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Imprint of the Reguibat Promontory (West Africa) on the Appalachian, Mauritanide and Souttoufide Belts During the Assembly of Pangaea

A peer-reviewed version of this preprint was published in:
Geosciences 2025, 16(1), 14. https://doi.org/10.3390/geosciences16010014

Submitted:

21 February 2025

Posted:

24 February 2025

Read the latest preprint version here

Abstract

In the course of the Carboniferous to Permian assembly of Pangaea, large parts of eastern Laurussia and northern Gondwana were affected by the Variscan Orogeny. Here, we particularly focus on the Appalachian belt of eastern Laurentia and the Mauritanide, Western Thrust (WTB) and Souttoufide belts of the western West African Craton. Owing to the irregular shapes of the craton margins, this collision resulted in several conjugate promontories and embayments on both cratons. Among others, the coupled pair formed by the African “Reguibat promontory” and its counterpart in North America, the “Pennsylvania embayment” is in focus of this study. The (relative) western movement of the Reguibat Shield had initially imprinted the West African belts but finally also affected the Appalachians. Forming such a classical “punch mark” produces two specific stacks of “nappes” (lobes) on both sides of the promontory. Related to the Reguibat promontory, the southern NW-SW stacking nappes (e.g. Akjoujt nappes) are known since a long time. However, those nappes of the “Adrar Souttouf Massif” to the north have not been recognised before because of its N-S alignment instead of a symmetrical SW-NE direction. Furthermore, the Adrar Souttouf Massif is partially covered by allochthons terranes (WTB or Appalachians). This discovery justifies the application of the classical imprinting model to the deformation of the North American and African belts by westward moving of the Reguibat Shield.

Keywords: 
Impingement
;  
Gondwana plate margins
;  
Variscan Orogeny
;  
Reguibat Shield
;  
West African belts
;  
North American belts
Subject: 
Environmental and Earth Sciences  -   Geophysics and Geology

1. Introduction

The Variscan suture between Laurussia and Northern Gondwana was formed during the assembly of Pangea and has an irregular, winded course (Figure 1). This results in several promontories and embayments. The embayments on the Laurentian side correspond to promontories on the West African Craton (WAC) and vice-versa.
Here, the focus is on the impact of the West African Reguibat promontory and the corresponding Pennsylvania embayment in the Laurentia. These two regions are bordered by Senegalese-Mauritanian embayment and the corresponding Virginia promontory,to the south and to by the Moroccan-Iberian embayment that corresponds to the New York or Avalonian promontory to the north (Figure 2). The southern limit of the Reguibat Shield is marked by the Aouker Fault Zone to the south and by the Anti-Atlas Fault zone to the north. While only the southern parts of the Reguibat Shield are cropping out, its northern parts are concealed underneath the sedimentary rocks of the Tindouf Basin.The latter often resulted in underestimations of the Reguibat Shield in previous reconstructions dealing its imprinting.
The whole western part of the Reguibat Shield is tripartite: the convex part surrounded by the northern part of the MauritanideBelt (Akjoujt area) to the south, the western part with the Appalachians and the Souttoufide Belt to the north. The latter includes, from the south to the north: The Adrar Souttouf Massif, the Zemmour Massif including the adjacent Dhlou-Sekkem Belt and, finally, the “plage Blanche” Belt [2]. The Reguibat promontory only concerns the southwesternmost part of the Reguibat Shield and is limited to the south by the Mauritanide Belt and to the north by the Adrar Souttouf Massif. Thus, the northern and southern parts of this Reguibat Shield are not symmetric (Figure 2). This asymmetry induced a mis-interpretation of the Reguibat imprinting model resulting of a controversial interpretation of the Adrar Souttouf Massif. Our new interpretation reconciles the different hypotheses, which allow proposing a better “imprinting” model for both sides of the Palaeozoic Rheic Ocean.

2. Geological Framework

The collision of West Africa and North America at the end of Pangaea’s assembly resulted in the formation of Variscan Orogen is shown in Figure 2. The Variscan suture separating West Africa and North America has a mainly N-S trend and can be followed from Morocco to Senegal. Furthermore, the suture is linked to the E-W-directed Brunswick magnetic anomaly that is located between the Appalachians and the Suwannee Basin of Florida. Furthermore, the North American part includes large portions of cratonal basement and the Appalachians. The eastern part of the Variscan suture is more complex. It includes the WAC basement surrounded by three Variscan belts: the Adrar Souttouf and Dlhou belts, both representing parts of the Souttoufide Belt to the north and the Western Thrust Belt (WTB) ,the Mauritanide Belt that are separated by the Senegalese Block including the foreland basins to the south.The foreland basins of the Reguibat Shield and the mentioned orogenic belts comprise the poorly deformed Tindouf, Taoudeni and Bové basins in Africa and the Guinean Palaeozoic (GPB) and Suwannee basins in the subsurface of Florida. A geological cross section from the Appalachians to the Mauritanides indicated in Figure 2 and presented in Figure 3, shows a double vergence between the Appalachians and the WTB [3]. We notice a vergence to the east for the Mauritanide Belt that is separated from the WTB by the rigid Senegalese Block. Taking a magmatic arc into account that is located in the Appalachians, a westward slab vergence is supposed (Figure 3).
Thus, this study concerns the northern zone including the northern part of the Mauritanides, the southern part of the Souttoufides and their western counterparts in the Appalachians (see location of Figure 12 in Figure 2). This area represents a western promontory of the Reguibat Shield.

3. The Reguibat Promontory Model.

A model of the Reguibat imprinting has been proposed by Lefort [4,5], which is presented in Figure 4. This model only considers the southwestern part of the Reguibat Shield as promontory. According to Figure 4, the westward motion of the southern part of the Reguibat Shield is squeezing the Appalachian and Mauritanide belts, giving way to the “nappes” that now stacked on both sides of the promontory (areas in green in Figure 4). These areas are furthermore characterised by dextral strike-slip motions along the northern fault and sinistral strike-slip motions along the southern fault that can also be found in the Appalachians.
Although the southern part of the Reguibat promontory can be observed in the field, its northern continuation is concealed under thick sedimentary sequences. The aim of this paper is to compare the model with field observations.

4. Field Observations

Field observations have been undertaken in the central Appalachians, in the Akjoujt area of the northern Mauritanides and in the southern Souttoufides (Adrar Souttouf Massif) in order to find the structural elements developed in the hitherto proposed model.

4.1. The Appalachians

The Reguibat promontory caused the separation of the southern from the northern Appalachians by the Pensylvania embayment (Figure 5).
According to Hibbart et al. [6], the Appalachians can be divided in three parallel zones (Figure 5): the Laurentian terranes to the West, the Iapetian terranes in the middle and the peri-Gondwanan terranes to the East. In the southern Appalachians, there are several strike-slip faults parallel to the three zones, such as the Brevard Fault Zone, Bowens Creek Fault, Towaliga Fault, Goat Rock Fault, Modoc Fault Zone, Hylas Fault Zone, Gold Hill Fault and Goat Rock Fault. The strike-slip movements along these faults are dextral [7,8,9]. In the Northern Appalachians, the geological structures are more complex, noticeably with three peri-Gondwanan terranes of Ganderia, W-Avalonia and Meguma. However, several authors [10,11,12,13] agreed with a dextral strike-slip motion along the major faults: Norumbega-Fredericton Fault, Bellisle Fault, Cabot Fault, Dog Bay Fault, Chedabucto and St.MaryFaults, Cobequid Fault, etc.

4.2. The Northern Mauritanides (see Figure 6 indicated in Figure 2).

This part of the Mauritanide Belt is located between the Aouker Trough (AFZ in Figure 2) and the Reguibat Shield. It has been well studied in the course of the prospecting activities for the copper mines around Akjoujt City. The main tectonic event in the Akjoujt series was finally ascribed to the Variscan Orogen by Teissier et al [14] and Sougy [15] as well as Lecorché [16] and Bradley et al. [17). Detailed mapping of this series is provided by from Martyn and Strickland [18] as well as Pittfield et al. [19]. The geological map in Figure 6 presents a Reguibat basement (Archaean and Palaeoproterozoic) covered by Neoproterozoic and Palaeozoic sedimentary rocks. These basal formations are capped by the Reg Unit, which contains various rocks resembling those of the Cambro-Ordovician foreland cover. This Reg Unit is dismembered and thrusted over the foreland units. The mainly allochthonous Akjoujt terrane is stratigraphically above them and includes a mix of sheets composed of various rocks such as quartzite, siltstone, migmatite and porphyritic granite. The Akjoujt Unit is considered as a very thin nappe stack (Figure 7) that was emplaced from the NW to the SE [20} and partially covered by the Agualilet Unit, which crops out in the south-western part of this area and which consists of siliciclastic and volcanic rocks such as basalt, gabbro, prasinite and silicitic tuff thrusted over the previously mentioned units during a Carboniferous tectonic event.

4.3. Souttoufide Belt

The SouttoufideBelt [2]) includes three separate parts: The Adrar Souttouf Massif, the Dhlou/Zemmour Massif and the “PlageBlanche” Belt.

4.3.1. Adrar Souttouf Massif (Figure 8 indicated in Figure 2)

This large and controversial area has been studied by many geologists since 1949. Initial studies were conductedby the Spanish geological Survey [22,23,25,26], who considered this massif as the western part of the Reguibat Shield with remnants of Palaeozoic covers. Then, Sougy [27] proposed the thrusting of this massif onto the Reguibat Shield and its thin Palaeozoic cover. Bronner, et al. [28] interpreted aerial photographs and considered this metamorphic massif as a pile of sheets with gabbro thrusted on top of the Reguibat basement and its Palaeozoic cover (Figure 8A,B). Le Goff et al. [29] discovered a Neoproterozoic basement with traces of Variscan metamorphic overprint. Villeneuve et al. [2,30] and Gärtner et al. [31,32] distinguished several units stacked from the West to the East during the Carboniferous Variscan tectonic event (Figure 9A,B) without evidence of “nappe synforms”. The eastern units are ascribed to the autochthonous Neoproterozoic belts reworked by the Variscan event. Meanwhile the western units are ascribed to exotic terranes likely related to the Appalachians and thrusted over the previous autochthonous terranes. Further geochronological ages by U-Pb on zircon and K/Ar on whole rock and several mineral phases, supported this interpretation [32,33,34,35,36]. Recently, Bea et al. [37] ascribed a part of the western units to the Reguibat Shield basement supporting the Bronner et al. [28] interpretation, which is in contrast to Villeneuve et al. [2].
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Figure 9. A: Geological scheme of the Adrar Souttouf Massif (modified after Gärtner et al. [31]) with location of cross-sections AB and CD in Figure 11. Figure 9B: Schematic cross-sections AB and CD in the Adrar Souttouf Massif (modified after Gärtner et al. [31]).
Figure 9. A: Geological scheme of the Adrar Souttouf Massif (modified after Gärtner et al. [31]) with location of cross-sections AB and CD in Figure 11. Figure 9B: Schematic cross-sections AB and CD in the Adrar Souttouf Massif (modified after Gärtner et al. [31]).
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Figure 10. a: Adrar Souttouf Massif photographed from space (NASA photo). Figure 10b: New Interpretation of the Adrar Souttouf Massif with the central gabbroic and metamorphic “nappe synforms”. The African units (UB, UC and UD) are covered by the allochthonous units (UE, UF and UG). These units are described in Villeneuve et al. [2].
Figure 10. a: Adrar Souttouf Massif photographed from space (NASA photo). Figure 10b: New Interpretation of the Adrar Souttouf Massif with the central gabbroic and metamorphic “nappe synforms”. The African units (UB, UC and UD) are covered by the allochthonous units (UE, UF and UG). These units are described in Villeneuve et al. [2].
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Figure 11. a: W-E Seismic profile across the Adrar Souttouf Massif (Fateh [39]). Figure 11b: Geological interpretation of the seismic profile in Adrar Souttouf Massif.Legend: Allochthonous or exotic terranes (Units E, F and G), African terranes (Units B, C and D), Palaeozoic cover (Unit UA).
Figure 11. a: W-E Seismic profile across the Adrar Souttouf Massif (Fateh [39]). Figure 11b: Geological interpretation of the seismic profile in Adrar Souttouf Massif.Legend: Allochthonous or exotic terranes (Units E, F and G), African terranes (Units B, C and D), Palaeozoic cover (Unit UA).
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At this stage of our knowledge, there are two opposite interpretations, but the study of the Landsat imagery (Figure 10a) shows that the two different interpretations are compatible since we are interpreting (Figure 10b) the black circular unit as the thrusted “synform”of Bronner et al. [28] partially covered by thin and peculiar units, which could be related to those mapped in the field by Rjimati and Zemmouri [38] and Villeneuve et al. [30]. Thus, the outcrop of parts of the Reguibat basement in the fore-western units [37] is consistent with an incorporation of a basement sheet into the exotic pilein the course of thethrusting to the east during the late Variscan tectonic event.
The seismic profile across the Adrar Souttouf Massif (Figure 11a) delivered by Fateh [39] suggests that the central gutter could be interpreted as the stack of African units (“stacked nappe units”) partially covered by exotic units (Figure 11b).
The section displayed in Figure 11 could explain why some parts of the Reguibat basement could be matched with allochthonous units like UE, UF or UG during the Variscan tectonic event, in the western part of the massif as it is hypothesised by Bea et al. [37].

4.3.2. ZemmourMassif and Dhlou-Sekkem Belt

The Zemmour area studied by Sougy [40] corresponds to the western part of the Tindouf Basin and consists of a sedimentary succession ranging from Ediacaran limestones to the Late Devonian. The Dhlou and Sekkem belts, located to the West, consist in parts of Tindouf Basin sediments folded, sheared and thrusted to the east over the western part of the Zemmour Massif. The Dhlou and Sekkem belts were studied by Dacheux [41], Rjimati and Zemmouri [38]) and Belfoul [42].The western part of these belts is concealed underneath the Palaeo- and Neogene sedimentary cover of thecoastal basin.

4.3.3. Plage Blanche Belt

Recent works (Belfoul [42] and Soulaimani and Burkhard [43]) extend the main Variscan Front Thrust (HFT) until “Plage Blanche”, which is located to the west of the Ifni Inlier. A W-E cross-section shows a succession of shales, quartzites and argilites deformed and oriented from N-S to NE-SW with dipping to the West. These sediments ascribed to the Ordovician exhibits many westward thrusts ascribed to the Variscan tectonic event. According to Villeneuve et al. [44] this part belongs to an N-S Cadomian/Variscan belt, cross-cutting the E-W pan-African Anti-Atlas belt in this area.

5. Structure of the Reguibat imprinting

5.1. Structure of the Mauritanian-Appalachian fold belts and the Reguibat imprinting

According to Figure 12, the main structural units are from the east to the west:
- The Reguibat Shield (in red) covered by the sedimentary Tindouf and Taoudeni foreland basins with Neoproterozoic and Palaeozoic formations (in yellow).
- The Variscan front thrust (in brown).
-An eastern Unit with remnants of Neoproterozoic and Early Palaeozoic belts (in blue).
- Two lobes of nappes on both sides of the Reguibat promontory: Adrar Souttouf lobe (ASL) and Akjoujt lobe (AKL) in green. AKL is partially covered by the early Palaeozoic Agualilet Belt (in light pink).
-The Senegalese Block (in pink).
-The exotic terranes (allochthons units), which are partially covering the northern lobe and are linked to the Western Thrust belt (WTB) to the West of the Senegalese Block (light orange).
-The Appalachian domain (dark orange).

5.2. Comparisons with the Previous Model.

Finally, the evidence of a “lobe of nappes” in the Adrar Souttouf Massif and the movement of terranes in the Appalachians as well as in the African belts, the Reguibat imprint (Figure 12) is similar to the previous model of Lefort [4,5]. The main difference between the model and the apparent imprint consists in the asymmetry in the orientation of the lobes which are oriented NW-SE in the northern Mauritanides (to the south of the Reguibat promontory) and SSW-NNE in the Adrar Souttouf Massif to the north of the Reguibat promontory. Meanwhile, they are symmetric in the model of Lefort. This discrepancy could be explained by the N-S oriented shape of western margin of the Reguibat Shield and the NNE-SSW orientation of the gutter in which the northern lobe (ASL) is infilled. The covering of the Adrar Souttouf lobe by the allochthonous units prevented to validate the similarities between the field observations and the theorical model. Thus, the previously geologic scheme of the Variscan assemblage between the Appalachians on the West African fold belts presented in Figure 2 (Villeneuve et al. [1]) should be modified (Figure 13) taking into account the partially capping of the West African structures by the late Variscan Orogeny.

6. Evolution of the Southern Variscan Belts During the Assembly of Pangea

According to Figure 14, three main stages can be distinguished in this assembly process: a pre-collisional stage, a collisional stage and a post-collisional stage.

5.2.1. The pre-Collisional Stage (Figure 14a).

The westward shifting of the Reguibat Shield forced a southward movement of the Senegalese Block, which consequently folded the northern part of the Bové Basin. The northward movement of the Adrar Souttouf terranes occurred coevally. In the Senegalese Block, the N-S-trending Wa-Wa trough which was infilled by post-Cambrian Palaeozoic sediments does not show any signs of strong deformation. Subsequently, the shift of the Reguibat Shield to the west induced the “lobes of nappes” on both sides of the Reguibat promontory. The northwards shift of the Adrarb Souttouf Massif is recorded by dextral strike-slip along the meridian faults in the field.

5.2.2. The Collisional Stage (Figure 14b).

In this collisional stage the Rheic Ocean was already closed. To the north the exotic terranes that are of WTB or Appalachian origin, are thrusted over the western parts of the Adrar Souttouf “lobe”. Meanwhile to the south, the Appalachian belts and the WTB were reunited. At this stage the main strike-slip faults in the Appalachians may have been active.

5.2.3. The Post-Collisional Stage (Figure 14c).

At this stage, the WTB is thrusted over the Senegalese Block which, itself, is thrusted onto the Taoudeni Basin. The Wa-Wa and the Agualilet Units were folded and the AgualiletUnit already covered the southern part of the Akjoujt “lobe”. The southern Bissau-Kidira Fault Zone (BKKF in Figure 2) is extended from the Brunswick Fault to the Kayes fault. Characteristics of dextral strike-slip are preserved in this fault zone.
The whole collisional processes, which have a temporal extension of more than 100 Ma is likely simplified at the current stage of knowledge and deserves to be enhanced by new geochronological and tectonic data.

6. Conclusion

After several decades of research and controversial debates, we are proposing a new hypothesis reconciliating most of the previous models. The thrusting of exotic terranes over the northern “lobe”of the Reguibat promontory hampers the recognition and correlation of features similar to the hitherto applied hypothetical model of imprinting. New data from the parts of the Adrar Souttouf lobe which are covering the Reguibat Shield allow us to reconstruct the promontory imprint. Our hypothesis is consistent with the currently available data. The collisional process between Laurentia and the West African Craton has lasted more than100 Ma. Due to complex geometries of the cratonic margins with marginal blocks like the Senegalese Block and owing to the covering of the WTB by the Palaeo- to Neogene sedimentary successions of the Senegalo-Mauritanian basin, a complete reconstruction of the proposed processes is quite complicated. The main driver of these process was the westward movement of the Reguibat Shield, which imprinted the belts setting on both sides of the cratons.

Author Contributions

MV: conceptualization, writing, supervision, OG: figure drawing, methodology, original draft preparation, AG: formal analysis, investigation, supervision, AE: validation, investigations, AM: data curation, HB: formal analysis, P.A.M: original draft preparation, PMN: visualization, NY: validation, UL: validation, review and editing, MC: supervision. All authors have read and agreed to the published version of the manuscript.

Funding

there was no funding.

Acknowledgments

We acknowledge the different geological surveys, which support our field investigations such as: the French BRGM, the Moroccan Geological Survey, the Mauritanian Geological Survey and the Senegalese Geological Survey. We also acknowledge the laboratories which provide a lot of consistent geochronological data as: the Senckenberg Natural History Collections Dresden (Germany), the Florida University (USA), the Brest University (France). The reviewers are thanked for their recommendations.

Conflicts of Interest

The authors declare no conflicts of interest.

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  33. Gärtner A, Villeneuve M, Linnemann U, El Archi A, Bellon H. An exotic terrane of Laurussian affinity in the Mauritanides and Souttoufides (Moroccan Sahara). Gondwana Res., 2013, 24:687–699. [CrossRef]
  34. Gärtner A. Geologic evolution of the Adrarb Souttouf Massif (Moroccan Sahara) and its significance for continental-scaled plate reconstructions since the Mid Neoproterozoic. Unpublished doctoral thesis, Technische Universität Dresden, Dresden (Germany),2017, 310p.
  35. Gärtner A, Youbi N, Villeneuve M, Sagawe A, Hofmann M, Mahmoudi A, Boumehdi MA, Linnemann U. The zircon evidence of temporally changing sediment transport – the NW Gondwana margin during Cambrian to Devonian time (Aoucert and Smara areas, Moroccan Sahara). Int. J. Earth Sci., 2017, 106:2747–2769. [CrossRef]
  36. Gärtner A, Youbi N, Villeneuve M, Linnemann U, Sagawe A, Hofmann M, Zieger J, Mahmoudi A, Boumehdi MA. Palaeogeographic implications from the sediments of the Sebkha Gezmayet unit of the Adrar Souttouf Massif (Moroccan Sahara). CR Geoscience, 2018, 350 (6):255–266.
  37. Bea F, Montero B, Haissen F, Molina JF, Lodeiro FG, Mouttaqui A, Kuiper YD, Chaib M. The Archean to Late-Paleozoic architecture of Oulad Dlim Massif, the main Gondwanan indenter during the collision with Laurentia. Earth Sci. Rev. 208:150–182. [CrossRef]
  38. Rjimati E, Zemmouri A (2002)- Carte géologique du Maroc au 1/100 000. Feuille de Smara, Notice explicative. Notes et mémoires du service géologique du Maroc, 2020, 438bis, 52p.
  39. Fateh B. Modélisation de la propagation des ondes sismiques dans les milieu visco-elastiques: Application a la détermination de l’atténuation des milieu sédimentaires. Thèse Université de Bretagne Occidentale, Brest, 2008, 181p.
  40. Sougy J. Les formations paléozoïques du Zemmour noir (Mauritanie septentrionale): etude stratigraphique, pétrographique et paléontologique. Ann. Fac Sci. Univ. Dakar, 1964, 12:1–695.
  41. Dacheux A, Etude photogéologique de la chaine du Dhlou (Zemmour-Mauritanie septentrionale). Laboratoire de Géologie, Université de Dakar, 1967, rapport 22:1–45.
  42. Belfoul M.A. Cinématique de la deformation hercynienne et geodynamique Paleozoique dans l’Anti-Atlas sud occidental et le Sahara Marocain. Thèse doctorat état, Université Ibn Zor, Agadir, Maroc, 2005, 379p.
  43. Soulaimani A, Burkhard M. The Anti-Atlas chain (Morocco): the southern margin of the Variscan belt along the edge of the West African craton.In: EnnihN, Liégeois JP (eds): The Boundaries of the West African Craton Geol.Soc. London, 2008, SP 297:433–452. [CrossRef]
  44. Villeneuve M, Vernhet E, El Archi A. Neoproterozoic belts in the Moroccan Anti-Atlas area. 29th IAS meeting, 10th-13thSeptember 2012, Schladming, Austria, 2012, Abstracts: 149.
  45. Villeneuve M, Gärtner A, Mueller PA, Guillou O, Linnemann U. Colliding cratons: linking the Variscan orogeny in West Africa and North America. Geol.Soc. London, 2024, SP 542-359–377. [CrossRef]
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Figure 1. Position of blocks during the Late Carboniferous to Early Permian times (ca. 300-270Ma) with the Variscan suture line in red. Legend: WAC-West African Craton, AMC-Amazons Craton, SAL- Alleghanian or Variscan Suture, Apl-Appalachian Belt,Ge-Guerrero Block,WS- Western Sahara, Ib-Iberia, CVe – European Variscan Belt, GB-Great Britain, GRL-Greenland, Mx-Mixteco Block, BAL -Baltica, Y- Yucatan, Ox-Oaxaquia, CH-Chortis, Cb-Cuba, NWAb-Northwestern Amazonian blocks, SP-South pole.
Figure 1. Position of blocks during the Late Carboniferous to Early Permian times (ca. 300-270Ma) with the Variscan suture line in red. Legend: WAC-West African Craton, AMC-Amazons Craton, SAL- Alleghanian or Variscan Suture, Apl-Appalachian Belt,Ge-Guerrero Block,WS- Western Sahara, Ib-Iberia, CVe – European Variscan Belt, GB-Great Britain, GRL-Greenland, Mx-Mixteco Block, BAL -Baltica, Y- Yucatan, Ox-Oaxaquia, CH-Chortis, Cb-Cuba, NWAb-Northwestern Amazonian blocks, SP-South pole.
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Figure 2. Geological sketch map of the Variscan belts in West Africa and North America [modified after [1.] with indication of local geological schemes of this study. Legend: AA-Anti-Atlas Belt, AS-Adrar Souttouf Massif, SB-Senegalese Block, MM-Moroccan Meseta, 360-Ages of deformation in Ma.
Figure 2. Geological sketch map of the Variscan belts in West Africa and North America [modified after [1.] with indication of local geological schemes of this study. Legend: AA-Anti-Atlas Belt, AS-Adrar Souttouf Massif, SB-Senegalese Block, MM-Moroccan Meseta, 360-Ages of deformation in Ma.
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Figure 3. Schematic cross-section along line A-B in Figure 1. Legend: as in Figure 1. Slab in blue, DKR-Dakar, Dl1-Diourbel well, LiF2-Linguere well, WTB- Western Thrust Belt, SB- Senegalese Block, MB-Mauritanide Belt, MFT- Mauritanide Front thrust, PS- Precambrian suture. External formations correspond to a melange with pre-Variscan and Variscan formations.
Figure 3. Schematic cross-section along line A-B in Figure 1. Legend: as in Figure 1. Slab in blue, DKR-Dakar, Dl1-Diourbel well, LiF2-Linguere well, WTB- Western Thrust Belt, SB- Senegalese Block, MB-Mauritanide Belt, MFT- Mauritanide Front thrust, PS- Precambrian suture. External formations correspond to a melange with pre-Variscan and Variscan formations.
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Figure 4. Block diagram that illustrates the tectonic model for the imprint of the Reguibat uplift onto the Southern and Central Appalachians (modified after [4]).
Figure 4. Block diagram that illustrates the tectonic model for the imprint of the Reguibat uplift onto the Southern and Central Appalachians (modified after [4]).
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Figure 5. Generalised map showing tectono-stratigraphic zones of the Appalachian Orogen (modified after [6]). Legend: TF- Towaliga Fault, RF-Goat Rock Fault, MOF- Modoc Fault Zone, AFZ- Hylas Fault Zone, CM- Cobequid Fault, MFZ-Minas Fault Zone, NF-Bellisle Fault, CM-Chedabucto and St. Mary Fault, CF- Cabot Fault (Aspy Fault), GF-Percé Fault, CVGT-Connecticut Valley Gaspé Trough.
Figure 5. Generalised map showing tectono-stratigraphic zones of the Appalachian Orogen (modified after [6]). Legend: TF- Towaliga Fault, RF-Goat Rock Fault, MOF- Modoc Fault Zone, AFZ- Hylas Fault Zone, CM- Cobequid Fault, MFZ-Minas Fault Zone, NF-Bellisle Fault, CM-Chedabucto and St. Mary Fault, CF- Cabot Fault (Aspy Fault), GF-Percé Fault, CVGT-Connecticut Valley Gaspé Trough.
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Figure 6. Geological sketch map of the northern Mauritanide area (indicated in Figure 2).
Figure 6. Geological sketch map of the northern Mauritanide area (indicated in Figure 2).
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Figure 7. Cross section illustrating the structure from Akjoujt to the Taoudeni foreland (modified after Lecorché et al.[21]).
Figure 7. Cross section illustrating the structure from Akjoujt to the Taoudeni foreland (modified after Lecorché et al.[21]).
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Figure 8. A: Sketch map of the Adrar Souttouf Massif after Bronner et al. [28].Figure 8B: Geological section across the Adrar Souttouf Massif interpreted as a synform of “nappes” by Lecorché et al. [21].
Figure 8. A: Sketch map of the Adrar Souttouf Massif after Bronner et al. [28].Figure 8B: Geological section across the Adrar Souttouf Massif interpreted as a synform of “nappes” by Lecorché et al. [21].
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Figure 12. New interpretation of the Reguibat Shield imprint within the Mauritanide and: Appalachian systems during the Variscan Orogeny and comparison with the imprinting model of the craton (see model in Figure 4).
Figure 12. New interpretation of the Reguibat Shield imprint within the Mauritanide and: Appalachian systems during the Variscan Orogeny and comparison with the imprinting model of the craton (see model in Figure 4).
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Figure 13. New schematic geological structures of the Variscan Orogen between Laurentia and WAC, in the part of Variscan system limited to the north by the Anti-Atlas Fault Zone andto the south by the Bissau-Kidira Fault Zone.
Figure 13. New schematic geological structures of the Variscan Orogen between Laurentia and WAC, in the part of Variscan system limited to the north by the Anti-Atlas Fault Zone andto the south by the Bissau-Kidira Fault Zone.
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Figure 14. Three figures to illustrate the three different stages of the collision between the Laurentia and the West African Craton during the last period of the Variscan Orogeny (modified after Villeneuve et al. [45]). Legend: SB- Suwannee Basin, GPB-Guinean Palaeozoic Basin, BB-Bové Basin, SB-Senegalese Block, RO- Rheic Ocean.
Figure 14. Three figures to illustrate the three different stages of the collision between the Laurentia and the West African Craton during the last period of the Variscan Orogeny (modified after Villeneuve et al. [45]). Legend: SB- Suwannee Basin, GPB-Guinean Palaeozoic Basin, BB-Bové Basin, SB-Senegalese Block, RO- Rheic Ocean.
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