activity (derived from the second

6913:

algae indicate that the palaeoenvironment of the lower Toarcian Amellago area was likely proximal continental shelf with a high terrestrial input, and notorious influence of brackish water in the depositional environment.

811:

are directly overlain by terrigenous deposits of the Azilal Formation after the initial major Toarcian regression: red clays, conglomerates with paleozoic elements. This deposits fill many small basins in tearing in the Atlas of

1289:

being one such diapiric sector spanning approximately 20 km. Oriented NE-SW, it slightly deviates from the dominant ENE-WSW structural trend of the central High Atlas, flanked by the Amezraï minibasin to the south and the

2919:

In the Tafraout Group, the fossil record of units like the Azilal Formation is very restrictive compared to the marine coeval/underliying units like the Amezraï or Tafraout Formations. In the Dadés area Coral patch

5212:(Bivalve). A large bivalve, with a subequivalent shell, reaching 60–70 cm high. It is one of the three main bivalves found on the Lithiotis Facies, whose accumulations generally cover megalodontid coquinas. 5415:(Bivalve). This genus was founded to be a bivalve with a byssate juvenile stage that developed different lifestyles as adults depending on the density of the individuals and the firmness of the bottom 1054:

or the reefs off the Bahamas). As in other coexisting Tethyan units, it is very likely that this section had sections with mangroves, given that the Tafraout Group lies close to a dry interior area

9696:

Ghandour, I. M.; Fürsich, F. T. (2022). "Allogenic and autogenic controls on facies and stratigraphic architecture of the Lower Jurassic Mashabba Formation, Gebel Al-Maghara, North Sinai, Egypt".

1096:, implying a hinterland that is frequently emerged and subject to erosion and the effects of diagenesis. The only ones of this nature in Morocco, that on the Atlas are located to the south in the 9557:"Données nouvelles sur le Jurassique rouge à Dinosauriens du Grand et du Moyen-Atlas (Maroc) [New data on the Jurassic red beds with dinosaurs from the Great and Middle Atlas (Morocco)]" 6834:

from ferns and, less frequently, cycad pinnulae, with common cuticles and no palynomorphs. Wood debris from the same locality showed affinity within the coniferophytes, resembling the abietoid

861:

Despite being claimed to have Latest Pliensbachian layers, the Azilal Formation is measured in post Polymorphum (Earliest Toarcian) levels, and impacts in the sedimentation (especially of the

1300:

Talmest allochthonous salt sheet at its SE end. In terms of paleoenvironment, the elongated carbonate platforms of Tazoult, formed by rifts, resemble those found in the shallow waters of the

610:

are also very present in the marginal marine strata of the Tafraout Group, with the Toksine Section recording a dramatic collapse on the scale of the Tethys of the neritic carbonate system.

6893:

stabilizing role, which is common in relatively humid environments conducive to the development of marginal marine plants and has the propensity to develop meandering channel morphologies.

8926:

Martín-Martín, J. D.; Vergés, J.; Saura, E.; Moragas, M.; Messager, G.; Baqués, V.; Razin, P.; Grélaud, C.; Malaval, M.; Joussiaume, R.; Casciello, E.; Cruz-Orosa, I.; Hunt, D. W. (2017).

9049: 9556: 9758:

Neri, M.; Roghi, G.; Ragazzi, E.; Papazzoni, C. A. (2017). "First record of Pliensbachian (Lower Jurassic) amber and associated palynoflora from the Monti Lessini (northern Italy)".

9413:"An insight into the systematics of Plicatostylidae (Bivalvia), with a description of Pachygervillia anguillaensis n. gen. n. sp. from the Lithiotis Facies (Lower Jurassic) of Italy" 1223:, a succession of near shore marine strata disposed along the Toarcian boundary, where its last 40 m belong to the lower part of the Azilal Formation and are composed of dolomitized 6718:. Recovered from the Tagoudite Formation, represents a genus of cosmopolitan fish, common in the Toarcian Mediterranean area. Most specimens appear to come from lagoonal facies. 8016:

Font, E.; Youbi, N.; Fernandes, S.; El Hachimi, H.; Kratinova, Z.; Hamim, Y. (2011). "Revisiting the magnetostratigraphy of the Central Atlantic Magmatic Province from Morocco".

9654:

Allain, Ronan; Aquesbi, Najat; Jean, Dejax; Meyer, Christian; Monbaron, Michel; Montenat, Christian; Richir, Philippe; Rochdy, Mohammed; Russell, Dale; Taquet, Philippe (2004).

6484:

articulated and fragmentary specimens and indeterminate echinoid fragments, are know from several localities, usually associated with large coral bioherms or sea trangressions.

1261:, sedimentation carbonate with bioconstructions (patch-reef), develops with a thickening towards the East and a still thinning towards the West in the direction of the reef of 8786:"Stratigraphic distribution and paleoecological significance of Early Jurassic (Pliensbachian-Toarcian) lithiotid-coral reefal deposits from the Central High Atlas of Morocco" 8475:

Kairouani, Hajar; Abbassi, Anas; Zaghloul, Mohamed Najib; El Mourabet, Mohamed; Micheletti, Francesca; Fornelli, Annamaria; Mongelli, Giovanni; Critelli, Salvatore (2024).

638:

periods. Its geometry is distinctive due to the presence of several ENE–WSW narrow rift basins, derived from four major tectonic phases: pre-rift, that was linked with the

1088:

along the entire Atlas Basin. These siliciclastic beds have abundant pebbles of metamorphic and igneous rocks, implying that the material must have been derived from the

8696:

Frizon de Lamotte, D.; Zizi, M.; Missenard, Y.; Hafid, M.; Azzouzi, M.E.; Maury, R.C.; Charrière, A.; Taki, Z.; Benammi, M.; Michard, A. (2008). "The Atlas System".

1115:

At the same time towards the South-East the Tafraout Formation in the Amezraï basin represents a marginal marine environment, with wave ripples, cross-bedding, the

8588:"Stratigraphie et paléoenvironnement des dépôts volcano-détritiques à dinosauriens du Jurassique inférieur de Toundoute (Province de Ouarzazate, Haut-Atlas–Maroc)" 905:

that corroborate the Toarcian age and the connection between both locations. Meanwhile, the presence of Aalenian (Bradfordernsis-Murchinsonae) Branchiopods in the

9217:"Données lithostratigraphiques et biostratigraphiques sur le Lias dans le cadre de deux transects du Haut-Atlas central (Beni Mellal et Midelt-Errachidia, Maroc)" 873:) in the Middle Toarcian-Lower Aalenian, marked by a notorious sea regression, distributed in at least 6 sequences, that overlie layers with the ammonite genus 7760: 9159:"Mise en évidence de la limite Pliensbachien-Toarcien par les ammonites, les foraminifères et l'interaction tectono-eustatique dans la région de Todrha-Dadès" 8648:"Toarcian carbon isotope shifts and nutrient changes from the Northern margin of Gondwana (High Atlas, Morocco, Jurassic): palaeoenvironmental implications" 7621:"Analyses biostratigraphiques dans le Lias de la bordure sud de la Téthys méditerranéenne: l'exemple de la frange méridionale du Haut-Atlas central (Maroc)" 1060:

The overall local climate was warm with alternating wet and dry periods have generated soils with differentiated calcareous profiles (pedogenetic nodules,

670:: west, where the basin was open to the Early Atlantic, being related to its passive margin, and east with several epicontinental troughs connected to the 1285:

The central High Atlas region harbors a cluster of elongated diapirs and minibasins formed during the Lower Jurassic rifting of the Atlas basin, with the

9188:

Chafiki, D. (1994). "Dynamique sédimentaire à l'articulation plate forme-bassin: Exemple du Lias de la région de Beni Melal (Haut Atlas central-Maroc)".

9133:"Le Toarcien (sommet de la Zone à Polymorphum–Zone à Bonarelli) d'Amellagou (Haut Atlas Central, Maroc) : Palynostratigraphie et Paléoenvironnement" 5513:(Bivalve). Is considered a genus that evolved from shallow-burrowing ancestors, secondarily becoming an edge-prone semi-fauna adapted to photosymbiosis. 7574:"The effects of strong sediment-supply variability on the sequence stratigraphic architecture: Insights from early Toarcian carbonate factory collapses" 9131:

Khaffou, H.; Hssaida, T.; Maatouf, W.; Essafraoui, B.; El Ouali, M.; Essamoud, R.; Louaya, A.; Rachid, J.; Chakir, S.; Jaydawi, S.; Chafai, K. (2023).

9257:

Rodríguez-Tovar, F. J. (2021). "Ichnology of the Toarcian Oceanic Anoxic Event: An understimated tool to assess palaeoenvironmental interpretations".

8477:"The Jurassic climate change in the northwest Gondwana (External Rif, Morocco): Evidence from geochemistry and implication for paleoclimate evolution" 8275:"Jurassic (uppermost Sinemurian - Aalenian) sequence stratigraphy and geodynamic evolution of the Ait Bou Guemmez area (Central High Atlas, Morocco)" 821:

and the marly marine Tagoudite or the carbonate Tafraout, ending both fully overlain by the terrigenous layers towards the Middle-Late Toarcian. The

9048:

Fonville, Tanner; Martindale, Rowan C.; N. Stone, Travis; Septfontaine, Michel; Bodin, Stéphane; Krencker, François-Nicolas; Kabiri, Lahcen (2024).

5013:). Mostly benthonic specimens are known. The presence of this species indicates an upper Toarcian-Aalenian age for the layers where was discovered. 1170:

and also in Morocco, indicate the return of carbonate activity in the Central Atlas. These Reefs showed strong zonation, starting with the bivalves

1084:, for example those of found in the modern Persian Gulf. These intervals have increased nutrient levels locally, as evidenced by the high amount of 8874:

Moragas, Mar; Baqués, Vinyet; Travé, Anna; Martín-Martín, Juan Diego; Saura, Eduard; Messager, Gregoire; Hunt, David; Vergés, Jaume (2019-07-10).

8106:"L'accident tizal-azourki haut atlas central du maroc: déformations synsedimentaires liasiques en extension et conséquences du serrage atlasique" 1265:, where the dew marine fossils of the formation are recovered. The Coralline faunas suffered a significant collapse visible in the locality of 7726: 780:

The Tafraout Group was deposited in the Moroccan Carbonate Platform, at a palaeolatitude between 19°-20°N, around the same latitude as modern

8713: 7993: 9071:

Löwner, Ralf (2009). "Recherches sedimentologiques et structurales à l'articulation entre Haut et Moyen Atlas et la Haute Moulouya, Maroc".

7761:"Deformations synsedimentaires en compression pendant le Lias superieur et le Dogger, au Tizi n'Irhil (Haut Atlas central de Midelt, Maroc)" 6901:. These black lithofacies shales are interpreted to represent a supratidal marsh developed at the edges of an intertidal zone and a lagoon. 468: 9356:"Le genre de Pseudogibbirhynchia : Rhynchonellacea : dans le Toarcien et l'Aalenien inferieur du Haut Atlas central et oriental" 7501:"Les formations lithostratigraphiques jurassiques du Haut Atlas central (Maroc) : corrélations et reconstitutions paléogéographiques" 5994:. The basis of this series is based on a regional discontinuity marked by a remarkable abundance of Eodactylites from the Lower Toarcian 1075:, near Dakhla. Some areas of the Azilal, Amezraï, Tafraout and Aguerd n’Tazoult Formations have layers derived from a similar deposition 1281:

Gubal Straits in Egypt have an appearance comparable to that recorded in the diapirs which generated the carbonate platforms of Tazoult

9851: 1050:, the Tafraout Formation developed lithiotidocoral reefs (These reefs would have been identical to modern reefs, such as those of the 663: 2936:

and algae. Plant remains are very abundant in places such as the north of Jbel Akenzoud and partly impregnated and/or carbonized by

9508:"A major sea-level drop briefly precedes the Toarcian oceanic anoxic event: implication for Early Jurassic climate and carbon cycle" 7865:"Extension et developpement des phenomenes recifaux jurassiques dans le domaine atlasique marocain, particulierement au Lias moyen" 7073: 9886: 9881: 8151:"Early post-rift depositional systems of the Central Atlantic: Lower and Middle Jurassic of the Essaouira-Agadir Basin, Morocco" 5075:). Relatively abundant on seashore deposits. Includes juvenile forms of Telothyris jauberti, present on benthic deposit strata. 3579:, avec une faune moderne apparentée, montrant la convergence écologique et la variété des animaux qui ont quitté cet Ichnogenus 7385: 9132: 8990:"Spatial and temporal distribution of ooids along a Jurassic carbonate ramp: Amellago outcrop transect, High-Atlas, Morocco" 1067: 7532:"Cadre stratigraphique et étapes de structuration de la plate-forme liasique d'Aït Bou Guemmez (Haut-Atlas central, Maroc)" 758:

The Tagoudite Formation represents a significant shift in Liassic sedimentation, replacing the carbonate turbidites of the

9876: 9866: 6822: 1216: 607: 442:

Right side valley of Assif Tafraout flowing in a northerly direction. The village of Tafraout lies about 1 km to the north

9459:

Benzaggagh, Mohamed; Khaffou, Hanane; Salamon, Mariusz A.; Hssaida, Touria; Ouali, Mohamed El; Essafraoui, Badre (2022).

9307:

Benzaggagh, Mohamed; Salamon, Mariusz A.; Khaffou, Hanane; Hssaida, Touria; El Ouali, Mohamed; Essafraoui, Badre (2022).

8876:"Diagenetic evolution of lower Jurassic platform carbonates flanking the Tazoult salt wall (Central High Atlas, Morocco)" 949:

coast in New Caledonia. Surrounding highlands hosted ecosystems with alternating tundra and moist forests (ex. Brazilian

575:(continental to subtidal, including its synonyms the "Wazzant Formation" and the "Continental Series of Toundoute"); the 8385:

Bassoullet, J. P.; Elmi, S.; Poisson, A.; Cecca, F.; Bellion, Y.; Guiraud, R.; Vrielynck, B. (1993). "Middle Toarcian".

7983: 312: 1037: 9622:"Recherches sedimentologiques et structurales à l'articulation entre Haut et Moyen Atlas et la Haute Moulouya, Maroc" 9215:

Chafiki, D.; ElHariri, K.; Souhel, A.; Lachkar, N.; Sarih, S.; Dommergues, J.L.; Garcia, J.P.; Quiquerez, A. (2007).

8150: 5088:"Dwarf black bivalves (Lucinidae?)" in great abundance where reported from the Azilal Formation at its type section. 8105: 618: 8784:

Brame, H. M. R.; Martindale, R. C.; Ettinger, N. P.; Debeljak, I.; Vasseur, R.; Lathuilière, B.; Bodin, S. (2019).

1203: 8532:"Sedimentation-calcrete cycles in the Mesozoic Red formations from the central High atlas (Telouet area), Morocco" 9846: 5728:(Snail). Local specimens appear to have algal material on the shells, indicating restricted lagoon environments. 319: 9871: 8353:"Le Mésozoïque dans Haut Atlas de Beni-Mellal (Maroc). Stratigraphie, sédimentologie et évolution géodynamique" 7415: 1296: 1240: 358: 187: 5662:

Multiple Gasteropodan faunas are know, specially associated with coral patch reefs, but lack proper studies.

591:(including the "Tamadout Formation", shallow subtidal to open pelagic). They are connected with the offshore 9861: 9856: 7365: 4098: 950: 862: 9594: 987:

and other coeval marine units, as well are found on fluviatile channels inside the own rocks of this unit.

650:-Late Triassic with several NE–SW to ENE–WSW rift-basins, al derived from the almost coeval opening of the 592: 8928:"Diapiric growth within an Early Jurassic rift basin: The Tazoult salt wall (central High Atlas, Morocco)" 7373: 5873: 5864: 5261:(Bivalve). Abundant along rootlets, indicating a very shallow and restricted lagoon or marsh environment 5006: 4724: 983:

The flow of the fluvial-washed sediments take place in a E-NE direction, being moved to the layers of the

838: 837:

Basin in the south, showed that the depocenter zone corresponded to the disposal area located between the

283: 7818:"Le Toarcien inférieur du Haut Atlas de Todrha–Dadès (Maroc) : sédimentologie et lithostratigraphie" 5520: 4735: 4153: 2427: 1513: 977: 900: 718:

This formation is predominantly exposed in the mini-basin bearing the same name, closely linked with the

658:. This rift-derived basins ended filled with continental siliciclastic sediments, and latter towards the 596: 221: 177: 8352: 6843: 1402: 1187:

recording several generations of lithiotic growth over ~1 km of exposure (consisting of the genera

849:

Two main stages can be then distinguished in the paleogeographic evolution of the western border of the

789: 211: 132:

The village of Zaouiat Ahançal (in the foreground) and the strata of the formations (in the background).

9412: 8587: 8239:"Événements tectono-sédimentaires au Lias-Dogger de la frange méridionale du Haut-Atlas central, Maroc" 7985:

Triassic–Jurassic rifting, Continental Breakup and the Origin of the Atlantic Ocean and Passive Margins

7950:"Superposed folding resulting from inversion of a synrift accommodation zone, Atlas Mountains, Morocco" 7170: 4801: 4046: 3868: 2555: 2367: 1661: 1266: 759: 236: 226: 8828:

Krencker, F. N.; Bodin, S.; Hoffmann, R.; Suan, G.; Mattioli, E.; Kabiri, L.; Immenhauser, A. (2014).

8785: 8647: 7817: 7085: 7023: 4891: 4594: 4561: 4492: 4444: 4329: 3901: 3857: 2762:. The presence of this genus indicates fresh or brackish water inputs in the depositional environment 2159: 1471: 1251: 1072: 923: 9806: 9767: 9705: 9670: 9472: 9320: 9266: 9001: 8939: 8841: 8797: 8662: 8602: 8543: 8488: 8441: 8165: 8061: 7917: 7829: 7585: 7391: 6595: 5456: 5412: 5258: 5209: 4816: 4650: 4362: 4142: 3997: 2253: 2242: 2148: 2101: 1761: 1305: 1139: 889: 875: 231: 197: 182: 141: 8646:

Bodin, S.; Mattioli, E.; Frohlich, S.; Marshall, J.D.; Boutib, L.; Lahsini, S.; Redfern, J. (2010).

7218: 5423: 5220: 5068: 4935: 4713: 4669: 4609: 4318: 4274: 4230: 4197: 4186: 4091: 4008: 3775: 2656: 2378: 1973: 1918: 1101: 834: 7291: 6010: 5787: 4950: 4507: 4459: 4405: 4285: 3819: 3757: 3462: 2667: 2604: 1625: 1564: 1363: 1313: 1286: 1262: 1200:

paralic and subtidal, subject of storm and tropical storm events, all set on a warm humid climate.

1182:

are limited to subtidal lagoon facies and even to certain poorly oxygenated environments. Finally,

1020:, being these collected and transported by a poorly developed river system during episodic floods. 822: 719: 667: 626:

The Central High Atlas of Morocco is part of a double-vergent mountain belt that originated due to

502: 192: 8586:

Montenat, C.; Monbaron, M.; Allain, R.; Aquesbi, N.; Dejax, J.; Hernandez, J.; Taquet, P. (2005).

5171: 5160: 4876: 3964: 3657: 3136: 2858: 2551: 2518: 2325: 2314: 2206: 2112: 2042: 2031: 1614: 1460: 1258: 1220: 1047: 9721: 9621: 9382:"Carte géologique du Maroc au 1/100 000: feuille Azilal (Haut Atlas central). Mémoire explicatif" 9282: 9197: 9088: 8678: 8618: 8512: 8457: 8181: 8079: 7703:

Stratigraphie, Fazies und Paläogeographie des Jura am Südrand des zentralen Hohen Atlas (Marokko)

7470:"Carte géologique du Maroc au 1/100 000: feuille Azilal (Haut Atlas central). Mémoire explicatif" 7403: 6944: 6872: 5743: 5374: 2618: 2195: 1929: 1772: 1719: 1708: 1208: 1132: 1051: 1017: 996: 984: 554: 7500: 7006: 6882: 5021: 3912: 3764: 3723: 2717: 1575: 1291: 1277: 6550: 5118: 4241: 3953: 1984: 1855: 1528: 1413: 9822: 9527: 9488: 9336: 9017: 8965: 8905: 8709: 8700:. Lecture Notes in Earth Sciences. Vol. 6. Springer Berlin Heidelberg. pp. 133–202. 8559: 8504: 8294: 7989: 7880: 7845: 7707: 7620: 7601: 7360: 7151: 6991: 6898: 6425: 5991: 5780: 5319: 2806: 2566: 1567:. It represents a species related to E. virguliana, known from the Middle Jurassic of Morocco 1127: 808: 743: 639: 216: 9050:"Early Jurassic Benthic Foraminiferal Ecology From The Central High Atlas Mountains, Morocco" 8149:

Duval-Arnould, A.; Schröder, S.; Charton, R.; Joussiaume, R.; Razin, P.; Redfern, J. (2021).

5467: 1105: 843: 9814: 9775: 9713: 9678: 9568: 9535: 9519: 9480: 9328: 9274: 9080: 9009: 8955: 8947: 8895: 8887: 8849: 8805: 8701: 8670: 8610: 8551: 8496: 8449: 8286: 8173: 8117: 8069: 8025: 7925: 7872: 7837: 7772: 7632: 7593: 7397: 7379: 7349: 6831: 6811: 6305: 5831: 3159: 995:, reveals the presence of vegetated soils in the vicinity. There is also evidence ephemeral 829:

The Tafraout Group co-evolved with several staggered sections from the southern edge of the

731: 570: 6723: 6247: 3571: 1028: 7530:

El Bchari, F.; Ibouh, H.; Souhel, A.; Taj-Eddine, K.; Canérot, J.; Bouabdelli, M. (2001).

7203: 6987: 6886: 6349: 2503: 1219:

is also highly present on the marginal marine strata of the formation, with the so-called

866: 747: 534: 518: 870: 9810: 9771: 9709: 9674: 9476: 9324: 9270: 9005: 8943: 8845: 8830:"The middle Toarcian cold snap: trigger of mass extinction and carbonate factory demise" 8801: 8666: 8606: 8547: 8492: 8445: 8169: 8065: 7921: 7833: 7589: 7269: 5732: 858:

in the center of the basin and by a relative tectonic calm in the other coeval sectors.

771: 9540: 9381: 7469: 7409: 7274: 6999: 6734: 6382: 6338: 6237: 6160: 6111: 6052: 5912: 4546: 3475: 3258: 2899: 2759: 1109: 651: 526: 514: 351: 9655: 9309:"Brachiopodes toarciens de la coupe d'Aït Athmane, Haut Atlas centro-oriental (Maroc)" 7864: 1231:, that show a slowly recovering a low-depth nearshore marine environment after in the 9840: 9818: 9725: 9572: 9286: 9201: 9158: 9092: 8829: 8682: 8622: 8555: 8516: 8476: 8461: 8185: 8177: 8049: 7949: 7929: 7876: 7573: 7531: 7332: 7324: 7062: 6995: 6562: 6294: 5923: 5646: 3530: 1232: 961: 797: 565: 559: 83: 38: 9278: 8853: 8500: 8453: 8238: 8083: 7776: 7597: 7258: 7254: 7097: 7011: 6866: 6715: 4109: 3336: 3064: 2847: 2507: 2470: 1309: 1121: 671: 9794: 9779: 9460: 9308: 8531: 9717: 9484: 9332: 8809: 8674: 6546:). These sea urchins are the most abundant echinoderms on local lithiolid reefs. 17: 9507: 8705: 7701: 7636: 7619:

Ettaki, M; Ouahhabi, B.; Dommergues, J. L.; Meister, C.; Chellaï, E. H. (2011).

6878: 6861: 6856: 6847: 6464: 3558: 2999: 2705: 1093: 830: 58: 9682: 9523: 8029: 7841: 7438: 6821:

The Major Vegetational distribution was compared with the modern inland of the

6601: 5998: 932: 9216: 9084: 8614: 7262: 6663: 6543: 6539: 6513: 6171: 6063: 5725: 5580: 5510: 5308: 5072: 5010: 4939: 4880: 4805: 4717: 4654: 4598: 4550: 4496: 4448: 3946: 3808: 3547: 3229: 3170: 2985: 2925: 1228: 1163: 1143: 1097: 1085: 965: 881: 850: 793: 781: 655: 600: 546: 538: 393: 248: 127: 103: 68: 9826: 9531: 9492: 9340: 9021: 8969: 8909: 8563: 8508: 8298: 8274: 8122: 7884: 7849: 7711: 7605: 3466:

Reconstruction d'un ichnofosil de Skolithos, avec une possible faune associée

945:

represents mostly fluvial-aluvial under arid to humid climate similar to the

373: 360: 334: 321: 9506:

Krencker, François-Nicolas; Lindström, Sofie; Bodin, Stéphane (2019-08-29).

8290: 7207: 7155: 7079: 7066: 6826: 6620: 6261: 6122: 5776: 5363: 3860:. These solitary corals were observed throughout the lower unit biostromes. 3663: 3588: 3553: 3454: 3405: 3235: 3150: 3143: 2937: 2902:

family. This genus is the dominant type of fossil algae found in biozone A (

1247: 1196: 1116: 1089: 992: 973: 687: 279: 108: 52: 7572:

Krencker, F.-N.; Fantasia, A.; El Ouali, M.; Kabiri, L.; Bodin, S. (2022).

1257:

In the Middle Toarcian the eastern and north-eastern part of High Atlas of

8927: 7162:, which usually accounts for more than 60.95% of the palynomorphs present 8951: 8074: 7328: 6839: 6835: 6625: 5569: 5269: 4057: 3653: 3540: 3349: 3132: 1672: 1236: 1224: 1155: 1012: 969: 679: 675: 659: 635: 631: 627: 542: 530: 510: 506: 98: 93: 78: 73: 63: 46: 42: 9739:

Pantić, N. K. (1952). "Liassic flora from Budos mountain - Montenegro".

9140:

Bulletin de l'Institut Scientifique, Rabat, Section Sciences de la Terre

8960: 8900: 8104:

Ibouh, H.; El Bchari, F.; Bouabdelli, M.; Souhel, A.; Youbi, N. (2001).

8050:"Tectonic shortening and topography in the central High Atlas (Morocco)" 646:

in the Paleozoic; syn-rift, that was developed mostly between the Late

8875: 6481: 5692: 3672: 3536: 3243: 2992: 2929: 1301: 1167: 1159: 1061: 1008: 946: 855: 817: 813: 804: 647: 550: 411: 113: 88: 8891: 8989: 4661:

indicates the Toarcian Serpentinus zone and base of the Bifrons zone

3563: 1081: 1000: 692: 643: 522: 9013: 2958: 622:

Geological map of the Central High Atlas and main structural domains

7015:, example of Unkomasiaceae plant with associated Alisporites Pollen 2924:

rarely occur in the middle of the unit with associated echinodems (

7072: 6851: 6722: 6549: 6246: 5997: 5786: 5731: 4723: 4097: 3952: 3763: 3671: 3570: 3461: 3335: 3242: 3158: 2963: 2933: 1276: 1151: 1147: 1066: 1004: 770: 617: 587:(deposited in a subtidal to inner platform environment) & the 8205: 8048:

Teixell, A.; Arboleya, M. L.; Julivert, M.; Charroud, M. (2003).

2921: 1138:

Within the Trafraout Formation, facies comprising "lithiotids" (

807:

and Azilal province maps) the local laguno-marine facies of the

785: 683: 6825:. In the Beni Mellal-Azilal areas paleosols show abundance of 9656:"A basal sauropod dinosaur from the Early Jurassic of Morocco" 7727:"Les dinosaures du Maroc–aperçu historique et travaux récents" 630:

shortening and inversion of a rift that developed between the

9795:"Bivalve mounds and reefs of the Central High Atlas, Morocco" 6830:

as abundant infra-centimeter plant debris composed mostly by

7725:

Ibrahim, N.; Sereno, P. C.; Zouhri, S.; Zouhri, S. (2017).

6881:). Other coeval flora includes the plants recovered on the 6467:(Ostracoda). Present with large accumulations of specimens 8988:

Pierre, A.; Durlet, C.; Razin, P.; Chellai, E. H. (2010).

6796:

Marine or brackish bony fish of the family Leptolepidae.

2659:. Dominant genera on some layers of the Lias Delta Stage. 1189:

Gervilleioperna, Mytiloperna, Lithioperna and Cochlearites

1142:

aberrant reef-forming bivalves), which are known from the

1131:

sp., all deposited on diagenetic mudstone. Concretely, on

7706:. Selbstverlag Fachbereich Geowissenschaften, FU Berlin. 7439:"Carte Géologique du Maroc au 1: 100.000, feuille Azilal" 6628:" and others are associated with abundant plant remains. 6591:

Complete specimens and isolated parts of the exoskeleton

6535:

Complete specimens and isolated parts of the exoskeleton

682:

strata, there was a great deposition of marine shales as

1178:, restricted to intertidal and shallow-subtidal facies. 972:

or vertebrates) and the sedimentary figures (impacts of

553:. The Group represents the remnants of a local massive 6714:

Marine, brackish or freshwater bony fish of the family

1064:), hosting active erosion on sparsely vegetated soils. 9190:

Thèse de 3ième cycle, Université Cadi Ayyad, Marrakech

826:

marine-based as marks the Aguerd-nˈTazoult Formation.

9461:"Ammonites du Toarcien du Haut Atlas central (Maroc)" 7816:

Ettaki, Mohammed; Chellaï, El Hassane (2005-07-01).

4994: