Aganane Formation
| Aganane Formation | |
|---|---|
| Stratigraphic range: Pliensbachian ~ | |
 Exposed lagoonal sequences of the Aganane Formation in South Todhra | |
| Type | Geological formation |
| Unit of | High Atlas |
| Underlies | |
| Overlies | |
| Area | Central High Atlas |
| Lithology | |
| Primary | Limestone, dolomite |
| Other | Sandstones, Claystone, Shale, Conglomerate |
| Location | |
| Coordinates | 31°36′N 6°24′W / 31.6°N 6.4°W |
| Approximate paleocoordinates | 25°54′N 4°18′W / 25.9°N 4.3°W |
| Region |
|
| Country |  Morocco |
| Type section | |
| Named for | Aganane Village, near Tizouggaghiyn |
  Aganane Formation (Morocco) | |
The Aganane Formation (also know as Calcaires de Tizi Nehassa in the Middle Atlas[1]) is a Pliensbachian (Early Jurassic), with some levels being potentially Latest Sinemurian, geologic formation in the Khenifra, Azilal, Béni-Mellal, Ouarzazate, Tinerhir and Errachidia areas, in the Middle & High Atlas of Morocco, being the remnant of a local massive Carbonate platform, and known mostly for its rich tracksites (up to 1350 tracks in 1988) including footprints of thyreophoran, sauropod and theropod dinosaurs.[2][3][4] It may also include the fossiliferous levels of the Calcaires du Bou Dahar, if true, it would be one of the richest Early Jurassic formations in the entire tethys area.[5]
This formation has been dated to the Pliensbachian stage of the Lower Jurassic, thanks to the find of the ammonite Arieticeras cf. algovianum, indicator of Middle Domerian (=Uppermost Pliensbachian) in the upper zone, and lower delimitation by the foraminifers Mayncina termieri and Orbitopsella praecursor (indicators of Carixian=Lower Pliensbachian age).[6] The dinosaur tracksites are all located a few metres below the Pliensbachian-Toarcian limit, being coeval and connected with the lowermost layers of the continental Azilal Formation. The Aganane Formation was also coeval with the Jbel Taguendouft Formation and the Tamadout 1 Formation, all developed along a local "platform-furrow" in the Middle Atlas Mountains, that act as a barrier controlling the western border of the Jurassic Atlas Gulf.[7] The nearshore sections, including both carbonate platforms and close to sea terrestrial facies where located on an isolated internal domain thanks to the control of the barrier, allowing the Aganane Formation to develop on a hot and humid climate, where a local algal marsh had intermittent progradations, intercalated with a layer of terrigenous continental origin.[7] The ichnosites were developed in tidal flats and coastal deposits suitable to sea flooding.[8]
The Aganane Formation is a member of the Pliensbachian facies section of the Central Atlas, which are distributed from west to east: The Aït Chitachen Formation & Aït-Bazzi Formation at Demnate (continental-fluvial, coastal lagoon), the Aganane itself at Azilal.[8] At Tazoult, part of the Azilal profile contacts the bottom with the karst Talmest-Tazoult Formation, then a section where the Aganane itself indicates an eastward expansion of the carbonate facies, finally, the most recent Pliensbachian strata belong to the Amezraï Formation (Intertidal to coastal marine), this last change being the result of a transgression where we see a westward advance of the Imilchil pelagic facies, mostly part of the Jbel Choucht Formation.[8]
At Tazoult, the presence of a Diapir (the Tazoult salt wall) is remarkable. In the Pliensbachian, this area begins with the deposition of the Talmest-Tazoult Formation, and then is invaded from the west by the shallow marine carbonate platform of the Aganane Formation.[9] At this time, a decrease in the growth rate of the diapir is detected compared to the Sinemurian. In fact, with the eastward extension of the Aganane Formation, the Tazoult salt wall registers a major change towards shallower facies, confirming a higher diapir relief and a decrease in water depth towards this area during the Pliensbachian, not excluding a complete stop of diapir activity in this interval.[9]
Paleoenvironment
[edit]
During the Pliensbachian, the region was situated at a nearly tropical paleolatitude and marked the western boundary of the ancient "Atlas Gulf," which faced the Tethys Sea to the East. The Aganane Formation is characterized as representing the coastal-shallow sector of a massive carbonate platform, the most important Lower Jurassic platform in the area.[4][10]
The Carbonates of this unit were subjected to an examination of the diagenetic characteristics, where changes in the surface environment were consistently reflected in a sequence of rocks by diagenetic characteristics, maybe a tentative correlation of major events, such as Hurricanes.[11] The carbonate rocks that form the massive "Aganane Platform" are clearly influenced by tidal and shallow marine flows, ascribed to three environments: supratidal, intertidal and subtidal.[12]
The supratidal sector was diverse, including continental deposits with abundant quartz-rich cricundant deposits and fluvial channels, as well as others composed of considerable thicknesses of stratified gypsum and chicken-wire cargneules, lime and dolomite shales and marls, with drying cracks, caliche crusts and vadose pisoliths. These sediments suggest a continental zone bordering river courses, connected to coastal sectors where shales and siltstones derived from Sabkhas in which interstitial evaporites were formed.[13][10] To the north of the Demnate fault, there existed an extensive subsiding tidal flat where carbonate deposits containing gypsum remnants and stromatolitic laminites formed, interspersed with desiccation polygons.[14] Here the Aganane beds were bounded to the west by the Aït-Bazzi & Aït Chitachen Formations, which represent environments ranging from fluvial to coastal lagoons, with palynological residues Corollina quezelii & Corollina yvesi (Cheirolepidiaceae) as dominant, indicating an arid environment, accompanied by Cupressacites oxycedroides & Diadocupressacites moghrebiensis, both palynological residues of Cupressaceae.[15] Along the Demnate fault's edge, active during this period, lignite layers were intercalated, likely resulting from the degradation of forests located to the south, indicated by root traces in sandstones at the base of the Aït-Bazzi Formation in Aït Tioutline. The area was inhabited by both herbivorous and carnivorous dinosaurs that roamed the expansive coastal marshland.[14]
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Intertidal deposits are composed of algal laminates, bioturbated pelletiferous shales, uniformitarian shales and wackestones with disruptive channels and storm sequences. Algal laminated Boundstones developed in both supratidal and intertidal zones, following present-day patterns such as Shark Bay in Australia or the Persian Gulf. Whereas the pelletoid lime packstone/wackestone facies most likely represented tidal flat areas, or analogs to modern coastal mangrove growth.[13][10] Towards the east, excluding the Demnate region, gypsum precipitated in sebkhas along the edge of a low continent, indicative of a possibly arid climate. Additionally, more massive facies with large lamellibranchs separated the tidal flat from the open sea with Ammonites, whose western extension bordered the eastern edge of Azilal.[14]
Subtidal deposits include both those of an intertidal nature, indicating shallow water or coastal lagoons, with extensive accumulations of skeletal lime packstones, oolitic tidal deltas and offshore bars, oncoliths and coral reefs, and occasional bivalves Opisoma spp. While further east the more open subtidal conditions are represented by flint-bearing calcareous shales and sparse faunas where ammonites begin to appear.[10][13]
The Carbonate Facies of the High Atlas Pliensbachian generally have a low bathymetry. They show a notable evolution from east to west from a lagoon-marine facies to brackish facies. At the level of the Azilal Atlas, the Middle Lias occurs on both sides of the Demnat Fault: to the southwest of the fault, the Aït Bazzi Formation with dolomitic and red marly facies (lagoonal and lagoon-evaporitic facies), while to the northeast develop the thicker facies of the Aganane Formation.[16] In this area, formations of this stage begin either with conglomeratic facies associated with red marls or with scree and conglomerates associated with local erosion, recovering the same lower Pliensbachian emersion phase observed in the Beni-Mellal Atlas.[16] Toward the south, the "basin" facies ends at the bottom of the gulf near the Jbel Oukarde accident, at the western end of the Tilougguit syncline. The southern limit of this basin, hidden by the later sediments, corresponds to the present-day course of the Azilal-Anergui submeridian fault. Towards the south, on the Amezraï and Aït Bouguemmez basins, a platform zone was established in the heart of the Central High Atlas, consisting of the Jbel Choucht, Aganane, Assemsouk, and Amezraï formations.[16] The Jbel Choucht Formation is the type locality here, characterized by a great development of coralligenous facies. The Jbel Choucht Formation is also present towards the north-central High Atlas, but without any reef character, being rather rich in Megalodontoidea bivalves, while the Aganane Formation presents more or less the same characteristics as those described in the Beni-Mellal Platform. To the east, at the level of the Jbel Aroudane, the thickening and sedimentary polarity of the Jbel Choucht Formation occurs this time southward, with a W-E subsident basin centered on the Jbel Azourki and the Jbel Aroudane.[16]
Locations such as Ait Athmane recover the typical Sinemurian-Pliensbachian mediterranean lithiotid bivalve reefs, composed by aggrupation of aberrant bivalves.[17] These "Reefs" had a strong zonation, starting with the bivalves Gervilleioperna and Mytiloperna, restricted to intertidal and shallow-subtidal facies. Lithioperna is limited to lagoonal subtidal facies and even in some low-oxygen environments. Finally Lithiotis and Cochlearites are found in subtidal facies, constructing buildups.[18] Locally, these reefs were developed as shallow subtidal, cross-bedded floatstones, later evolving to layers with evidence of subaerial exposure, including lagoonal marls, and bioturbated red mudstones with root traces and calcrete.[17] These layers are abundant on the aberrant bivalves Lithioperna and Cochlearites, as well common corals, gastropods, the bivalve Opisoma and oncoids, all living in a sheltered lagoon in the interior of the local carbonate platform, similar to the Rotzo Formation of the Trento Platform.[17]
Depositional settings
[edit]
The lower and middle parts of the Aganane Formation mainly consist of light gray dolomitic limestone, often with a rhythmic layering. This environment represents a shallow, coastal area similar to modern tidal flats where seawater periodically covered the land during high tides. Areas like Ait Athmane record rhizoliths (including massively rooted levels), tree trunks and pisoids, which are indicative of pedogenic or freshwater vadose conditions with periodic exposure to air and fresh water.[17][19] A significant portion of this environment was influenced by coastal lagoon and supratidal plains, areas only occasionally submerged by the sea.[20] Red and white marls mixed with thin dolomite layers suggest periods of exposure to the air, with sediments deposited by rivers and occasional flooding from the sea. This setting is comparable to the modern Persian Gulf's sabkha environments, where salt flats and shallow waters mix. Evidence of land exposure includes features like mudcracks and evaporite crystals. Occasional storm events likely washed in marine sediments, indicated by brecciated layers (broken rock fragments). Dinosaur footprints found in these layers suggest a nearby vegetated land area with sufficient rainfall to support life, and thus high annual precipitation, suggesting overall tropical conditions reminiscent of the modern Andros Island model in the Bahamas.[20]
Further offshore, the platform transitioned into a more open lagoon setting, where shallow marine conditions dominated. The rocks here include mud-rich limestones and dark biodetrital limestones (formed from broken fossil fragments). This part of the formation often shows signs of marine life, including llamellibranchs, gastropods, brachiopods, with calcareous algae (Palaeodasycladus, Solenopora, etc.) oncoliths and Foraminifers. Some layers contain large shells of bivalves like Lithiotids, occasionally forming shell beds. These shell accumulations and their arrangement suggest the influence of tidal currents, creating small channels within the lagoons. The presence of gray, organic-rich sediments indicates a low-oxygen, calm-water environment where fine carbonate mud accumulated.[20][21]
In the more open, wave-exposed parts of the platform, the sediment becomes coarser and contains reef-related deposits. These deposits include bioclastic limestones (composed of broken shells and coral fragments) with large coral colonies and sea urchins. The corals likely formed small patch reefs, protecting the inner platform from strong wave action. The transition between these reef zones and the inner platform was gradual, with occasional storm events depositing coarse sediments into the quieter lagoon areas. This reef barrier acted as a natural protection for the lagoon, allowing finer sediments to accumulate behind it.[20]
Small cycles within the bank with frequent reworking and/or rearrangement phenomena demonstrate the importance of episodic storms, which repeatedly led to the displacement of individual facies zones.[3] The only slightly consolidated bottom of the extensive, shallow lagoon areas was repeatedly reworked, with thicknesses of 2-4 meters are characteristic of restrictive lagoonal berelches in the lee of offshore bars or reef belts. The asymmetric large cycles are interpreted, with some reservations, as regressive cycles in connection with global sea level fluctuations and regional tectonic development.[3]
At Ait Bou Guemmez, the upper Aganane Formation records the development of a lagoonal environment south of the Jbel Tizal-Jbel Azourki accident, which evolves to a more or less open subtidal platform environment north of this accident.[22] The local transgressive procession is marked by the dominance of subtidal facies with a microfauna of biozone C1, whereas the high marine level procession is represented by a succession of intertidal to supratidal dolomitic limestones, its top is surmounted by an important subaerial discontinuity materialized by red clay with paleosols and abundant plant roots (e.g. at Tizi n'Terghist).[22] In other localities are mainly biodetritic limestones, showing emersion structures at their top (dolomitization, mud cracks, roots and plant remains, footprints of Dinosaurs).[22]
Paleogeography
[edit]
The Aganane Formation is located largely within the "Grand e Accident du Nor d'Altasien" or North Atlas Fault, the largest and most important of the Central High Atlas faults.[10] During the late Pliensbachian, 200 m of carbonate sediments accumulated south of the fault on an overturned block, while to the north more than 700 m of similar material accumulated.[10] This fault line probably marked the northern boundary of a Paleozoic basement peninsula that advanced eastward from the Tichka Massif into the Atlas Trench.[10]
The paleogeographic evolution of our region can be described in three main stages:
- The Lower Pliensbachian ("Carixian"), which follows the typical Sinemurian paleogeographic pattern with foreshores and prolonged emersion facies (paleosols, karsts and teepee-shaped structures), the latter being mainly observed on the southern slopes of the central High Atlas, evolving on the subtidal platform of the Upper Sinemurian, with the "Lithiotidae" colonizing for the first time the main areas located in line with the active accidents, notably the fault located NE-SW, separating the Tilougguit trough to the SE from its limiting platform to the NW.[16]
- The "middle" Pliensbachian ("Carixian" - lower "Domerian") marine environment gradually resettles along the western edge of the High Atlas Basin, with maximum opening of depositional environments in the Carixian-Domerian transition (rhythmic mamocalcic sedimentation in the Tilougguit Trench, turbidite facies on the SE edge of the Beni-Mellal platform and subsident lagoons in the other sectors). At the same time, the NW-SE-trending Demnat Fault and the N70-trending North Atlas Fault become evident, whereas the southern edge of the Telouet Graben does not appear to have changed significantly during the Middle Lias like its counterpart in the northern part of the range, being here the main site of the shallow sedimentation of the Aganane Formation.[16] Towards the Tincghir meridian, open sea facies are encountered.[16]
- The last facies belong to the Upper Pliensbachian (Upper Domerian) where the paleogeography of the Central High Atlas becomes very contrasted, with emersion of a vast sector of the platform (At Demnat), leading to the development of paleosols and karst and the accumulation of lignite deposits along tectonically active faults.[16] At the same time, there is a filling of the Tilougguit ditch by carbonate and terrigenous sedimentation, showing small basins like Tamadout and Taquat N'Agrd with a sedimentation with a gravity component, and shoals (Jbel Taguendouft) with condensed deposits.[16] Finally an intensification of the activity of the North leading to the deepening of the central platform (creation of the new basin of Amezraï), to the individualization of strongly subsident zones in the aplomb of this accident (gutter of Jbel Azourki-Jbel Aroudane) and to the birth of the first wrinkles in the center of the high-Atlasic basin.[16]
Foraminifera
[edit]Local Foraminifers have been the major reference to stablish the local different enviromental settings, as it´s distribution is clearly based on cyclic sedimentary evolution: the base banks "Term A" represents a shallow subtidal setting with rich thanatocoenosis of Siphovalvulina, Mayncina or Orbitopsella, associated with a intensely bioturbated environment, analogous to present Bahamas, Florida or Persian Gulf.[20] In the Aganane type section limestone beds (biopelmicrite) rich in Orbilopsella, Haurania or Pseudopfenderina could be interpreted as brought by tidal currents covering the supratidal zone. In "Term B" a thanatocoenosis of monospecific Foraminifera with Mayncina termieri, Pseudopfenderina or Lituosepta compressa are common, interpreted as allochthonous, resulting from sorting in an intertidal environment higher than supratidal, under or alternated with the supratidal laminations and the storm breccias, as well in rarer cases covering (aeolian origin?) surface of the supratidal coastal plain.[20] The Aganane Foraminifera in Terms "D" and "E" underwent significant evolutionary and environmental changes.[23] During D, the foraminiferal population was dominated by Planisepta, a smaller morphovariant of Lituosepta, which persisted after the decline of larger orbitopsellids like Orbitopsella due to internal biological factors and mechanical instability related to their large size. The population remained stable until the Middle Domerian anoxic crisis, which triggered a microfaunal turnover. E saw the emergence of smaller, simpler foraminifera such as Haurania gracilis and Paleocyclammina liasica, adapted to eutrophic lagoon conditions.[23]
| Genus | Species | Stratigraphic position | Material | Habitat | Notes | Images |
|---|---|---|---|---|---|---|
| Ammobaculites[1] |
|
|
Isolated Tests/Shells | Lagoonal | A foraminifer of the Ammomarginulininae family. | |
| Dentalina[19] |
|
|
Isolated Tests/Shells | Lagoonal | A foraminifer of the Nodosariinae family. | |
| Eariandia[14] |
|
|
Isolated Tests/Shells | Marine or Lagoonal | A foraminifer of the family Earlandiidae. | |
|
|
Isolated Tests/Shells |
Marine or Lagoonal |
A foraminifer of the Everticyclamminidae family. It represents a species similar to E. virguliana, known from the Middle Jurassic of Morocco. |
||
| Glomospira[14][25] |
|
|
Isolated Tests/Shells | Lagoon | A foraminifer of the family Ammodiscidae. | |
| Glomospirella[25] |
|
|
Isolated Tests/Shells | Lagoon | A foraminifer of the family Ammovertellininae. | |
| Haurania[14][23] |
|
|
Isolated Tests/Shells | Marine or Lagoonal | A foraminifer of the family Spirocyclinidae. | |
|
|
Isolated Tests/Shells |
Marine or Lagoonal |
A foraminifer of the Mesoendothyridae family. |
||
|
|
Isolated Tests/Shells |
Marine or Lagoonal |
A foraminifer of the Nezzazatoidea family. |
||
|
|
Isolated Tests/Shells |
Marine or Lagoonal |
A foraminifer of the Mesoendothyridae family. |
||
| Nodosaria[25] |
|
|
Isolated Tests/Shells | Lagoonal | A foraminifer of the family Nodosariinae. | |
| Ophtalmidium[25] |
|
|
Isolated Tests/Shells | Lagoonal | A foraminifer of the family Ophthalmidiidae. | |
|
|
Isolated Tests/Shells |
Marine or Lagoonal |
A foraminifer of the Mesoendothyridae family. |
||
| Planisepta[25] |
|
|
Isolated Tests/Shells | Lagoonal | A foraminifer of the Mesoendothyridae family. | |
|
|
Isolated Tests/Shells |
Marine or Lagoonal |
A foraminifer of the Pfenderinidae family. |
||
|
|
Isolated Tests/Shells |
Marine or Lagoonal |
A foraminifer of the Pfenderinidae family. |
||
|
|
Isolated Tests/Shells |
Marine or Lagoonal |
A foraminifer of the Pfenderinidae family. |
Invertebrata
[edit]Ichnofossils
[edit]| Genus | Species | Location | Material | Type | Made by | Images |
|---|---|---|---|---|---|---|
|
|
Borrowing Traces |
Domichnia |
|
 | |
| Asterosoma[26] |
|
Bulb-like swelling burrows | Fodinichnia |
|
||
|
Tubular Fodinichnia |
Fodinichnia |
|
|||
|
Tubular Fodinichnia |
Fodinichnia |
|
 | ||
| Cruziana[26] |
|
Ribbon-like furrows | Repichnia and/or fodinichnia |  | ||
| Gastrochaenolites[26] |
|
clavate-shaped to flask-shaped tubes | Domichnia |
|
 | |
| Glossifungites[26] |
|
Infilled abandoned burrows | Domichnia and/or fodinichnia. | |||
| Ophiomorpha[26] |
|
Tubular Fodinichnia | Domichnia and/or fodinichnia. |
|
 | |
|
Tubular Fodinichnia |
Domichnia and/or fodinichnia. |
|
 | ||
|
Cylindrical to subcylindrical burrows |
Domichnia |
|
 | ||
|
Tubular Fodinichnia |
Fodinichnia |
|
 | ||
| Teichichnus[26] |
|
Vertical to oblique burrows | Fodinichnia |
|
||
|
Dwelling traces |
Domichnia & Fodinichnia |
|
 |
Anthozoa
[edit]The Reef facies of the Aganane Formation featured a nearshore, tropical setting.[27] Dominant Plicatostylidae bivalves, in a way akin to modern Crassostrea, thrived in both clear and turbid waters, forming biostromes and bioherms in protected lagoons. Their growth outpaced sediment accumulation thanks to soft carbonate mud and their own fecal matter providing support. Fluctuating water depths influenced habitat suitability, with lithiotids adapting to shallow subtidal environments. Co-existing scleractinian corals, possibly photosymbiotic, suggest warm, clear, oligotrophic conditions, yet their symbiotic nature is hard to confirm in fossils. These corals were sensitive to changes in environmental parameters like temperature and salinity.[27]
| Genus | Species | Stratigraphic Position | Material | Notes | Images |
|---|---|---|---|---|---|
| Actinastreidae[27] | Indeterminate |
|
Colonial Imprints | Thamnasterioid corals |  |
|
|
Imprints |
A solitary coral of the family Stylinidae. |
||
|
|
Imprints |
A solitary coral of the family Zardinophyllidae. Late Pliensbachian corals of the Aganane Formation are mainly limited to Retiophyllia, Thamnasteria and Archaeosmilia. |
||
|
|
Colonial Imprints |
A coral of the family Archaeosmiliidae. |
||
| Eocomoseris[27] |
|
|
Colonial Imprints | A thamnasterioid coral of the family Archaeosmiliidae. | |
| Icaunhelia[27] |
|
|
Imprints | A solitary coral of the family Archaeosmiliidae | |
|
|
Colonial Imprints |
A coral of the family Oppelismiliidae. |
||
| Paleomillepora[27] |
|
|
Colonial Imprints | A plocoid coral of the family Spongiocoenia | |
|
|
Colonial Imprints |
A coral of the family Stylophyllidae. |
||
|
|
Colonial Imprints |
A coral of the family Dermosmiliidae. |
||
|
|
Colonial Imprints |
A coral of the family Latomeandridae. |
||
| Proleptophyllia?[27] |
|
|
Imprints | A solitary coral of the family Dermosmiliidae | |
| Reimaniphyllidae[27] | Indeterminate |
|
Imprints | Solitary corals | |
|
|
Colonial Imprints |
A coral of the family Reimaniphylliidae. It belongs to the otherwise common Triassic genus Retiophyllia. |
||
| Stylophyllidae[27] | Indeterminate |
|
Colonial Imprints | Phaceloid corals | _(Jurassic;_Weymouth,_England)_(35396422650).jpg) |
|
|
Colonial Imprints |
A thamnasterioid coral of the family Thamnasteriidae. |
 |
Porifera
[edit]| Genus | Species | Stratigraphic position | Material | Habitat | Notes | Images |
|---|---|---|---|---|---|---|
|
|
Colonial Imprints |
Marine or Lagoonal |
An Axinellidan demosponge of the family Cladocoropsidae. Fossils of this and other unidentified sponges are commonly found in reef deposits, associated with corals. |
||
| Stylothalamia[31] |
|
|
Colonial Imprints | Marine or Lagoonal | A Dictyoceratidan demosponge of the family Verticillitidae |
Crustacea
[edit]| Genus | Species | Stratigraphic position | Material | Habitat | Notes | Images |
|---|---|---|---|---|---|---|
| Favreina[14][20] |
|
|
Coprolites | Marine, Tidal Flat or Lagoon | Crustacean fossil coprolites, assigned to the ichnofamily Favreinidae. Possibly coprolites of taxa similar or belonging to Thalassinidea |  |
|
|
Coprolites |
Marine, Tidal Flat or Lagoon |
Crustacean fossil coprolites, assigned to the ichnofamily Favreinidae. Possibly coprolites of taxa similar or belonging to Thalassinidea |
Brachiopoda
[edit]| Genus | Species | Stratigraphic position | Material | Notes | Images |
|---|---|---|---|---|---|
|
|
Isolated Shells |
A Brachiopodan of the family Cirpinae. Relatively abundant on seashore deposits. It was originally identified as part of the genus Rhynchonella |
||
| Gibbirhynchia[1][33][34] |
|
|
Isolated Shells | A Brachiopodan member of the family Tetrarhynchiidae | |
| Grandirhynchia[35] |
|
|
Isolated Shells | A Brachiopodan member of the family Tetrarhynchiidae | |
|
|
Isolated Shells |
A Brachiopodan of the family Zeilleriidae |
||
| Liospiriferina[1][33][34] |
|
|
Isolated Shells | A Brachiopodan of the family Spiriferinidae |  |
| Lobothyris[34] |
|
|
Isolated Shells | A Brachiopodan of the family Lobothyrididae | |
| Parathyridina[34] |
|
|
Isolated Shells | A Brachiopodan of the family Zeilleriidae. A taxon living on the inner carbonate platforms rarely communicating with the open sea. | |
|
|
Isolated Shells |
A Brachiopodan of the family Spiriferinidae |
Bivalves
[edit]| Genus | Species | Stratigraphic position | Material | Notes | Images |
|---|---|---|---|---|---|
|
|
Isolated Shells |
A saltwater bivalve of the family Mytilidae. |
||
|
|
Isolated Shells |
A saltwater bivalve of the family Plicatostylidae. A large bivalve, with a subequal shell, that can reach 60–70 cm in height. It is one of the three principal bivalves found on the Lithiotis facies, whose accumulations generally cover megalodontid coquinas. |
||
|
|
Isolated Shells |
A saltwater/brackish bivalve of the family Neomiodontidae. This genus is considered an opportunistic suspension feeder of shallow infauna, and the marker genus for brackish environments.[41] |
||
|
|
Isolated Shells |
A saltwater bivalve of the family Lucinidae. |
 | |
|
|
Isolated Shells |
A saltwater bivalve of the family Bakevelliidae. |
||
|
|
Isolated Shells |
A saltwater bivalve of the family Plicatostylidae. Abundant along the rootlets, indicating a very shallow and restricted lagoon or swamp environment |
||
| Gryphaea[17][19] |
|
|
Isolated Shells | A saltwater/brackish bivalve of the family Gryphaeidae |  |
|
|
Isolated Shells |
A saltwater bivalve of the family Gryphaeidae. This genus develops a noted material oyster biostrome at Aït Athmane, where a discontinuous, patchy layer is formed, developed under submarine lithification and a relative enrichment in terrigenous matter.[19] |
 | |
|
|
Isolated Shells |
A saltwater bivalve of the family Plicatostylidae. This genus was founded to be a bivalve with a juvenile byssate stage that developed different lifestyles in adulthood depending on the density of individuals and the firmness of the bottom |
 | |
|
|
Isolated Shells |
A saltwater/brackish bivalve of the family Lucinidae. Linked with intertidal settings |
 | |
| Megalodon?[39] |
|
|
Isolated Shells | A saltwater bivalve of the family Megalodontidae |  |
| Modiolus[13] |
|
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Isolated Shells | A saltwater bivalve of the family Mytilidae | .jpg) |
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Isolated Shells |
A saltwater bivalve of the family Plicatostylidae. |
||
| Nanogyra[17][19] |
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Isolated Shells | A saltwater/brackish bivalve of the family Gryphaeidae | |
|
|
Isolated Shells |
A saltwater/brackish bivalve of the family Astartidae. Is considered a genus that evolved from shallow burrowing ancestors, secondarily becoming an edge-lying semi-fauna adapted to photosymbiosis.[42] |
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|
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Isolated Shells |
A saltwater bivalve of the family Pachyrismatidae |
||
|
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Isolated Shells |
A saltwater bivalve of the family Pectinidae |
 | |
|
|
Isolated Shells |
A saltwater bivalve of the family Pholadomyidae |
 | |
| Plagiostoma[17][19] |
|
|
Isolated Shells | A saltwater/brackish bivalve of the family Limidae |  |
|
|
Isolated Shells |
A saltwater bivalve of the family Pachyrismatidae |
Gastropoda
[edit]| Genus | Species | Stratigraphic position | Material | Notes | Images |
|---|---|---|---|---|---|
| Ceritella[34] |
|
|
Isolated Shells | A saltwater gastropod of the family Ceritellidae | |
|
|
Isolated Shells |
A saltwater gastropod of the family Nerineidae. Local specimens appear to have algal material on the shells, indicating a restricted lagoon environment. |
 | |
|
|
Isolated Shells |
A saltwater gastropod of the family Nerineidae |
||
|
|
Isolated Shells |
A saltwater gastropod of the family Nerineidae. "Scurria" was found in the Assemsouk structure on a "Cochlearites" valve and a shallow ovoid excavation, similar to the resting trace of a limpet, was found inside a transported "Lithiotis". |
 |
Ammonites
[edit]| Genus | Species | Stratigraphic position | Material | Notes | Images |
|---|---|---|---|---|---|
|
|
Isolated Shells |
An ammonite of the family Hildoceratidae. Arieticeras cf. algovianum is indicative of the Middle Domerian (Upper Pliensbachian) in the upper zone |
 | |
|
|
Isolated Shells |
An ammonite of the family Hildoceratidae |
||
| Fuciniceras[6] |
|
|
Isolated Shells | An ammonite of the family Hildoceratidae | |
| Galaticeras[6] |
|
|
Isolated Shells | An ammonite of the family Lytoceratidae | |
| Lioceratoides[6] |
|
|
Isolated Shells | An ammonite of the family Hildoceratidae | |
| Protogrammoceras[6] |
|
|
Isolated Shells | An ammonite of the family Hildoceratidae | |
|
|
Isolated Shells |
An ammonite of the family Amaltheinae |
 | |
| Reynesoceras[6] |
|
|
Isolated Shells | An ammonite of the family Dactylioceratidae |
Annelida
[edit]| Genus | Species | Stratigraphic position | Material | Habitat | Notes | Images |
|---|---|---|---|---|---|---|
|
Indeterminate |
|
Isolated or accumulated tubes |
Marine or Lagoonal |
A sessile Annelid of the family Serpulidae. These annelids are found as well in the reef facies as in the lagoon deposits |
 |
Dinosauria
[edit]Theropoda
[edit]| Genus | Species | Stratigraphic position | Material | Notes | Images |
|---|---|---|---|---|---|
|
|
Footprints |
Incertae sedis within Neotheropoda, maybe ceratosaur tracks. Includes the large tracks.[46][45] |
 | |
| Indeterminate |
|
Footprints |
incertae sedis within Theropoda. 64 footprints of medium to large (30-55 cm) theropods referred as "Morphotype 3", some with resemblance to Allosauroid pes (Megalosauripus? ispp.).[46] |
 | |
|
|
Footprints |
Member of the ichnofamily Grallatoridae, incertae sedis within Theropoda. Up to 96 tracks of small theropods, referred originally to "Morphotype 1", and usually attributed to dinosaurs similar to Coelophysidae and Dilophosaurus. Includes didactyl, tridactyl and tetradactyl tracks, as well as pathologic trackways with evidence of limping.[2] Has been suggested to be tracks from tridactyl taxa under different conditions.[48] |
 | |
|
Footprints |
Type member of the ichnofamily Eubrontidae, incertae sedis inside Theropoda. Eubrontes is usually related to the genus Dilophosaurus, representing basal Neotheropods. The local record include up to 208 tracks, referred as "Morphotype 2".[43] |
 | ||
| Indeterminate |
|
Footprints |
Theropod Tracks of uncertain affinity or non studied |
Sauropodomorpha
[edit]| Genus | Species | Stratigraphic position | Material | Notes | Images |
|---|---|---|---|---|---|
|
|
Footprints |
Incertae sedis within Sauropoda. Includes traces with pes similar to Diplodocoidea, but also others that resemble basal sauropods.[54][55] |
 | |
|
|
Footprints |
Incertae sedis within Sauropodomorpha. Described as the "Morphotype 1" Includes traces with pes similar to those of basal quadrupedal forms like Blikanasaurus or Melanorosauridae.[55] Referred to quadrupedal taxa such as Gongxianosaurus.[45] Alternatively, the tracks, or some of them, can belong to the ichnogenus Lavinipes.[56] |
||
|
|
Footprints |
Type member of the ichnofamily Otozoidae, incertae sedis within Sauropodomorpha. Includes a gigantic 84 or 75 cm track that represents the largest Otozoum ever described in the literature.[57][58] |
 | |
|
|
Footprints |
Typical member of the ichnofamily Parabrontopodidae, incertae sedis within Sauropoda. Includes tracks with pes similar to those of Vulcanodon (perhaps left by Tazoudasaurus?) and other morphotype more similar to Rhoetosaurus.[55] |
 | |
|
|
Footprints |
Incertae sedis within Sauropodomorpha. |
 | |
| Indeterminate |
|
Footprints |
Sauropodomorph tracks of uncertain affinity |
||
| Indeterminate |
|
Footprints |
Sauropod tracks of uncertain affinity |
Ornithischia
[edit]| Genus | Species | Location | Material | Notes | Images |
|---|---|---|---|---|---|
|
|
Footprints |
Incertae sedis inside Neornithischia. Due to its morphology, this tracks have been latter identified as possible Deltapodus, yet this does not mean they are of Stegosauria origin, but maybe belong to a basal Thyreophoran.[59] |
 |
Chlorophyta/Rhodophyta
[edit]| Genus | Species | Stratigraphic position | Material | Habitat | Notes | Images |
|---|---|---|---|---|---|---|
|
|
Calcareous Imprints |
Marine or Lagoonal |
A Green alga of the Halimedaceae or Udoteaceae family. |
 | |
|
|
Calcareous Imprints |
Marine or Lagoonal |
A Green alga of the Halimedaceae or Udoteaceae family. |
 | |
| Fanesella[19] |
|
|
Calcareous Imprints | Lagoonal | A Green alga of the Dasycladaceae family. | |
|
|
Calcareous Imprints |
Marine or Lagoonal |
A Green alga of the Dasycladaceae family. |
 | |
| Pseudolithocodium[20] |
|
|
Calcareous Imprints | Marine or Lagoonal | A Green alga, likely a member of the Ulotrichales group. Has been compared with the extant genus Gomontia | |
| Pycnoporidium[14] |
|
|
Calcareous Imprints | Marine or Lagoonal | A Red Alga of the family Solenoporaceae | |
|
|
Calcareous Imprints |
Marine or Lagoonal |
A Green alga alga of the Triploporellaceae family. This genus is the most common algal type found in the Biozone A (Lituosepta recoarensis). |
||
| Solenopora[60][36] |
|
|
Calcareous Imprints | Marine or Lagoonal | A Red Alga of the family Solenoporaceae |  |
| Terquemella[1] |
|
|
Calcareous Imprints | Marine or Lagoonal | A Green alga of the Bornetellaceae family. | |
|
|
Calcareous Imprints |
Marine or Lagoonal |
A Green alga of the Thaumatoporellales group |
Photo Gallery
[edit]-
Metric emersive cycle in the carbonate platform. Deposition of marine lagoon with foraminifera then dolomitized algal laminations in intertidal to supratidal environment. -
Desiccation cracks in a dolomitized limestone bench, emersive cycle top of the Lagoon -
Ammonites and belemnites displaced on the supratidal plain ("teepee") by a storm wave or a tidal current -
Storm breach at the top of a metric regressive sequence. -
Vadose pisoliths and "birdseyes" in coastal carbonate sand, emergent; outer shelf. -
Aerial, supratidal (vadose) diagenesis in a carbonate sand with foraminifera displaced by tidal currents and storm waves on the shelf. -
Thin layer: calcretes (calcareous crusts) reworked in a gravelly coastal sediment, partly dolomitized. -
Stalactite cement at the top of a "keystone vug" typical of diagenesis in a vadose environment, at the top of an emersive cycle (L=0.3 mm). -
Calcretes (calcareous crust) and "birdseyes" in a gravelly coastal sediment. -
Diagenetic structure in "teepee" on the supratidal plain, formed by the increase in volume of the sediment following the crystallization of carbonates (dolomite).
See also
[edit]References
[edit]- ^ a b c d e f g Benshili, Khadija (1989). "Lias - Dogger du Moyen-Atlas plissé (Maroc). Sédimentologie, biostratigraphie et évolution paléogéographique". Travaux et Documents des Laboratoires de Géologie de Lyon. 106 (1): 3–285.
- ^ a b c d Ishigaki, Shinobu; Lockley, Martin G. (March 2010). "Didactyl, tridactyl and tetradactyl theropod trackways from the Lower Jurassic of Morocco: evidence of limping, labouring and other irregular gaits". Historical Biology. 22 (1–3): 100–108. Bibcode:2010HBio...22..100I. doi:10.1080/08912961003789867. ISSN 0891-2963. S2CID 129632881.
- ^ a b c Hauptmann, Manfred (1990). "Untersuchungen zur Mikrofazies, Stratigraphie und Paläogeographie jurassischer Karbonat-Gesteine im Atlas-System Zentral-Marokkos". Selbstverlag Fachbereich Geowissenschaften, FU Berlin. doi:10.23689/fidgeo-6546.
- ^ a b Danisch, Jan; Kabiri, Lahcen; Nutz, Alexis; Bodin, Stéphane (2019-05-01). "Chemostratigraphy of Late Sinemurian – Early Pliensbachian shallow-to deep-water deposits of the Central High Atlas Basin: Paleoenvironmental implications". Journal of African Earth Sciences. 153: 239–249. doi:10.1016/j.jafrearsci.2019.03.003. ISSN 1464-343X.
- ^ MERINO-TOMÉ, ÓSCAR; PORTA, GIOVANNA DELLA; KENTER, JEROEN A. M.; VERWER, KLAAS; HARRIS, PAUL (MITCH); ADAMS, ERWIN W.; PLAYTON, TED; CORROCHANO, DIEGO (2011). "Sequence development in an isolated carbonate platform (Lower Jurassic, Djebel Bou Dahar, High Atlas, Morocco): influence of tectonics, eustacy and carbonate production". Sedimentology. 59 (1): 118–155. doi:10.1111/j.1365-3091.2011.01232.x. ISSN 0037-0746.
- ^ a b c d e f g h i Dubar, G.; Mouterde, R. (1978). "Les formations à ammonites du Lias Moyen dans Ie Haut Atlas du Midelt et du Tadla" (PDF). Notes & M. Servo Geo/. Maroc. 274 (4): 77.
- ^ a b Michard, A. (March 2011). "Nouveaux guides géologiques et miniers du Maroc/New Geological and Mining Guidebooks of Morocco, volume 7: Haut Atlas occidental, Haut Atlas central nord-ouest". Notes & M. Servo Geo/. Maroc. 562 (1–3): 70–76. Retrieved 1 April 2022.
- ^ a b c Jossen, J.A. (1988). "Carte geologique du Maroc au 11100 000: Feuille Zawyat Ahancal". Notes & M. Servo Geo/. Maroc. 335 (4): 23–31.
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- ^ a b c d e f g Lee, C. W.; Burgess, C. J. (1978). "Sedimentation and tectonic controls in the early Jurassic central High Atlas trough, Morocco". Geological Society of America Bulletin. 89 (8): 1199–1204. Bibcode:1978GSAB...89.1199L. doi:10.1130/0016-7606(1978)89<1199:SATCIT>2.0.CO;2. Retrieved 20 April 2023.
- ^ Burgess, C. J. (1979). "The development of a Lower Jurassic carbonate tidal flat, central High Atlas, Morocco; 2, Diagenetic history". Journal of Sedimentary Research. 49 (2): 413–427. Retrieved 20 April 2023.
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- ^ a b c d e Lee, C. W. (1976). "Facies and Faunistic Variation in the Middle Lias (Domerian) of the Central High Atlas Mountains, Morocco". Thesis University College of Swansea. 1 (1): 331.
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- ^ Courtinat, B.; Le Barrec, A. (1986). "Nouvelles donnees palynologiques sur les "Coaches Rouges" (Jurassique Moyen) de la Region de Demnat (Haut-Atlas,Moroc)" (PDF). Bulletin de l'Institut Scientifique, Rabat. 10 (2): 15–20. Retrieved 21 April 2022..
- ^ a b c d e f g h i j Souhel, A. (1996). "The Mesozoic in the High Atlas of Beni-Mellal (Morocco). Stratigraphy, sedimentology and geodynamic evolution" (PDF). Strata: Series 2, Memoirs. 27 (6): 1–227. Retrieved 12 May 2022..
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{{cite book}}: CS1 maint: multiple names: authors list (link) - ^ a b c Moussa, Masrour; Pérez-Lorente, Félix; Boutakiout, M.; Ladel, L.; Díaz-Martínez, I. (2010). "Nuevos yacimientos de icnitas domerienses en Ibaqalliwn (Aït Bou Guemez, Alto Atlas Central. Marruecos) [New Domerian dinosaur footprint sites from Ibaqalliwn (Aït Bou Guemez, Central High Atlas, Morocco)]" (PDF). Geogaceta. 48 (1): 91–94. Retrieved 1 April 2022.
- ^ Mudroch, Alexander; Richter, Ute; Joger, Ulrich; Kosma, Ralf; Idé, Oumarou; Maga, Abdoulaye (2011-02-14). "Didactyl Tracks of Paravian Theropods (Maniraptora) from the ?Middle Jurassic of Africa". PLOS ONE. 6 (2): e14642. Bibcode:2011PLoSO...614642M. doi:10.1371/journal.pone.0014642. ISSN 1932-6203. PMC 3038851. PMID 21339816.
- ^ Plateau, H.; Giboulet, G.; Roch, E. (1937). "Sur la présence d'empreintes de Dinosauriens dans la région de Demnat (Maroc) [On the presence of dinosaur tracks in the Demnat region (Morocco)]". Comptes Rendus sommaires dela Société géologique de France. 7 (16): 241–242.
- ^ a b c d e Masrour, M.; Ladel, L.; Pérez-Lorente, F. (2015). "New theropod and prosauropod ichnites from Issil-n-Aït Arbi (Lower Jurassic, Central High Atlas, Morocco)" (PDF). Geogaceta. 57 (1): 55–58. Retrieved 1 April 2022.[dead link]
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