Rémi Leprêtre
email: remi.lepretre@upmc.fr

Jocelyn Barbarand

Yves Missenard

Cécile Gautheron

Rosella Pinna-Jamme

Omar Saddiqi

Mesozoic evolution of NW Africa: implications for the Central Atlantic Ocean dynamics

Keywords:

ou non, émanant des établissements d'enseignement et de recherche français ou étrangers, des laboratoires publics ou privés.

Introduction

In the past two decades, substantial evidence has been presented to show that passive margins are anything but passive. For example, the Atlantic-type margins have been thoroughly studied and show repeated uplift or burial events in the course of their post-rift history [START_REF] Gallagher | Fission track analysis and its applications to geological problems[END_REF][START_REF] Turner | Thermal history of the Rio Muni)-NE Brazil margins during continental breakup[END_REF][START_REF] Holford | Regional intraplate exhumation episodes related to plate-boundary deformation[END_REF][START_REF] Japsen | Elevated, passive continental margins: long-term highs or Neogene uplifts? New evidence from West Greenland[END_REF][START_REF] Japsen | Elevated, passive continental margins: Not rift shoulders, but expressions of episodic, post-rift burial and exhumation[END_REF][START_REF] Cogné | Post-breakup tectonics in southeast Brazil from thermochronological data and combined inverse-forward thermal history modeling[END_REF][START_REF] Green | Stratigraphic landscape analysis, thermochronology and the episodic development of elevated, passive continental margins[END_REF][START_REF] Leprêtre | Postrift history of the eastern central Atlantic passive margin: Insights from the Saharan region of South Morocco[END_REF][START_REF] Wildman | Post breakup tectonic inversion across the southwestern cape of South Africa: New insights from apatite and zircon fission track thermochronometry[END_REF]. These studies have demonstrated that the precise determination of the timing of burial/uplift phase of the onshore margins can offer a better understanding of the stratigraphical record along the margins [START_REF] Japsen | Elevated, passive continental margins: Not rift shoulders, but expressions of episodic, post-rift burial and exhumation[END_REF]. Despite the evidence that passive margins are active features in plate tectonics, these studies also highlight the poor knowledge we have on the underlying mechanisms controlling these processes [START_REF] Japsen | Elevated, passive continental margins: Not rift shoulders, but expressions of episodic, post-rift burial and exhumation[END_REF]Green et al., 2013 and references therein).

In order to better understand the underlying mechanisms controlling rift and post-rift evolution, it is necessary to assess the simultaneous uplift/burial events on conjugate passive margins (e.g. [START_REF] Turner | Thermal history of the Rio Muni)-NE Brazil margins during continental breakup[END_REF][START_REF] Green | Synchronous exhumation events around the Arctic including examples from Barents Sea and Alaska North Slope[END_REF]. In this study, we compare the stratigraphical record of the conjugate margins of the Central Atlantic Ocean during the Mesozoic and the vertical evolution of the onshore domains. These margins have received considerable attention in the past (eastern North America: Sheridan & Grow, 1988;[START_REF] Miall | The Atlantic Margin Basins of North America[END_REF]Northwest Africa: von Rad et al., 1982;[START_REF] Poag | Depositional sequences and stratigraphic gaps on submerged United States Atlantic margin[END_REF], although there have been a limited number of comparison studies focusing on their respective stratigraphical records [START_REF] Jansa | Mesozoic-Cenozoic Development of the Eastern North American and Northwest African continental margins: a comparison[END_REF][START_REF] Von Rad | Early Cretaceous "events" in the evolution of the eastern and western North Atlantic continental margins[END_REF] and no study has ever compared the two margins considering their onshore evolutions. Many lowtemperature thermochronology studies have been undertaken along the onshore eastern North American passive margin [START_REF] Crowley | Thermal History of Michigan Basin and Southern Canadian Shield from apatite fission track analysis[END_REF][START_REF] Wang | Thermal History of the Michigan Basin from Apatite Fission-Track Analysis and Vitrinite Reflectance[END_REF][START_REF] Boettcher | Mesozoic-Cenozoic unroofing of the Southern Appalachian Basin: Apatite fission track evidence from Middle Pennsylvanian sandstones[END_REF][START_REF] Roden-Tice | Evidence for Differential Unroofing in the Adirondack Mountains, New York State, determined by apatite fission-track thermochronology[END_REF][START_REF] Roden-Tice | Early Cretaceous Normal Faulting in Southern New England: Evidence from Apatite and Zircon Fission-Track Ages[END_REF][START_REF] Grist | Post-Paleocene cooling in the southern Canadian Atlantic region: evidence from apatite fission track models[END_REF][START_REF] Lorencak | Combined apatite fission track and (U-Th)/He thermochronometry in a slowly cooled terrane: results from a 3440-m-deep drill hole in the southern Canadian Shield[END_REF][START_REF] Spotila | Origin of the Blue Ridge escarpment along the passive margin of Eastern North America[END_REF][START_REF] Roden-Tice | Regional-Scale Mid-Jurassic to Late Cretaceous Unroofing from the Adirondack Mountains through Central New England Based on Apatite Fission-Track and (U-Th)/He Thermochronology[END_REF][START_REF] Taylor | Low-temperature thermal history and landscape development of the eastern Adirondack Mountains, New York: Constraints from apatite fission-track thermochronology and apatite (U-Th)/He dating[END_REF][START_REF] Roden-Tice | Apatite fission-track evidence for the Cretaceous development of kilometer-scale relief and steady-state Tertiary topography in New England[END_REF]. However, along the Northwest African passive margin, a similarly large coverage of onshore data is still lacking (first data in [START_REF] Leprêtre | Vertical movements along the northern border of the West African Craton : the Reguibat Shield and adjacent basins[END_REF]2015) to achieve a detailed comparison of both margins and addressing this issue is a major goal of this study.

This study reports low-temperature thermochronology (LTT) data across the whole range of the northern West African Craton, which is the main continental domain of the eastern Central Atlantic Ocean (Fig. 1a). We used apatite fission-track and (U-Th-Sm)/He (AFT and AHe, respectively)

LTT and thermal modeling techniques [START_REF] Gallagher | Transdimensional inverse thermal history modeling for quantitative thermochronology[END_REF] to constrain the timing and amplitude of erosion/burial events for Mesozoic-Cenozoic times. Given a 40-120°C thermal sensitivity, these methods provide insights into the evolution of the uppermost 3-4 km of the crust [START_REF] Gallagher | Fission track analysis and its applications to geological problems[END_REF][START_REF] Flowers | Apatite (U-Th)/He thermochronology using a radiation damage accumulation and annealing model[END_REF][START_REF] Gautheron | Effect of alpha-damage annealing on apatite (U-Th)/He thermochronology[END_REF][START_REF] Djimbi | Impact of apatite chemical composition on (U-Th)/He thermochronometry: An atomistic point of view[END_REF]. We then combine our new LTT study with the wealth of LTT data on the eastern American passive margin and the sedimentary records of both conjugate passive margins. These data form the basis of our comparison between the two margins and discussion of the Mesozoic evolution of the Central Atlantic Ocean.

Geological setting

Within the northern West African Craton (NWAC), the Reguibat Shield is a flat basement domain, divided into a western Archean domain (> 2.5 Ga; [START_REF] Potrel | Archean crustal evolution of the West African Craton: example of the Amsaga Area (Reguibat Rise). U-Pb and Sm-Nd evidence for crustal growth and recycling[END_REF][START_REF] Schofield | U-Pb dating and Sm-Nd isotopic analysis of granitic rocks from the Tiris Complex: New constaints on key events in the evolution of the Reguibat Shield, Mauritania[END_REF] and an eastern Eburnean domain (2-2.2 Ga;Lahondère et al., 2001;[START_REF] Peucat | The Eglab massif in the West African Craton (Algeria), an original segment of the Eburnean orogenic belt: petrology, geochemistry and geochronology[END_REF]. Its westernmost tip is part of the Variscan Mauritanides [START_REF] Villeneuve | Review of the orogenic belts on the western side of the West African craton: the Bassarides, Rokelides and Mauritanides[END_REF][START_REF] Michard | The South-Western Branch of the Variscan Belt: Evidence from Morocco[END_REF]. North and south of the Reguibat Shield, the Tindouf and Taoudeni basins display a km-scale Paleozoic infill [START_REF] Boote | Paleozoic petroleum systems of North Africa[END_REF], unconformably lying on the Neoproterozoic rocks (Fig. 1b). Both basins have large-scale synclinal shapes with low (5-10°) dipping flanks, with the exception of the steeper northern flank of the Tindouf Basin, which was involved in the Variscan deformation [START_REF] Burkhard | Tectonics of the Anti-Atlas of Morocco[END_REF]. Most authors acknowledge the existence of a continuous sedimentary realm until the Early Carboniferous [START_REF] Bertrand-Sarfati | Cover sequences of the West African Craton[END_REF][START_REF] Legrand-Blain | Brachiopodes et Conodontes carbonifères du bassin de Taoudeni (Mali, Afrique de l'Ouest) : biostratigraphie et paléogéographie[END_REF]. On top of Paleozoic formations, unconformable horizontal Mesozoic-Cenozoic formations are observed. The oldest Mesozoic deposits are Early Cretaceous rocks in the Tindouf Basin [START_REF] Gevin | Etudes et reconnaissances géologiques sur l'axe cristallin Yetti-Eglab et ses bordures sédimentaires (1ere partie: bordures sédimentaires)[END_REF][START_REF] Fabre | Géologie du Sahara occidental et central[END_REF].

In the eastern Taoudeni Basin (Tanezzrouft), the oldest Mesozoic deposits are possibly Late Cretaceous [START_REF] Fabre | Géodynamique du craton ouest africain central et oriental : héritage et évolution post-panafricains. Service géologique de l'Algérie, Boumerdès[END_REF] (Fig. 1). This hiatus of more than 100 Myr (from Late Carboniferous/Permian to at least Early Cretaceous) differentiates the WAC from the central and eastern Sahara domains where post-Variscan deposits can be as old as Triassic in central Sahara [START_REF] Busson | Principes, méthodes et résultats d'une étude stratigraphique du mésozoïque saharien[END_REF][START_REF] Boudjema | Evolution structurale du bassin pétrolier "triasique" du Sahara nord oriental (Algerie)[END_REF].

The Tarfaya-Laayoune-Dakhla Basin (TLDB; Fig. 1b) is a NE-SW oriented basin which bounds the Atlantic Ocean. This basin formed during the opening of the Central Atlantic Ocean, with an estimated break-up in the Late Sinemurian (~190 Ma; [START_REF] Labails | An alternative early opening scenario for the Central Atlantic Ocean[END_REF]. The basin is built on a 100km wide stretched crustal domain with a crust thickness that varies from 27 to 7 km oceanward [START_REF] Klingelhoefer | Deep crustal structure of the SWMorrocan margin from wideangle and reflection seismic data (The DAKHLA experiment)[END_REF]. The thick Mesozoic-Cenozoic infill reaches more than 10 km [START_REF] Auxini | Correlación estratigrafica de los sondeos perforados en el Sahara Español[END_REF][START_REF] Martinis | Données géologiques sur le bassin sédimentaire côtier de Tarfaya[END_REF][START_REF] Ratschiller | Lithostratigraphy of the Northern Sahara[END_REF][START_REF] Ranke | Stratigraphy, facies and tectonic development of the on-and off-shore Aaiun-Tarfaya basin-A review[END_REF]Fig. 1c) and represents a reliable record of the large-scale changes, which occurred during that time. On top of Triassic clasticevaporitic deposits, the Middle-Late Jurassic witnesses the build-up of a large carbonate platform that ended in the Neocomian (up to the Barremian). The margin was then buried under unconformable km-scale continental clastic deposits before marine conditions resumed in Aptian-Albian and continued during the Late Cenomanian-Turonian times. The early Paleogene environment was still marine but characterized by shallower depths before becoming continental from the Eocene onwards. Paleogene formations lie unconformably on the Early and Late Cretaceous in TLDB.

Neogene deposits are scarce, thin and usually continental.

Sampling and methodology

Sampling

The dataset presented here consists of 29 samples and allows us to present a ~1300 km E-W LTT transect of the NWAC from the Atlantic passive margin to the Panafrican suture in the east. Our new data adds two AFT data to the 11 existing AFT data in the western Reguibat Shield [START_REF] Leprêtre | Postrift history of the eastern central Atlantic passive margin: Insights from the Saharan region of South Morocco[END_REF], four new AFT and three new AHe datasets to the existing four AFT and one AHe datasets [START_REF] Leprêtre | Vertical movements along the northern border of the West African Craton : the Reguibat Shield and adjacent basins[END_REF] and eight new AFT and 6 new AHe datasets for the eastern Reguibat Shield (Fig. 1b). For the reader's information, the complete dataset encompassing samples from [START_REF] Leprêtre | Vertical movements along the northern border of the West African Craton : the Reguibat Shield and adjacent basins[END_REF][START_REF] Leprêtre | Postrift history of the eastern central Atlantic passive margin: Insights from the Saharan region of South Morocco[END_REF] are presented in Supplementary data (Tables S1,S2).

The Reguibat Shield was geographically divided into three regions on the basis of the LTT results. With the exception of one AFT age (256 Ma from TEN1153 sample, in central Reguibat Shield), AFT age ranges largely overlap between western and central domains (Fig. 2). Mean track lengths (MTLs) are also comparable between these two domains whereas MTLs from the eastern domain are shorter (Fig. 3). 1; Fig. 2,3) and shows a larger scattering of the AHe data (32 to 384 Ma).

Low-temperature thermochronology

Samples were processed at the GEOPS laboratory (Université Paris-Sud, Orsay, France). AFT dating was carried out using the external detector method [START_REF] Gleadow | A natural long-term track annealing experiment for apatite[END_REF] for calculating the central age [START_REF] Galbraith | Statistical models for mixed fission track ages[END_REF] using the Zeta calibration [START_REF] Hurford | The zeta age calibration of fission-track dating[END_REF]. Zeta calibration was done with a CN5 glass dosimeter and Durango/Fish Canyon apatite standards [START_REF] Hurford | Standardization of fission track dating calibration: recommendation by the Fission Track Working Group of the I[END_REF]ζ = 368 ± 10 for RL). Neutron irradiation was carried out at Garching facility (Germany). Spontaneous tracks were revealed by etching in 5M HN0 3 for 20 seconds at 20±1°C. The size of the etch pit made between the track and polished apatite surface (Dpar) was measured and used as a kinetic parameter for fission track annealing [START_REF] Carlson | Variability of apatite fission-track annealing kinetics: I. Experimental results[END_REF]. Dpar measurements act as a proxy for compositional and structural variations in apatite [START_REF] Barbarand | Compositional and structural control of fissiontrack annealing in apatite[END_REF]. Horizontal confined track-lengths were measured using a LEICA microscope with a x1000 magnification and a digitizing tablet linked via a drawing tube to the microscope. AFT ages, lengths and Dpar measurements are given in Table 1 andfigures 2-4. AHe analysis was carried out on euhedral inclusion-free apatite crystals with a minimum of four replicates per sample. Crystal dimensions and geometry were measured along the three axes and grains were placed into a platinum basket. Ejection factors and sphere equivalent radius were determined using the Monte Carlo simulation from [START_REF] Ketcham | Accounting for long alpha-particle stopping distances in (U-Th-Sm)/He geochronology: refinement of the baseline case[END_REF]. More details on He, U, Th and Sm content determination can been found in [START_REF] Gautheron | Chemical influence on α-recoil damage annealing in apatite: Implications for (U-Th)/He dating[END_REF]. The analysis was calibrated using internal and external age standards (Durango: McDowell et al., 2005;Limberg Tuff: Kraml et al., 2006). The error on the AHe age at 1σ is estimated to be a maximum of 8% reflecting uncertainty in the ejection factor (FT) correction and standard dispersion. The final He, U-Th-Sm content and AHe age are reported in Table 2.

AHe closure temperature was defined after [START_REF] Dodson | Closure temperature in cooling geochronological and petrological systems[END_REF] depending on apatite grain size, the cooling rate and on He diffusion coefficient. It has been shown that a pure apatite crystal "freedefault crystals" yield closure temperature of c.a. 30-40°C depending on chemical content [START_REF] Djimbi | Impact of apatite chemical composition on (U-Th)/He thermochronometry: An atomistic point of view[END_REF]. For natural apatite, the closure temperature is tightly linked to the alpha-recoil damage fraction [START_REF] Shuster | The influence of natural radiation damage on helium diffusion kinetics in apatite[END_REF]Shuster & Farley, 2009). This behavior has been incorporated into two predictive models by [START_REF] Flowers | Apatite (U-Th)/He thermochronology using a radiation damage accumulation and annealing model[END_REF] and [START_REF] Gautheron | Effect of alpha-damage annealing on apatite (U-Th)/He thermochronology[END_REF]. These models consider that recoil damage annealing follows kinetics similar to fission-tracks, after the results of [START_REF] Ketcham | Improved modeling of fission-track annealing in apatite[END_REF]. Different closure temperatures can be monitored through the relationship of AHe age vs. efficient uranium (eU). The eU represents the amount of radioactive elements contributing to the 4 He production and its amount controls the closure temperature for a given thermal history [START_REF] Shuster | The influence of natural radiation damage on helium diffusion kinetics in apatite[END_REF]. Thus, scattered AHe ages emphasize, at first order, differences in AHe closure temperatures between replicates in the same sample. Moreover, the damage-annealing rates can be influenced by the apatite chemistry [START_REF] Gautheron | Chemical influence on α-recoil damage annealing in apatite: Implications for (U-Th)/He dating[END_REF][START_REF] Djimbi | Impact of apatite chemical composition on (U-Th)/He thermochronometry: An atomistic point of view[END_REF]. In particular, [START_REF] Gautheron | Chemical influence on α-recoil damage annealing in apatite: Implications for (U-Th)/He dating[END_REF] demonstrated that complex thermal histories in slow moving geological settings can greatly enhance the scattering in the data given the chemistry differences between grains. Also, the 4 He apatite content can increase through implantation from rich eU neighbors crystals in the rock [START_REF] Spiegel | Apatite (U-Th-Sm)/He thermochronology of rapidly cooled samples: The effect of He implantation[END_REF][START_REF] Gautheron | Accounting for long alpha-particle stopping distances in (U-Th-Sm)/He geochronology: 3D modeling of diffusion, zoning, implantation, and abrasion[END_REF] or for low eU apatite, this effect has also been observed (Kendra et al., 2013;[START_REF] Murray | Effects of U-Th-rich grain boundary phases on apatite helium ages[END_REF][START_REF] Janowski | Neogene exhumation and relief evolution in the eastern Betics (SE Spain): insights from the Sierra de Gador[END_REF]. Helium implantation produces an artificial aging trend for the more exposed apatite crystals. In addition, the analysis of broken apatite crystals can add scattering to the data [START_REF] Brown | Natural age dispersion arising from the analysis of broken crystals. Part I: Theoretical basis and implications for the apatite (U-Th)/He thermochronometer[END_REF].

Thermal modeling

Modeling procedure

Inverse thermal modeling was performed using the software QTQt [START_REF] Gallagher | Transdimensional inverse thermal history modeling for quantitative thermochronology[END_REF] while HeFTy [START_REF] Ketcham | Forward and Inverse modeling of Low-temperature Thermochronometry data[END_REF] was used for forward modeling. We used the fission track annealing kinetics of [START_REF] Ketcham | Improved modeling of fission-track annealing in apatite[END_REF] and the He-trapping/diffusion model of [START_REF] Flowers | Apatite (U-Th)/He thermochronology using a radiation damage accumulation and annealing model[END_REF]. The [START_REF] Flowers | Apatite (U-Th)/He thermochronology using a radiation damage accumulation and annealing model[END_REF] radiation damage accumulation and annealing model is empirically calibrated and is not well-representative of the physical processes of diffusion compared to the [START_REF] Gautheron | Effect of alpha-damage annealing on apatite (U-Th)/He thermochronology[END_REF] model but it gives better predictions, mainly for low-eU apatite (< 20 ppm; majority of our samples, see Table 2). QTQt works with a probabilistic Bayesian approach for inverse modeling. It samples numerous thermal histories and from them builds a population of models selected according to the degree of agreement between data and model-this is the burn-in phase. It then proceeds with inverse modeling, which is called the post burn-in phase. For each phase, the user can choose the number of iterations, depending on the complexity of its own data set. In QTQt, the fit between the data and the model is defined by the Log Likelihood (LL; details are given in [START_REF] Gallagher | Transdimensional inverse thermal history modeling for quantitative thermochronology[END_REF].

Strategy for thermal modeling

The strategy for the thermal modeling of the LTT data relies on the geological context of the study. Importantly for this study, we consider, following [START_REF] Burov | Rheology and strength of the lithosphere[END_REF], that deformation of old lithospheres (> 1Ga) is mostly controlled by the rheology of the lithosphere which is dependent on its age. The Reguibat Shield is an old lithosphere (> 2 Ga; [START_REF] Potrel | Archean crustal evolution of the West African Craton: example of the Amsaga Area (Reguibat Rise). U-Pb and Sm-Nd evidence for crustal growth and recycling[END_REF]Lahondère et al., 2001;[START_REF] Peucat | The Eglab massif in the West African Craton (Algeria), an original segment of the Eburnean orogenic belt: petrology, geochemistry and geochronology[END_REF][START_REF] Schofield | U-Pb dating and Sm-Nd isotopic analysis of granitic rocks from the Tiris Complex: New constaints on key events in the evolution of the Reguibat Shield, Mauritania[END_REF][START_REF] Bea | 2.46 Ga kalsilite and nepheline syenites from the Awsard pluton, Reguibat Rise of the West African Craton, Morocco. Generation of extremely K-rich magmas at the Archean-Proterozoic transition[END_REF] and as such, its deformation will involve the whole lithosphere with wavelengths > 500 km. We thus infer that samples separated from each other by less than few hundred kilometers should behave coherently and share similar thermal paths. Furthermore, it implies that stratigraphical unconformities located on the boundaries of the Reguibat Shield can give precious information for the evolution of its basement since the latter is rarely wider than 400 km (Fig. 1).

For eastern Reguibat Shield, two major stratigraphical constraints were used: (1) unconformable Cambrian deposits on the NWAC basement [START_REF] Trompette | Le Précambrien et le Paléozoïque inférieur de l'Adrar de Mauritanie (bordure occidentale du bassin de Taoudeni, Afrique de l'Ouest). Un exemple de sédimentation de craton. Etude stratigraphique et sédimentologique[END_REF]Deynoux, 1980 for Taoudeni Basin;Boote et al., 1998 for Tindouf Basin); [START_REF] Turner | Thermal history of the Rio Muni)-NE Brazil margins during continental breakup[END_REF] unconformable poorly-dated upper Cretaceous deposits on the eastern boundary of the Reguibat basement. We used a large temperature box (20-180°C) for the 470-230 Ma interval as no constrain exists for this period. Firstly, a general thermal path was modeled with inverse modeling for eastern Reguibat shield samples that have both AFT and AH data (Fig. 6a-c, 7a; Fig. S2-7). By combining AFT and AHe datasets, we can achieve a better resolution of the thermal history path. The important temperature/time (or (T,t)) nodes obtained in this first modeling were used as constraints for other eastern Reguibat Shield samples where only AFT data were available (CH2 and DEG6, Fig. S2-3). Only final models are presented in the results (Fig. 6a,7a). Considering the old LTT ages of samples from eastern Reguibat Shield (> 237 ± 21 Ma), we only used the constraint that rocks were at surface during Cambrian. In the course of thermal modeling, no stable solutions were obtained for samples GH20 and IG3.

For central Reguibat Shield only one meaningful stratigraphical constraint was used: Lower Cretaceous deposits rest unconformably on the Paleozoic succession in the Tindouf Basin and directly on the basement in the east of the TLDB (Fig. 1b). This Lower Cretaceous unconformity is distant from the samples by less than 400 km. We suggest that it likely implies that even samples from the interior of the Reguibat Shield were at or close to the surface at this time. We used here a two-step approach for thermal modeling.

Firstly, we carried out a phase of forward modeling to explain the AHe age-eU positive correlation (Fig. 5b,8). In this phase, we consider the AHe data of all samples as these data should behave coherently given that they are restricted to cratonic areas and the entire AHe dataset samples a larger eU range than any one sample. Various thermal paths were tested to check their AHe predictions and compare them to the measured data. Given that the AFT ages are all younger than 250 Ma, the tested thermal history paths are chosen in order to display cooling initiated by the Early Jurassic. Using the initial forward modeling step, we have identified the scenarios that best explain the observed AHe data. These scenarios yield (T,t) constraints, i.e. compulsory nodes in the (T,t) space through which the thermal path must go to fit the AHe age-eU relationship. Secondly, we then performed inverse modeling that included these (T, t) constraints, so as to investigate the degree of freedom left to fit the AFT data. The same stratigraphic constraint was used for all samples.

All detailed individual models are presented figures S8-15 and only the final thermal paths are presented in figure 7b.

The two new samples from the western Reguibat Shield were modeled using the (T, t) constraints determined in [START_REF] Leprêtre | Postrift history of the eastern central Atlantic passive margin: Insights from the Saharan region of South Morocco[END_REF] (Fig. S16-17 and Text S1). One detailed thermal modeling is presented in figure 6c and all thermal paths for the western Reguibat Shield are shown in figure 7c.

Finally, considering the predictions made by the He-trapping/diffusion models [START_REF] Flowers | Apatite (U-Th)/He thermochronology using a radiation damage accumulation and annealing model[END_REF][START_REF] Gautheron | Effect of alpha-damage annealing on apatite (U-Th)/He thermochronology[END_REF], we advocate that for a given thermal history path, single-grain AHe ages are expected to display a correlation with eU. As a methodological consequence for our thermal modeling, we removed the single-grain AHe ages that were outliers from the mean AHe age-eU correlation, i.e. in our samples, being outliers by more than 50-100 Ma or a very different eU value (e.g. [START_REF] Flowers | Interpreting data dispersion and "inverted" dates in apatite (U-Th)/He and fission-track datasets: An example from the US Midcontinent[END_REF]. Using these "outlier" replicates would impede the thermal modeling as the model would attempt to fit out-of-trend data and lead to either no acceptable solutions being found (in the case of HeFTy) or to a thermal model with bad fit for many replicates (e.g. QTQt, Fig. S1). A clear assumption is made here that favors an acceptable goodness of fit for the majority of replicates, which belong to a common AHe age-eU trend, instead of trying to explain all the replicates resulting in a poor fit between predicted and observed data. Following this criteria, one single-grain AHe age of nine was removed in sample CH1 and TL3 for being too far from the mean AHe age-eU correlation (Fig. 5d, i; Table 2). Also, 3 of 11 replicates were removed in sample AL10 for the same reason (Fig. S1).

Results

The new and published AFT and AHe ages presented for 29 samples give the first comprehensive dataset across the whole Reguibat Shield. Based on the data location and their thermal histories, the studied area has been divided into western, central and eastern domains.

Published data from the western and central Reguibat Shield [START_REF] Leprêtre | Vertical movements along the northern border of the West African Craton : the Reguibat Shield and adjacent basins[END_REF]2015) are only briefly summarized, but the complete Reguibat dataset is presented together in Tables S1 andS2.

LTT results

The eastern domain shows the oldest and the most scattered AFT ages, ranging from 237 ± and 12 ± 0.2 µm (Fig. 3). Track length disributions (TLDs) are largely unimodal and spread around the mean (Fig. 4). Dpar measurements range from 1.7 ± 0.2 to 2.1 ± 0.2 µm. AHe ages corrected from alpha ejection range from 32 ± 3 to 384 ± 31 Ma with eU contents that range from 2 to 32 ppm. No clear trend in the AHe age vs. eU plot exists (Fig. 5a) and the very variable AHe ages for similar eU contents suggest that process other than a variable diffusion coefficient. This process will be discussed later.

In the central Reguibat Shield, new AFT ages range from 150 ± 8 to 202 ± 14 Ma (Table 1) and are in agreement with published data (139 ± 9 to 256 ± 21 Ma; [START_REF] Leprêtre | Vertical movements along the northern border of the West African Craton : the Reguibat Shield and adjacent basins[END_REF]. New MTLs range from 11.4 ± 0.3 to 12.0 ± 0.2 µm and are undistinguishable from the 11.9 ± 0.2 to 12.4 ± 0.2 µm range for published data (Fig. 3,4). Dpar measurements range from 1.6 ± 0.2 to 2.1 ± 0.5 µm. AHe ages corrected from alpha ejection range from 38 ± 3 to 396 ± 32 Ma (Table 2) with eU content ranging from 7 to 83 ppm. Overall, they are younger than AFT ages with the exception of some replicates from samples AL10 and TGH3163. AHe age vs. eU plot shows a general positive correlation (Fig. 5b).

In the western Reguibat Shield, the two new samples yielded AFT ages of 137 ± 12 Ma and 118 ± 10 Ma with no measurable confined lengths (Table 1). Published AFT ages range from 107 ± 8 to 175 ± 16 Ma, with mean track length (MTL) ranging from 11.8 ± 0.2 µm to 12.5 ± 0.2 µm [START_REF] Leprêtre | Postrift history of the eastern central Atlantic passive margin: Insights from the Saharan region of South Morocco[END_REF]. Track length distributions (TLDs) are largely unimodal, slightly spread around the mean with some complex shapes but for samples with few confined lengths (Fig. 3,4). Dpar measurements range from 1.5 ± 0.2 to 1.8 ± 0.3 µm. Overall, AFT ages are quite homogenous, with a mean around 130-140 Ma. All AFT ages are younger than the 190 Ma rifting [START_REF] Labails | An alternative early opening scenario for the Central Atlantic Ocean[END_REF]. AHe ages corrected from the alpha-ejection range from 14 ± 1 Ma to 185 ± 15 Ma, with an eU content ranging from 7 to 71 ppm. AHe age vs. eU plot shows positive correlations when samples are grouped by region (Fig. 5c) and these AHe age-eU relationships reflect thermal histories with successive reheating/cooling events [START_REF] Leprêtre | Postrift history of the eastern central Atlantic passive margin: Insights from the Saharan region of South Morocco[END_REF]. Lepretre et al. (2015) demonstrated that AHe age scattering within each data set could be explained by radiation damage effects with a secondary role played by variations in apatite chemistry.

Thermal modeling results

For each domain of the Reguibat Shield, we present one representative thermal model with all predicted vs. measured AFT and AHe data (Fig. 6). All individual models are presented in detail in the supplementary data (Fig. S2-S17).. A synthesis with all the thermal paths is given in figure 7. The models for western Reguibat Shield are highly dependent on the constraints determined by [START_REF] Leprêtre | Postrift history of the eastern central Atlantic passive margin: Insights from the Saharan region of South Morocco[END_REF] as neither AHe nor length data are available for the two new samples (Fig. 6g-h).

Sample GH3 illustrates the general shape of the thermal paths for the eastern Reguibat Shield (Fig. 1b, 6a-c). Thermal paths obtained from the inverse modeling for 6 of the 8 samples of this domain are presented in figure 7a. For the best constrained, double LTT dated samples (TL3, GH3, CH1 and CH3), thermal paths show a major cooling episode during the Early Cretaceous. This cooling is variable among samples. At the very end of the Jurassic, samples were generally at temperatures higher than 60°C (except for TL3) and were not undergoing cooling. Results are similar for AFT-dated samples CH2 and DEG6. Whereas the western and central domains suffered post-Early Cretaceous reheating, samples from the eastern domain cooled by 30 ± 10°C and stayed at relatively low temperatures up to the present-day.

For the central Reguibat Shield, the forward modeling with AHe datasets clearly favored the scenario involving the occurrence of a Jurassic-Early Cretaceous cooling event followed by a lowamplitude reheating step (Fig. 8; Table S3). Five forward scenarios were tested: a small Middle Jurassic-Lower Cretaceous cooling with stable thermal conditions during Late Cretaceous (HT1); a large Jurassic-Early Cretaceous cooling (> 40°C) bringing samples close to the surface (HT2 and HT3) before reheating episode; a continuous slow cooling (HT4); a major cooling between Early and Late Cretaceous (HT5). HT1, HT4 and HT5 all provide too young AHe ages compared to the HT2 and HT3. This preliminary treatment confirms the necessity to set a constraint related to the Lower Cretaceous unconformity in the Tindouf Basin and the TLDB. It is also in line with our consideration regarding the wavelength of cratonic deformation at large wavelength. The inverse modeling was conducted using the Lower Cretaceous unconformity and constraints deduced from the forward modeling. The latter suppose that samples were (1) at temperatures higher than 80°C before Early-Middle Jurassic and ( 2) reheated after the beginning of the Early Cretaceous by 20-40°C. We let the inverse modeling determine the temperature before the Jurassic, between 0 and 200°C. Samples with double LTT datings display similar thermal paths (Fig. 6d-f, 7b). A significant cooling event (ΔT > 40°C) is recorded between the beginning of the Jurassic (220-190 Ma) with minimum temperatures reached in the Early Cretaceous (150-140 Ma) ranging from 55 to 45°C. Samples underwent a small reheating event (by 20-25°C) until the beginning of the Late Cretaceous (with the exception of a later and stronger reheating for sample TEN1153). Afterwards, samples cooled down to present-day temperature.

The two samples from the western Reguibat Shield yield similar results than the other samples (Fig. 6g-h, 7c). Their thermal path shows an important cooling from Early-Middle Jurassic to Early Cretaceous, from temperatures higher than 100°C to 35-40°C. A reheating phase occurred until the beginning of Late Cretaceous (between 100-80 Ma), reaching temperatures as high as 65-70°C. It is followed by a rapid cooling event until early Cenozoic up to 35-40°C before a slow cooling until present.

Discussion

Interpretation of LTT data

AFT and AHe ages

Data show a clear increase of AFT and AHe ages towards the east and both datasets also display more scattering eastwards (Fig. 2). From the LTT data and our thermal modelings one can clearly see that samples stayed in the Partial Retention Zone (PRZ)/Partial Annealing one (PAZ) for a long time. This more or less protracted stay within the PRZ strongly impacts the distribution of AHe ages with respect to the eU (Fig. 5). For example, the curved positive trend of the AHe age-eU plot in figure 5b can be explained by low-eU apatites experiencing greater diffusive loss of He (causing younger AHe ages) than high-eU apatites during a short time in the PRZ during Early Cretaceous (10-30 Myrs at T> 50-60°C; Fig. 7b). This short stay within the PRZ was sufficient to partially reset the low-eU AHe ages in the case of the central Reguibat Shield. We consider for now that the best explanation for anomalous replicates behavior (mostly showing older AHe than what is expected) lies in process of implantation of He from minerals neighbouring apatite in the rock [START_REF] Spiegel | Apatite (U-Th-Sm)/He thermochronology of rapidly cooled samples: The effect of He implantation[END_REF].

Up to >300% 4 He excess has been estimated in most extreme cases by [START_REF] Gautheron | Accounting for long alpha-particle stopping distances in (U-Th-Sm)/He geochronology: 3D modeling of diffusion, zoning, implantation, and abrasion[END_REF].

Moreover, low-eU apatites are logically more sensitive to implantation than high-eU apatite and this can dramatically distort the AHe ages [START_REF] Janowski | Neogene exhumation and relief evolution in the eastern Betics (SE Spain): insights from the Sierra de Gador[END_REF]. With this hypothesis, we propose that implantation and a long residence in the PRZ might explain the larger dispersion of the AHe ages for the eastern Reguibat Shield compared to the central Reguibat Shield. In the case of the western Reguibat Shield, [START_REF] Leprêtre | Postrift history of the eastern central Atlantic passive margin: Insights from the Saharan region of South Morocco[END_REF] demonstrated that the apatite crystal chemistry was responsible for an enhanced scattering around a mean AHe age-eU trend (their Fig. 567). In addition to eU and equivalent sphere radius, the influence of apatite composition may also explain some of the scattering seen here given the range of Dpar measurements for the central and eastern Reguibat Shield samples (Tables S1,S2; further discussion in Text S2; Fig. S18).

The NWAC in the Mesozoic

Our results show that the Reguibat Shield experienced significant cooling event between the Early-Middle Jurassic and the Late Cretaceous. This cooling occurred between Early-Middle Jurassic and Early Cretaceous for western and central Reguibat Shield whereas it happened later, by the end of the Early Cretaceous, for the eastern Reguibat Shield. Elevated temperatures during the Early Jurassic can have two origins: (1) a thermal perturbation, linked either to the emplacement of the Central Atlantic Magmatic Province (CAMP, [START_REF] Verati | 40 Ar/ 39 Ar ages and duration of the Central Atlantic Magmatic Province volcanism in Morocco and Portugal and its relation to the Triassic-Jurassic boundary[END_REF] or to thermal flux increase in connection with rifting; (2) a burial under a sedimentary cover which has been removed only after the break-up. Importantly, the CAMP rocks do not crop out within the Reguibat Shield [START_REF] Marzoli | Extensive 200 million-year-old continental flood basalts of the Central Atlantic Magmatic Province[END_REF][START_REF] Verati | The farthest record of the Central Atlantic Magmatic Province into West Africa Craton: Precise 40 Ar/ 39 Ar dating and geochemistry of Taoudenni basin intrusives (northern Mali)[END_REF]. Basal heat flow might have been higher during CAMP magmatism and/or rifting, but would not be anymore anomalous during Cretaceous (Fig. 7b-c). LTT data from borehole samples in the cratonic Anti-Atlas domain, north of the Tindouf Basin [START_REF] Sehrt | Variscan to Neogene long-term landscape evolution at the Moroccan passive continental margin (Tarfaya Basin and western Anti-Atlas)[END_REF] estimate an average 40°C.km -1 palaeogeotherm during the Early-Middle Jurassic/Early Cretaceous without measurable changes afterward. We thus favor the hypothesis of burial of the Reguibat Shield by a Paleozoic sedimentary cover. This cover was removed during Lower-Middle Jurassic/Lower Cretaceous erosion in the western and central Reguibat Shield and fed the clastic deposits of the TLDB during the Early Cretaceous. Similarly, the reheating in the western and central domains between 150 and 100 Ma is interpreted as a re-burial of the samples as no large magmatic anomaly is recorded [START_REF] Matton | The Cretaceous Peri-Atlantic Alkaline Pulse (PAAP): deep mantle plume origin or shallow lithospheric break-up?[END_REF]. The timing and, to a lesser extent, the amplitude of the reburial differs slightly to that proposed in [START_REF] Leprêtre | Vertical movements along the northern border of the West African Craton : the Reguibat Shield and adjacent basins[END_REF]. This can be attributed to the additional AHe datasets used for thermal modeling in the present study. The models differ in the onset and duration of the heating after the Upper Jurassic/Lower Cretaceous transition for models of the central Reguibat (Fig. 7b; Leprêtre et al., 2014, their figure 5). Our present study refines the [START_REF] Leprêtre | Vertical movements along the northern border of the West African Craton : the Reguibat Shield and adjacent basins[END_REF] models and adds more consistency to them. The heating phase occurred from the end of Early Cretaceous up to the beginning of Late Cretaceous (Fig. 7b) when the major Cenomanian-Turonian flooding is recorded. Plus, the beginning of cooling occurred at the beginning of the Late Cretaceous when the Africa-Europe convergence began. We assert that AHe datasets have helped to better constrain the post-Jurassic evolution of central Reguibat Shield, in comparison with our previous investigations using only AFT analysis.

Assuming a palaeogeotherm of 30-50°C.km -1 during the cooling and reheating and using the duration and amplitude of the thermal changes predicted by our thermal models, we estimated the eroded/deposited rock thicknesses for each event. The ranges of Jurassic/Cretaceous erosion are between 0.8-2.1 km and 1-1.6 km from western to eastern Reguibat Shield respectively. The amplitude of re-burial reaches 0.4 to 1.7 km for the western and central domains, with no re-burial in the eastern Reguibat Shield (Fig. 7a). During the re-burial, the southern TLDB record Albian-Turonian thicknesses that can reach 1 km (AUXINI, 1969), which are compatible with our estimates. Moreover this cover might have been even thicker given the subsequent Late Cretaceous erosion. In comparison with western and central domains, the eastern Reguibat Shield shows a late cooling event, mostly occurring at the Lower/Upper Cretaceous transition (Fig. 7a). Whether this cooling can be linked to the one recognized in western and central domains is challenging; however, we believe that cooling in the eastern domain represents another phenomenon. There is no significant time lapse between the cooling phase recorded in the western and central Reguibat Shield. If all three domains were cooled by the same process we would then expect the timing of cooling in the eastern Reguibat Shield to be approximately the same as the west and central domains, which is not the case. As there is a significantly delay before the eastern Reguibat Shield cools, this cooling could better be related to the Austrian phase recognized in the Sahara platform [START_REF] Boudjema | Evolution structurale du bassin pétrolier "triasique" du Sahara nord oriental (Algerie)[END_REF], occurring in Aptian-Albian times. The former N/S Panafrican faults separating the WAC from the Tuareg Shield were reactivated as the northern Tuareg Shield underwent anticlockwise rotation resulting from the opening of the South Atlantic Ocean. The cooling in the eastern Reguibat Shield might stem from the large-scale tectonic reorganization at that time.

Few other studies have dealt with the evolution of cratonic domains on the NWAC. In the Anti-Atlas north of the Tindouf Basin, [START_REF] Ruiz | From central Atlantic continental rift to Neogene uplift -western Anti-Atlas (Morocco)[END_REF] and [START_REF] Oukassou | Post-Variscan exhumation of the Central Anti-Atlas (Morocco) constrained by zircon and apatite fission-track thermochronology[END_REF] demonstrated using LTT data that the northern tip of the craton also underwent uplift and erosion during Jurassic/Early Cretaceous times before a reheating step. Further east (Ahnet-Reggane-Timimoun basins), based on organic matter maturity, AFT and zircon fission-tracks from several wells, [START_REF] Logan | An investigation of the thermal history of the Ahnet and Reggane Basins, Central Algeria, and the consequences for hydrocarbon generation and accumulation[END_REF] proposed a general cooling from Triassic to Early Cretaceous. They also show that the Variscan erosion is highly reduced in most of the area, in agreement with our results. Eastward, in the central and eastern Sahara, the evolution becomes more diverse. In the Illizi Basin, LTT and organic matter maturity were used by [START_REF] English | Intraplate uplift: new constraints on the Hoggar dome from the Illizi basin (Algeria)[END_REF] to support Cenozoic uplift undergone by the Tuareg Shield. However, their borehole data are not able to resolve the Mesozoic history since they found various likely scenarios for the Jurassic-Cretaceous period, with one scenario involving a small cooling event in the Early Cretaceous. A limited number of LTT studies have been undertaken on the Hoggar basement and they are focused on the Cenozoic exhumation without being able to properly address the Mesozoic history given their poor confined length contents and the abundance of Cenozoic AFT ages [START_REF] Carpéna | Evidence of the contrasted fission-track clock behavior of the apatites from In Ouzzal carbonatites (northwest Hoggar): The low-temperature thermal history of an Archean basement[END_REF][START_REF] Cavellec | Evolution diagénétique du basin de Tim Mersoï et conséquences pour la génèse des minéralisations uranifères dans les formations carbonifères du Guezouman et du Tarat (district Arlit-Akokan, Niger[END_REF][START_REF] Rougier | Interactions Lithosphère-Asténosphère et mouvements verticaux : Le cas du massif du Hoggar[END_REF][START_REF] Rougier | Eocene exhumation of the Tuareg Shield (Sahara Desert, Africa)[END_REF].

Evolution of the conjugate passive margins of the Central Atlantic Ocean

Several lines of evidence testify to the existence of common processes on each side of the northern Central Atlantic Ocean during Jurassic-Cretaceous times. We present them in the following section.

LTT record on the onshore eastern American passive margin

Outcrops from the Appalachian orogen and surroundings basins have been used in numerous LTT studies but have never been considered as a whole dataset [START_REF] Crowley | Thermal History of Michigan Basin and Southern Canadian Shield from apatite fission track analysis[END_REF][START_REF] Wang | Thermal History of the Michigan Basin from Apatite Fission-Track Analysis and Vitrinite Reflectance[END_REF][START_REF] Boettcher | Mesozoic-Cenozoic unroofing of the Southern Appalachian Basin: Apatite fission track evidence from Middle Pennsylvanian sandstones[END_REF][START_REF] Roden-Tice | Evidence for Differential Unroofing in the Adirondack Mountains, New York State, determined by apatite fission-track thermochronology[END_REF][START_REF] Roden-Tice | Early Cretaceous Normal Faulting in Southern New England: Evidence from Apatite and Zircon Fission-Track Ages[END_REF][START_REF] Grist | Post-Paleocene cooling in the southern Canadian Atlantic region: evidence from apatite fission track models[END_REF][START_REF] Lorencak | Combined apatite fission track and (U-Th)/He thermochronometry in a slowly cooled terrane: results from a 3440-m-deep drill hole in the southern Canadian Shield[END_REF][START_REF] Spotila | Origin of the Blue Ridge escarpment along the passive margin of Eastern North America[END_REF][START_REF] Roden-Tice | Regional-Scale Mid-Jurassic to Late Cretaceous Unroofing from the Adirondack Mountains through Central New England Based on Apatite Fission-Track and (U-Th)/He Thermochronology[END_REF][START_REF] Taylor | Low-temperature thermal history and landscape development of the eastern Adirondack Mountains, New York: Constraints from apatite fission-track thermochronology and apatite (U-Th)/He dating[END_REF][START_REF] Roden-Tice | Apatite fission-track evidence for the Cretaceous development of kilometer-scale relief and steady-state Tertiary topography in New England[END_REF]. We have collated all of the existing AFT data along eastern North America (Fig. 9a,c). A clear division in AFT ages is observed with young AFT ages along a 600-km wide strip of land parallel to the hinge line (i.e. the place where the continental crust begin to thin toward the ocean; Fig. 1b,9a). The "young" AFT datings range between c.a. 80-180 Ma, with the exception of slightly older samples along the Nova Scotia segment in the north. AFT ages become progressively older landward (up to 600 Ma, beyond 600-700 km off the hinge line). The spatial pattern of AFT age is strikingly similar to the NWAC (Fig. 9b-c; after the data of [START_REF] Ghorbal | Unexpected Jurassic to Neogene vertical movements in "stable" parts of NW Africa revealed by low temperature geochronology[END_REF][START_REF] Saddiqi | Apatite fission-track analyses on basement granites from south-western Meseta, Morocco: paleogeographic implications and interpretation of AFT age discrepancies[END_REF][START_REF] Ruiz | From central Atlantic continental rift to Neogene uplift -western Anti-Atlas (Morocco)[END_REF][START_REF] Oukassou | Post-Variscan exhumation of the Central Anti-Atlas (Morocco) constrained by zircon and apatite fission-track thermochronology[END_REF] this study), with ages being younger (c.a. 100-220 Ma) from the coast to 600 km. AFT-MTL plots are given for both margins (Fig. 9c-d) and show that there is no relationship between the age of rifting and length datasets. This significant observation means that for samples within the 600/700-km proximal land strip, the effects of the Lower Jurassic rifting (c.a.

190 Ma) are barely distinguishable. Both margins seem coherently affected by a more regional event.

Along-strike variations of the passive margin stratigraphical record

Passive margin sedimentary infills have been studied along both passive margins and can be compared to identify the similarities in their evolution. For this comparison, we use the regional studies of [START_REF] Jansa | Mesozoic-Cenozoic Development of the Eastern North American and Northwest African continental margins: a comparison[END_REF] for Northwest Africa, Grew & Sheridan (1988) and [START_REF] Miall | The Atlantic Margin Basins of North America[END_REF] for eastern North America. In the following, we present only the stratigraphical records from Early-Middle Jurassic to the end of Early Cretaceous.

From north to south along the eastern American passive margin, four segments have been well-documented: Nova Scotia, the Georges Bank, the Baltimore canyon Trough and the Blake plateau (Fig. 10). On the African counterpart, we will present the Essaouira, Tarfaya and Senegal segments.

The Nova Scotia and Georges Bank basins and the Baltimore Canyon Trough are defined by similar stratigraphical formations. The Early Jurassic witnessed the deposition of dolomite and anhydrite layers. These unconformably overlie Triassic formations and gradually became clastic deposits moving laterally and upward in the section. On top of the Early Jurassic rocks, a large carbonate platform aggraded and prograded seaward although a clastic influx still occurred during Middle-Late Jurassic. During Early Cretaceous, carbonate platforms were buried under a thick clastic influx of coarse sandstones, which even bypassed the platform edge (Jansa & Wiedman, 1982;Wade & MacLean, 1990). By the end of the Early Cretaceous, clastic sedimentation was still ongoing but with a lower influx during the Aptian-Turonian interval when a major transgressive period occurred.

South of these three basins, the Blake Plateau has received little attention. Its Middle Jurassic stratigraphy is less known but the Late Jurassic witnessed the formation of a mixed terrigenouscarbonated platform and the build-up of a massive carbonate platform occurred during the Early Cretaceous. The platform was drowned during the Late Cretaceous due to the high-stand sea-level which brought carbonate facies up to the Appalachian range with the deposition of deep-marine marls on the former carbonate platform [START_REF] Poag | Mesozoic and Cenozoic stratigraphy of the United States Atlantic continental shelf and slope[END_REF].

On the northwest African passive margin, [START_REF] Jansa | Mesozoic-Cenozoic Development of the Eastern North American and Northwest African continental margins: a comparison[END_REF] described very similar successive facies. In the Essaouira Basin, middle-upper Liassic (Lower Jurassic) records the early postrift transgression with the deposition of dolomites and evaporites, subsequently covered during lower-middle Dogger (Middle Jurassic) by clastics with features characteristic of a marine regression.

A stable carbonate platform was built afterwards up to the end of the Late Jurassic. Carbonate deposition was interrupted by some clastic deposition before a last regression in Berriasian times.

The Lower Cretaceous formations buried the former platform under kilometer-thick clastics with large prograding deltas until the Aptian. Marine conditions resumed during Aptian with carbonate deposition. From the Cenomanian-Turonian onwards, deeper marine conditions prevailed with outer-shelf to slope type deposit. In the TLDB, the sedimentary record is similar to that in the Essaouira Basin. Finally, in the southern segment of the Senegal Basin, a large carbonate platform formed during the Middle-Late Jurassic to the end of Early Cretaceous. In contrast to the northern segments, deposition of the carbonate platform was not interrupted and small volumes of clastic sediments deposited in the Senegal Basin [START_REF] Brownfield | Assessment of the undiscovered oil and gas of the Senegal Province, Mauritania, Senegal, The Gambia, and Guinea-Bissau, Northwest Africa[END_REF]. A carbonate platform even prevailed until the Late Cretaceous in the southern part of the basin.

The overall stratigraphical record on both sides of the Central Atlantic Ocean is strikingly similar for the considered period. It becomes increasingly different afterwards in the Late Cretaceous [START_REF] Jansa | Mesozoic-Cenozoic Development of the Eastern North American and Northwest African continental margins: a comparison[END_REF] during the convergence climax of Africa and Europe. For the whole margin, the Jurassic witnessed the build-up of an almost continuous carbonate platform, which ended in the beginning of the Early Cretaceous for the north Central Atlantic Ocean whereas this build-up persisted until the Late Cretaceous for the southern segments of the margin. Given the LTT record for both sides of the northern Central Atlantic Ocean described previously, we consider that this abundant clastic feeding of the margins during the Neocomian must be related to a common process which will be discussed in the next section.

Evolution of the Central Atlantic Ocean

The Central Atlantic Ocean underwent break-up during the Sinemurian (~190 Ma; [START_REF] Labails | An alternative early opening scenario for the Central Atlantic Ocean[END_REF]. During rifting and the early post-rift stage, a shared stratigraphical record is observed predictably on both sides of the ocean [START_REF] Jansa | Mesozoic-Cenozoic Development of the Eastern North American and Northwest African continental margins: a comparison[END_REF]; Fig. 10). The spreading rate of the young Atlantic has been estimated by various authors [START_REF] Cogné | Trends and rythms in global seafloor generation rate[END_REF][START_REF] Schettino | Breakup of Pangaea and plate kinematics of the central Atlantic and Atlas regions[END_REF][START_REF] Labails | An alternative early opening scenario for the Central Atlantic Ocean[END_REF][START_REF] Kneller | Inverse methods for modeling non-rigid plate kinematics: Application to Mesozoic plate reconstructions of the Central Atlantic[END_REF] for the Jurassic period. We present in figure 11 a compilation of these rates. Even if slight differences exist between the different models, all authors agree with a significant increase of this rate during Middle and Late Jurassic before a dramatic decrease in the Early Cretaceous.

One must remember that LTT studies only give the simplest thermal paths between constraint points that can reproduce the data. As such, the Jurassic-Early Cretaceous cooling we obtained could alternate between discrete phases of accelerations and decelerations of the cooling rate from the Early-Middle Jurassic to the Early Cretaceous. Considering the regression and clastic burial of the Jurassic carbonate platforms, we think that an acceleration of the cooling rate would have occurred during the Late Jurassic/Early Cretaceous because of enhanced exhumation. This process can also be suggested for the symmetrical clastic feeding on the conjugate American passive margin. Indeed, LTT studies on eastern North America suggest that a significant cooling occurred over large areas during the Middle-Late Late Jurassic to the Early Cretaceous (Fig. 12a-c). This cooling event is partially hidden in the northern Appalachian domain (central transect, the portion close to the Atlantic Ocean in figure 9) where, a strong Early-Late Cretaceous cooling event is attributed to the passage over/close to the Great Meteor hotspot [START_REF] Taylor | Low-temperature thermal history and landscape development of the eastern Adirondack Mountains, New York: Constraints from apatite fission-track thermochronology and apatite (U-Th)/He dating[END_REF], which could have disrupted the record of the earliest cooling phase (Fig. 12d).

Valid explanations for this Jurassic-Lower Cretaceous uplift must consider the following: (1) the uplift event affected the onshore domains of either side of the conjugate passive margins and over a longer wavelength than it is typically the case usually for other passive margins settings (up to 600 km landward compared to less than 200-300 km; see [START_REF] Gallagher | Fission track analysis and its applications to geological problems[END_REF]; [START_REF] Turner | Thermal history of the Rio Muni)-NE Brazil margins during continental breakup[END_REF] in spite of a shared spreading history [START_REF] Labails | An alternative early opening scenario for the Central Atlantic Ocean[END_REF], the Central Atlantic Ocean behaved differently at that time and was split into a northern domain, whose margins were uplifted and a southern domain, which experienced the continuous build-up of carbonate platforms (Fig. 10); (3) it must be followed by a significant burial stage during the Early Cretaceous on the western and central Reguibat Shield, with decreasing intensity landward. This burial is not evidenced on the American conjugate margin and thermal stability has been retained after these changes (e.g. Taylor & Fitzgerald, 2011, their fig. 8;Roden-Tice et al., 2012, their fig. 6-7).

The exhumation recorded on both margins peaked during the post-rift phase, interrupting the classical subsidence post-rift phase, associated with the carbonated platform build-up. It is difficult to argue that early post-rift geomorphological models like scarp retreat or pinned-divide [START_REF] Gallagher | Fission track analysis and its applications to geological problems[END_REF] could be responsible for the distribution of the AFT ages and the evolution of the margin. The NW African passive margin is characterized by a low-elevation profile which does not seem to indicate any erosion retreat and that these rift-related processes usually exert themselves on more restricted geographical scales (< 300 km inland). Moreover, huge erosion on the coastal plain (and commonly ONLY studied for high-elevation passive margins) is classically explained by primary controls such as the geometry of the rifting and the flexural rebound (see Bishop, 2007 and[START_REF] Green | Stratigraphic landscape analysis, thermochronology and the episodic development of elevated, passive continental margins[END_REF] for contrasted reviews). In our studied case, the asymmetrical mechanism of rifting and the different crust-lithosphere geometries of the conjugate margins do not argue for both margins to behave in such a similar way [START_REF] Maillard | Imaging a lithospheric detachment at the continent-ocean crustal transition off Morocco[END_REF][START_REF] Labails | Crustal structure of the SW Moroccan margin from wide-angle and reflection seismic data (the Dakhla experiment). Part B -The tectonic heritage[END_REF]. We also discard an explanation involving regional compression to account for these results in the western and central domains of the Reguibat Shield and the American conjugate passive margin. [START_REF] Bertotti | Post-rift vertical movements and horizontal deformations in the eastern margin of the Central Atlantic: middle Jurassic to Early Cretaceous evolution of Morocco[END_REF] proposed this tectonic hypothesis for northern Morocco over the Late Jurassic/Early Cretaceous.

However, their arguments are based on limited structural evidence that is focused on their study area. These features could also be explained as being halokinesis features (e.g. Saura et al., 2014).

Additionally, pre-Late Cretaceous compressional features have never been described on the Moroccan-Mauritanian passive margin during this period, before the onset of Africa-Europe convergence [START_REF] Rosenbaum | Relative motions of Africa, Iberia and Europe during Alpine orogeny[END_REF].

We propose a hypothesis that involves mantle-related dynamic processes to account for the symmetrical uplifts on both sides of the northern Central Atlantic. The geographical extension of the eroded area points to a large-scale process, which could be attributed to ascending hot mantle material below the northern Central Atlantic Ocean. During Late Jurassic-Early Cretaceous, magmatism is absent across both margins (see the review by [START_REF] Matton | The Cretaceous Peri-Atlantic Alkaline Pulse (PAAP): deep mantle plume origin or shallow lithospheric break-up?[END_REF]. Scarce basic magmatic outcrops exist in northern Morocco (Frizon de [START_REF] Frizon De Lamotte | The Atlas system[END_REF] and in North America [START_REF] Mchone | Mesozoic igneous provinces of New England and the opening of the North Atlantic Ocean[END_REF] from this period. Their absence over most of the NWAC can be explained by lack of structural pathways that allow the magma to pierce through the cratonic domain of the Reguibat Shield. Spreading of a large shallow plume head below the northern Central Atlantic Ocean lithosphere is thus not discarded but it would have to have impacted the base of the lithosphere at a lower temperature than typical plume heads or at great sub-lithospheric depths, which therefore prevent the development of a large volume of magmatism. Such a large hot mantle would have had wide reaching effects at this time and would have impacted Northwest Africa and eastern North America (this study), and even Iberia (e.g. [START_REF] Grobe | Mesozoic exhumation history and paleolandscape of the Iberian Massif in eastern Galicia from apatite fission-track and (U+Th)/He data[END_REF]. The timing of the mantle plume is concomitant with the second phase of the rifting between Iberia and Newfoundland [START_REF] Tucholke | Breakup of the Newfoundland-Iberia rift[END_REF]. The delay between the increase in Middle-Upper Jurassic spreading rates in the Central Atlantic Ocean and the Lower Cretaceous clastic influx to the margins (Fig. 10,11) is consistent with the lag time for the thermal mantle anomaly to reach the surrounding continents and create uplift.

On a smaller scale, such a mechanism, as proposed here, could be similar to the "hot pulses" linked to the Icelandic plume that spread out radially beneath the lithosphere as proposed by [START_REF] Hartley | Transient convective uplift of an ancient buried landscape[END_REF] to explain various Cenozoic uplifts in this area of North Atlantic Ocean. In our case, the more important Mesozoic uplift-burial cycle affecting Northwest Africa is interpreted as being a result of NW Africa residing closest to an underlying mantle thermal anomaly compared to the conjugate margin. This has resulted in a stronger dynamic uplift effect which triggered episodes of erosion and burial that are able to be recorded by LTT methods. After the "dynamic pulse" that pushed upward the NWAC, its decrease led consequently to an opposite trend in the western and central Reguibat domains that allowed the re-burial of the margin in the extent revealed by our study, fading eastward within the craton. A potential contribution of eroding material from the eastern Reguibat Shield to this burial may be possible. Nevertheless, we are not able to properly evaluate this contribution since no sedimentary remnants are preserved within the Reguibat Shield nowadays.

Conclusion

This LTT study evidenced a Lower-Middle Jurassic to Upper Cretaceous kilometric erosion event that occurred in the previously presumed to be stable Northwest Africa. This result has major consequences for the Reguibat Shield and Northwest Africa and is probably related to the Central Atlantic expansion.

Along a roughly E-W ~1300 km transect of the Reguibat Shield, we show that kilometer-scale erosion occurred from Early-Middle Jurassic to the Early Cretaceous for the western and central domains. The eastern domain of the Reguibat Shield also underwent an erosional event but it occurred later in the Early Cretaceous. The erosion of central and western domains was followed by subsequent reheating/burial with decreasing intensity landward, before final cooling from Late Cretaceous to present-day in western and central Reguibat Shield domains. For eastern Reguibat Shield domain, the brief pulse of erosion can be identified at the Lower-Upper Cretaceous transition and we may tentatively relate it to the Austrian unconformity.

These results have important implications when placed in the wider context of the geodynamic setting of the Central Atlantic Ocean evolution. We demonstrate a similar pattern of erosion occurring on the conjugate passive margin of eastern North America during the same period. This long wavelength uplift event only affected the northern part of the continents surroundings the young ocean and has an extent compatible with transient large scale mantle processes. A lowtemperature or deeply located sub-lithospheric mantle plume head responsible for this uplift is concomitant with the second and last phase of rifting in the southern North Atlantic Ocean and could have played a significant role in triggering its oceanic opening. For the western domain, black thermal paths correspond to the thermal modelings realized by [START_REF] Leprêtre | Postrift history of the eastern central Atlantic passive margin: Insights from the Saharan region of South Morocco[END_REF]. Due to the new AHe data, we have made new thermal modeling for the data from the central domain obtained by [START_REF] Leprêtre | Vertical movements along the northern border of the West African Craton : the Reguibat Shield and adjacent basins[END_REF]. For all modelings, the way we have defined the constraint-boxes is explained within the text. AFT datings along perpendicular profiles, from the hinge line at x=0. For the African AFT profile, data are from: [START_REF] Ghorbal | Unexpected Jurassic to Neogene vertical movements in "stable" parts of NW Africa revealed by low temperature geochronology[END_REF]; [START_REF] Saddiqi | Apatite fission-track analyses on basement granites from south-western Meseta, Morocco: paleogeographic implications and interpretation of AFT age discrepancies[END_REF]; [START_REF] Ruiz | From central Atlantic continental rift to Neogene uplift -western Anti-Atlas (Morocco)[END_REF]; [START_REF] Oukassou | Post-Variscan exhumation of the Central Anti-Atlas (Morocco) constrained by zircon and apatite fission-track thermochronology[END_REF], [START_REF] Leprêtre | Vertical movements along the northern border of the West African Craton : the Reguibat Shield and adjacent basins[END_REF][START_REF] Leprêtre | Postrift history of the eastern central Atlantic passive margin: Insights from the Saharan region of South Morocco[END_REF] and this study. For the American profile, data come from the studies quoted in the text. Smaller panels on each profile show the MTL vs. AFT age plot. The grey bar indicates the age range of the rifting of the Central Atlantic Ocean [START_REF] Labails | An alternative early opening scenario for the Central Atlantic Ocean[END_REF]. Cretaceous. This compilation is based on works by [START_REF] Schettino | Breakup of Pangaea and plate kinematics of the central Atlantic and Atlas regions[END_REF], [START_REF] Labails | An alternative early opening scenario for the Central Atlantic Ocean[END_REF] and [START_REF] Kneller | Inverse methods for modeling non-rigid plate kinematics: Application to Mesozoic plate reconstructions of the Central Atlantic[END_REF]. Fig. 12: Representative thermal paths from the onshore eastern North America. Thermal paths are coming from: (a) Nova Scotia in the northern proximal passive margin (Grist & Zentili, 2003); (b) the Michigan Basin, deep in the interior of the continent [START_REF] Wang | Thermal History of the Michigan Basin from Apatite Fission-Track Analysis and Vitrinite Reflectance[END_REF]; (c) the southern Canadian Shield [START_REF] Lorencak | Combined apatite fission track and (U-Th)/He thermochronometry in a slowly cooled terrane: results from a 3440-m-deep drill hole in the southern Canadian Shield[END_REF]; (d) the Northern Appalachian [START_REF] Taylor | Low-temperature thermal history and landscape development of the eastern Adirondack Mountains, New York: Constraints from apatite fission-track thermochronology and apatite (U-Th)/He dating[END_REF]. Dark grey box defines the main period of uplift in the western and central Reguibat Shield domains in the conjugated African passive margin. corresponds to a kinetic factor determined for each sample [START_REF] Barbarand | Compositional and structural control of fissiontrack annealing in apatite[END_REF]. The thermal modeling for western RS samples is briefly recalled here. The reader is invited to read the extensive description given in [START_REF] Leprêtre | Postrift history of the eastern central Atlantic passive margin: Insights from the Saharan region of South Morocco[END_REF].

Figure captions

The modeling of samples of the western RS was done through three steps, given the complexity of the dataset. A first step of inverse modeling was used as an exploratory tool to search the (T, t) space. The stratigraphical constraint given by the unconformity of the Lower Cretaceous deposits and a data-dependent constraint implying samples to be at temperatures higher than 110°C before 200 Ma were incorporated in the modeling to narrow the exploration of the (T, t) space.

Second, representative thermal histories obtained in the first step were discriminated using the forward modeling. They implied further restrictions on the available (T,t) paths that were incorporated as constraints in the third step of the modeling. The last step used inverse modeling with all determined constraints during the early steps to explore the degrees of freedom left to the model to better fit the data. This three-step procedure led to four major constraints that we re-use here to model the AFT ages of AG167 and AG169 samples: (1) samples were at temperatures higher than 110°C before 200 Ma; (2) samples were near or at the surface during the Early Cretaceous; (3) a necessary reheating step occurred until the beginning of the Late Cretaceous; (4) a subsequent cooling up to 40°C by the end of the Late Cretaceous.

Text S2 -influence of apatite chemistry on the single-grain AHe ages scattering

To investigate the influence of the chemistry on the scattering of the single-grain AHe age, we used the mean thermal paths obtained through thermal modeling for all samples with AHe datasets. With forward modeling, we consider the whole range of Dpar and grain size of single grain within each sample. The grain size range is approximated through the equivalent sphere radius (Rs; see Table 2). The chemistry variations are taken into account through the rmr0 factor, as defined by [START_REF] Ketcham | Improved modeling of fission-track annealing in apatite[END_REF]. An empirical relationship links the Dpar and the rmr0 through the following equation: rmr0 = 0.84 x [(4.58-Dpar)/2.98] 0.21 , the rmr0 being used as the chemical determinant for the forward modeling with HeFTy for our tests.

We tested each final thermal path in forward modeling, varying the values of rmr0 and Rs. For an eU range, we then reported the obtained AHe age-eU relationship for the four couple (rmr0; Rs) tested (Fig. S17). One can see on figure S17 that generally, the single-grain AHe ages scattering can simply depend on these two parameters. Some out-of-trend replicates need others explanations, like the shape of broken apatite crystals [START_REF] Brown | Natural age dispersion arising from the analysis of broken crystals. Part I: Theoretical basis and implications for the apatite (U-Th)/He thermochronometer[END_REF] or contamination [START_REF] Gautheron | Accounting for long alpha-particle stopping distances in (U-Th-Sm)/He geochronology: 3D modeling of diffusion, zoning, implantation, and abrasion[END_REF]. [START_REF] Barbarand | Compositional and structural control of fissiontrack annealing in apatite[END_REF].

Reguibat East

Sample

Fig. 1 :

 1 Fig. 1: Geological map of the Reguibat Shield and location of the samples. (a) Geographical location of

Fig. 2 :

 2 Fig. 2: Segmentation of the Reguibat shield based on the LTT results. The data are projected along a

Fig. 3 :

 3 Fig. 3: AFT age vs. MTL plot for the whole Reguibat Shield. The grey bar indicates the timing and

Fig. 4 :

 4 Fig. 4: Track length distributions for all samples. They are separated by geographical area. Samples

Fig. 5 :

 5 Fig. 5: Corrected AHe ages vs. eU plots. (a) for the eastern Reguibat Shield; (b) for the central

Fig. 6 :

 6 Fig. 6: Representative individual modeling for each domain of the Reguibat Shield. (a) Thermal

Fig. 7 :

 7 Fig. 7: Inverse thermal modelings for the three Reguibat Shield domains. (a-c) Thermal modeling

Fig. 8 :

 8 Forward modeling for the central Reguibat Shield. (a) Tested thermal paths with HeFTy software[START_REF] Ketcham | Forward and Inverse modeling of Low-temperature Thermochronometry data[END_REF]. (b) Corresponding predicted AHe ages for each tested thermal path in (a). The measured Ft-corrected single-grain AHe ages are also indicated to ensure direct comparison. A small simplified map of the Reguibat Shield shows the segmentation between the different domains.

Fig. 8 :

 8 Fig. 8: Forward and inverse modeling for the central Reguibat Shield. (a) Tested thermal paths with

Fig. 9 :

 9 Fig. 9: Comparison between AFT datasets of the conjugate passive margins of the northern Central

Fig. 10 :

 10 Fig. 10: Comparison of Middle Jurassic-Aptian stratigraphical record of Central Atlantic Ocean

Fig. 11 :

 11 Fig. 11: Evolution of the spreading rates in the Central Atlantic Ocean from Early Jurassic to Early

  ) and F T (ejection factor) have been calculated using the developed procedure ofGautheron & Tassan-Got (2010) andKetcham 1053[START_REF] Ketcham | Accounting for long alpha-particle stopping distances in (U-Th-Sm)/He geochronology: refinement of the baseline case[END_REF]. eU (effective uranium) has been calculated with the formula [eU] = [U] + 0.24*[Th] + 0.008*[Sm]. "Age c." means (U-Th-Sm)/He age corrected 1054 from alpha-ejection with the F T . The error is estimated to be a maximum of 8%.

Figure 1 Figure 2 Figure 3

 123 Figure 1

Figure 4 Figure 5

 45 Figure 4

Figure 5 Figure 6 Figure 7 Figure 8

 5678 Figure 5

Figure 9 Figure 10 Figure 11

 91011 Figure 9

-

  Figure 12

Figure S1 :

 S1 Figure S1: Thermal modeling of AL10 sample with all single-grain AHe ages. The figure must be compared with figure S12. It shows the instabilities produced by the use of anomalous replicates. . (a) Thermal history with different outputs (see details in Gallagher, 2012); (b) Evolution of the LL and the number of T(t) points during the post-burn-in phase; (c) Predicted parameters for the expected model (black line in (a)). In red line is the predicted length distribution (superimposed on blue histogram in other samples). LL: LogLikelihood; FTA: fission track age; MTL: mean track length; Kin: Dpar; O: observed; P: predicted.

Figure S2 :

 S2 Figure S2: Thermal modeling of CH2 sample. (a) Thermal history with

Figure S4 :

 S4 Figure S4: Inverse modeling for sample CH1. Same legend as in figure S2. (d) observed vs. predicted AHe ages.

Figure S5 :

 S5 Figure S5: Inverse modeling for sample CH3. Same legend as in figures S2 and S4.

Figure S6 :

 S6 Figure S6: Inverse modeling for sample TL3. Same legend as in figures S2 and S4.

Figure S7 :

 S7 Figure S7: Inverse modeling for sample GH3. Same legend as in figures S2 and S4.

Figure S8 :

 S8 Figure S8: Inverse modeling for sample YT7. Same legend as in

Figure S9 :

 S9 Figure S9: Inverse modeling for sample TGH3111B. Same legend as

Figure S10 :

 S10 Figure S10: Inverse modeling for sample TEN4065. Same legend as

Figure S11 :

 S11 Figure S11: Inverse modeling for sample TGH4072A. Same legend as

Figure S12 :

 S12 Figure S12: Inverse modeling for sample AL10. Same legend as in figures S2 and S4.

Figure S13 :

 S13 Figure S13: Inverse modeling for sample TEN1153. Same legend as in figures S2 and S4.

Figure S14 :

 S14 Figure S14: Inverse modeling for samples TEN1185. Same legend as in figures S2 and S4.

Figure S15 :

 S15 Figure S15: Inverse modeling for sample TGH3163. Same legend as in figures S2 and S4.

Figure S16 :

 S16 Figure S16: Inverse modeling for sample AG167. Same legend as in figure S2.

Figure S17 :

 S17 Figure S17: Inverse modeling for sample AG169. Same legend as

Figure S18 :

 S18 Figure S18: Compositional chemical variations in apatites

  ) and F T (ejection factor) have been calculated using the developed procedure ofGautheron & Tassan-Got (2010) and[START_REF] Ketcham | Accounting for long alpha-particle stopping distances in (U-Th-Sm)/He geochronology: refinement of the baseline case[END_REF]. eU (effective uranium) has been calculated with the formula [eU] = [U] + 0.24*[Th] + 0.008*[Sm]. "Age c." means (U-Th-Sm)/He age corrected from alpha-ejection with the F T . The error is estimated to be a maximum of 8%.

  Western and central Reguibat Shield domains are differentiated based on their AHe age ranges. AHe ages from western Reguibat Shield are younger than 127 Ma (only one replicate is older) whereas they range from 38 to 191 Ma for central Reguibat Shield (4 of 11 AL10 replicates are out of the trend) with significantly older AHe ages at eU > 20 ppm. Compared to central Reguibat Shield (AFT range: 139 to 256 Ma; AHe range: 38 to 269 Ma when excluding the two anomalously old AL10 replicate; see Table 2), eastern Reguibat Shield yielded significantly older AFT ages (237 to 497 Ma against 139 to 256 Ma for central Reguibat; Table

Table 1 :

 1 AFT results* 1041 ρ -density of tracks with s and i -spontaneous and induced densities in apatite crystals and the mica detector; d -tracks density of the neutron glass monitor (CN5); for ρs, ρi,ρd, are written in italics the number of counted tracks. Densities are expressed in 10 5 t/cm 2 . MTL -mean track length. Values in bracket for central age and MTL are, respectively, the number of single-grain ages and the number of lengths measured. 1σ is the standard deviation. Dpar

		Sample	Rock-type	Location	Elevation (m)	ρ s (10 5 .cm-²) / Ns	ρ i (10 5 .cm-²) / Ni	ρ d (10 5 .cm-²) / Nd	P (χ²) %	Central age (Ma) ± 1σ	U (ppm)	MTL (µm) ± se	Std dev.	Dpar (µm)
	Western	AG167	charnockite	13°24'2.07"W	233	0.218	0.195	6.73	74	137 ± 12	4	-	-	1.72 ± 0.1
	domain			20°42'56.76"N		323	289	6849		(20)		-	-
		AG169	charnockite	13°24'2.07"W	237	0.201	0.207	6.682	93	118 ± 10	4	-	-	1.54 ± 0.2
				20°42'56.76"N		309	319	6849		(20)
	Central TGH3111B	granite	9°22'12"W	252	3.246	2.598	6.611	65	150 ± 8	48	11.9 ± 0.2	1.7	1.63 ± 0.1
	domain			24° 00'00"N		1097	878	6563		(20)		(101)
		TEN4065 microgranite 10° 1'47.00"W	258	6.444	4.462	6.595	8	172 ± 13	82	11.7 ± 0.3	2	2.06 ± 0.5
				24°20'23.00"N		883	477	6563		(20)		(35)
		AL10	granodiorite	7° 7'5.15"W	394	1.334	0.866	7.255	63	202 ± 14	15	12 ± 0.2	1.6	1.77 ± 0.1
				26°37'33.06"N		675	438	6849		(20)		(49)
		YT7	monzogranite 7°20'37.34"W	384	1.862	1.394	6.825	72	166 ± 8	25	11.4 ± 0.3	1.8	1.60 ± 0.2
				26°28'59.39"N		1380	1033	6849		(20)		(49)
	Eastern	IG3	rhyolite	6° 9'0.43"W	366	0.469	0.149	6.968	84	393 ± 36	3	-	-	1.66 ± 0.2
	domain			26° 6'22.40"N		543	172	6849		(20)		-
		CH1	gabbrodiorite 3°35'36.69"W	252	1.098	0.454	7.159	6	307 ± 26	8	11.5 ± 0.2	2.1	1.86 ± 0.2
				25°35'45.94"N		862	356	6849		(20)		(101)
		CH2	gabbrodiorite 3°35'36.69"W	252	3.105	1.516	7.112	18	264 ± 21	26	12 ± 0.2	1.7	1.99 ± 0.2
				25°35'45.94"N		770	376	6849		(20)		(69)
		CH3	gabbrodiorite 3°35'36.69"W	252	1.059	0.426	7.064	86	315 ± 24	7	11.5 ± 0.3	2.3	1.95 ± 0.2
				25°35'45.94"N		686	276	6849		(20)		(64)
		GH3	trondhjemite	6° 3'54.77"W	360	1.177	0.41	7.016	6	359 ± 27	7	11.5 ± 0.2	1.9	1.76 ± 0.2
				25°29'36.53"N		1130	394	6849		(20)		(100)
		DEG6	gabbro	2°57'15.60"W	355	2.276	0.701	6.111	46	355 ± 25	12	11.2 ± 0.4	2.1	1.97 ± 0.1
				26° 4'50.02"N		1065	328	6849		(20)		(27)
		GH20	gabbro	6° 0'2.87"W	350	0.471	0.101	5.996	73	497 ± 61	2	-	-	1.75 ± 0.1
				25°32'51.89"N		206	44	3012		(10)		-
		TL3	gabbro	3°10'37.45"W	381	0.818	0.376	6.052	66	237 ± 21	8	-	-	2.12 ± 0.2
				27°21'31.99"N		447	207	3012		(20)		-

*

Table 2 :

 2 AHe results* 1051

		Name Rs (µm) Weight(µg)	F T	4 He(ncc/g) U (ppm) Th (ppm) Sm (ppm) eU (ppm) Age (Ma) Age c. (Ma)
	Central	1153-A	80.8	11.85	0.87	46201.6	3.8	11.9	7.0	6.7	57	66 ±
	Domain	1153D	34.4	1.17	0.715	120399,0	10.4	31.9	20.3	18.3	55	77 ±
		1153-F	63.2	6.54	0.815	100000.8	7.6	20.3	9.5	12.6	66	81 ±
		1153-H	59	4.69	0.83	63086.4	11.2	22.6	12.5	16.7	31	38 ±
		1153-I	47.5	2.56	0.79	57756,0	5.5	16.8	13.3	9.6	50	63 ±
		3163-A	54.1	3.6	0.809	717183.1	37.7	1.9	27.2	38.3	155	191 ±
		3163-E	66	7.11	0.827	288616.5	16.9	1.4	17.6	17.4	137	166 ±
		3163-I	65.6	6.26	0.847	470679.8	17.8	25.6	24.6	24.1	162	191 ±
		3163G	96.1	17.27	0.875	549045.6	25,0	22,0	NA	30.3	150	172 ±
		AL10-A	46	2.4	0.755	405681.5	22.5	20.6	31.8	27.7	121	161 ±
		AL10-E	39.3	1.18	0.701	675195,0	76.1	26.7	31.3	82.8	67	96 ± 8*
		AL10-C	50.5	3.53	0.765	229447.2	11.1	11.9	29.3	14.2	134	175 ±
		AL10-L	44.1	1.57	0.679 1341456.8	34.3	31.1	59.4	42.2	263	388 ± 31*
		AL10-J	37.2	1.22	0.724	231868.3	7.9	10,0	37.4	10.5	182	252 ±
		AL10-I	45.5	2.02	0.76	395904.9	22.4	14.9	41,0	26.3	124	164 ±
		AL10-B	39	1.39	0.726	557702.2	20.6	11.6	37.5	23.7	195	269 ±
		AL10-K	37.9	1.28	0.717	145483.1	12.5	8.8	35.5	14.9	81	112 ± 9
		AL10-F	38.7	1.23	0.687	129286.7	9.5	15.8	44.8	13.6	79	115 ± 9
		AL10-G	39.9	1.23	0.707 1327362.4	32.4	26.5	65.3	39.3	280	396 ± 32*
		AL10-H	42.6	1.58	0.713	236976.2	18.4	18.2	50.1	23.2	85	119 ±
	Eastern	CH1-A	47.3	2.43	0.789	79475.1	7.2	6.9	5.3	9	74	93 ±

Table S1 :

 S1 AFT results* for the Reguibat Shield density of tracks with s and i -spontaneous and induced densities in apatite crystals and the mica detector; d -tracks density of the neutron glass monitor (CN5); for ρd is written in italics the number of counted tracks. Densities are expressed in 10 5 t/cm 2 . MTL -mean track length. Values in italics for central age and MTL are, respectively, the number of single-grain ages and the number of lengths measured. 1σ is the standard deviation. Dpar corresponds to a kinetic factor determined for each sample

			22°32'N		1301	1241	6528		21		100
	AOS5	syénite neph	14°17'W	400	1.381 1.308	6.55	1	128 ± 8	24	11.8 ± 0.19	1.8	1.79 ± 0.33
	Reguibat Central	22°32'N		1153	1092	6528		21		92
	SC11	granite	14°21'38''W	293	0.85	0.627	6.5	50	160 ± 11	12	12.1 ± 0.33	1.8	1.75 ± 0.28
	Sample	Rock-type	Location 22°34'36''N	Elevation	ρ s 604	ρ i 446	ρ d 6528	P (χ²) % Central age (Ma) ± 1σ U (ppm) MTL (µm) ± se Std dev. 21 32	Dpar
	SC12	granite	14°23'00''W	(m) 292	1.383 1.155	6.47	27	141 ± 8	22	12.2 ± 0.17	1.8	1.54 ± 0.22
	TEN1153	gabbro	10° 30' 36"W 22°35'14''N	216	0.759 0.333 1094 914	6.14 6528	73	256 ± 21 21	7	12.3 ± 0.22 108	2.3	2.89 ± 0.29
	TCH7	granite	24° 1' 12"N 15° 6'37.25"W	194	581 0.955 0.889 255	4738 6.52	27	23 127 ± 8	17	102 9.4 ± 0.27	2	1.60 ± 0.36
	TEN1185	gabbro	10° 30' 0"W 21°50'54.88"N	236	2.652 1.806 916 853	6.07 6528	62	163 ± 10 21	36	12.4 ± 0.21 37	2.1	1.13 ± 0.43
			24° 6' 36"N		875	596	4738		23		101
	TGH3163 SC5	granite granite	9° 52' 48"W 14°29'38.00"W	305 284	1.546 1.219 1.04 0.839	5.99 6.657	44 < 1	139 ± 9 156 ± 15	25 15	11.9 ± 0.18 10.7 ± 0.31	1.8 1.7	1.95 ± 0.12 1.63 ± 0.10
			24° 52' 48"N 22°40'50.00"N		881 1131	695 913	4738 6563		20 20		101 32
	TGH4072A	granite	9° 43' 12"W	273	1.784 0.964	5.92	68	199 ± 13	20	12.4 ± 0.15	1.6	1.02 ± 0.11
	SC9	granite	24° 28' 48"N 14°18'56.00"W	318	883 1.742 1.549 477	4738 6.641	< 1	20 143 ± 13	28	113 11.2 ± 0.35	1.9	1.70 ± 0.11
	TGH3111B	granite	9°22'12"W 22°33'8.00"N	252	3.246 2.598 866 770	6.611 6563	65	150 ± 8 20	48	11.9 ± 0.17 31	1.7	1.63 ± 0.06
	TEN4065 SC15	24° 00'00"N microgranite 10° 1'47.00"W granite 14°28'52.00"W 24°20'23.00"N 22°40'17.00"N	258 282	1097 6.444 4.462 878 0.6 0.425 754 522 482 341	6563 6.595 6.626 6563 6563	8 10	20 172 ± 13 175 ± 16 20 20	82 8	101 11.7 ± 0.33 -35 -	2 --	1.70 ± 0.12 2.06 ± 0.53
	AL10 TAS29	granodiorite gneiss	7° 7'5.15"W 15°32'55.96"W	394 110	1.334 0.866 0.743 0.778	7.255 6.586	63 11	202 ± 14 115 ± 6	15 14	12 ± 0.23 12.2 ± 0.25	1.6 1.8	1.77 ± 0.12 1.70 ± 0.12
			26°37'33.06"N 20°59'34.10"N		675 1047	438 1096	6849 6849		20 20		49 51
	YT7 AG167	monzogranite 7°20'37.34"W charnockite 13°24'2.07"W	384 233	1.862 1.394 0.218 0.195	6.825 6.73	72 74	166 ± 8 137 ± 12	25 4	11.4 ± 0.25 -	1.8 -	1.60 ± 0.19 1.72 ± 0.08
			26°28'59.39"N 20°42'56.76"N		1380 323	1033 289	6849 6849		20 20		49 -	-
	AG169	charnockite	13°24'2.07"W	237	0.201 0.207	6.682	93	118 ± 10	4	-	-	1.54 ± 0.17
	Reguibat West * ρ -	20°42'56.76"N		309	319	6849		20		-	-
	Sample TAS233	Rock-type volcanite	Location 15°32'55.96"W	Elevation 110	ρ s 0.68	ρ i 0.651	ρ d 6.634	P (χ²) % Central age (Ma) ± 1σ U (ppm) MTL (µm) ± se Std dev. 87 126 ± 7 12 12.5 ± 0.18 1.8	Dpar 1.63 ± 0.15
			20°59'34.10"N	(m)	797	763	6849		20		102
	AOS2	syénite neph	14°17'W	400	1.1237 1.258	6.61	2	107 ± 8	23	11.8 ± 0.24	1.8	1.65 ± 0.27
			22°32'N		654	732	6528		21		56
	AOS3	syénite neph	14°17'W	400	1.899 1.772	6.58	63	128 ± 6	33	11.9 ± 0.16	1.6	1.65 ± 0.27

Table S2 :

 S2 AHe results* for the whole Reguibat Shield

		AL10-K SC5A TAS29B	37,9 46,9 42,1		1,28 2,61	2	0,717 0,756 0,767	145483,1 209790,4 238975,6	12,5 20,7 16,0	8,8 5,3 16,9	35,5 83,0 27,9	14,9 22,6 20,1		77 98		112 101	9 10
		AL10-F SC5C TAS29C IG3-C	38,7 56,6 50 43,8		1,23 4,35 2,57 1,72	0,687 0,802 0,758 0,722	129286,7 26663,6 196139,6 332846,2	9,5 6,3 19,6 18,1	15,8 6,0 4,9 18,9	44,8 16,0 10,1 44,7	13,6 7,9 20,8 23,0		28 78 120		115 35 166	9 8 13
		Rock-type AL10-G SC5D TAS29D IG3-E	39,9 59,9 56,9 39,4	Location 1,23 5,69 3,14 Elevation 0,707 0,802 0,748 1,31 0,686	ρ s 1327362,4 ρ i 214046,7 196541,4 191182,1	ρ d 32,4 26,8 10,7 5,0	P (χ²) % Central age (Ma) ± 1σ U (ppm) MTL (µm) ± se Std dev. 26,5 65,3 39,3 280 396 10,6 14,9 29,5 60 75 3,9 13,1 11,7 138 10,0 48,9 7,8 203 295	Dpar 32 15 24
	IG3	rhyolite AL10-H TAS29E IG3-F Reguibat Central 42,6 71,4 36,7 SC9B 59,9 IG3-G 40,6	6° 9'0.43"W 1,58 7,22 0,99 5,4 1,56	(m) 366 0,713 0,84 0,675 0,809 0,741	0.469 0.149 236976,2 57789,0 118582,6 59285,0 91106,9	6.968 18,4 7,2 3,8 6,7 3,7	84 18,2 1,8 10,9 11,6 4,9	393 ± 36 50,1 6,5 47,2 271,0 38,8	23,2 7,6 6,8 11,7 5,1	3	62 146 42 147	-	119 74 216 52 198	-	1.66 ± 0.16 10 6 17 16
	CH1 CH2	26° 6'22.40"N gabbrodiorite 3°35'36.69"W 25°35'45.94"N gabbrodiorite 3°35'36.69"W 25°35'45.94"N Name Rs (µm) Weight(µg) SC9D 41,4 1,92 IG3-I 40,4 1,67 1185C 52,1 3,11 SC9E 45,8 2,35 Reguibat East 1185D 74,5 10,33 Reguibat West TL3-L 41,1 1,58 1185E 33,4 1,02 SC11C 50,3 3,01 Name Rs (µm) Weight(µg) TL3-B 49,4 2,68 Name Rs (µm) Weight(µg) SC11D 68 7,34 TL3-C 41,3 1,57	252 252 FT 0,717 0,721 0,756 0,761 0,849 0,745 0,65 0,782 FT 0,803 FT 0,839 0,778	543 1.098 0.454 172 862 356 3.105 1.516 770 376 4He(ncc/g) U (ppm) 6849 7.159 6849 7.112 6849 282683,0 26,7 187725,0 3,9 678000 45,4 606340,6 52,0 868000 44,4 131554,4 6,3 530000 39,4 18223,7 4,7 4He(ncc/g) U (ppm) 66784,2 8,8 4He(ncc/g) U (ppm) 92903,5 7,3 73141,8 9,2	6 18 Th (ppm) 37,2 5,5 63,3 65,8 51,6 18,8 74 4,0 Th (ppm) 17,0 Th (ppm) 13,5 43,5	20 307 ± 26 20 264 ± 21 20 Sm (ppm) eU (ppm) 274,0 37,9 49,9 5,6 NA 60,6 401,0 71,0 -56,8 29,8 11,1 -57,1 284,0 7,9 Sm (ppm) eU (ppm) 23,8 13,1 Sm (ppm) eU (ppm) 228,0 12,4 27,0 19,8	8 26	-11.5 ± 0.21 101 12 ± 0.2 69 Age (Ma) Age c. (Ma)* 2.1 1.7 62 86 277 384 104 71 93 138 142 99 133 167 86 19 24 Age (Ma) Age c. (Ma)* 42 53 133 Age (Ma) Age c. (Ma)* 62 74 31 40	1.86 ± 0.19 1.99 ± 0.17 31 s.d. 11 s.d. s.d.
	CH3 GH3 DEG6 GH20	gabbrodiorite 3°35'36.69"W 25°35'45.94"N trondhjemite 6° 3'54.77"W 25°29'36.53"N gabbro 2°57'15.60"W 26° 4'50.02"N gabbro 6° 0'2.87"W 1153-A 80,8 11,85 SC11E 53,2 2,98 CH1-A 47,3 2,43 TL3-D 39 1,44 1153D 34,4 1,17 AOS3A 57,7 4,14 SC11F 66,7 5,97 CH1-B 56,4 4,13 TL3-F 41,4 1,92 1153-F 63,2 6,54 AOS3B 48,3 2,56 CH1-C 49,4 2,68 TL3-G 43,5 1,98 1153-H 59 4,69 AOS3C 58,4 5,02 SC12A 41,6 1,65 CH1-D 40,2 1,45 TL3-J 52 3,29 1153-I 47,5 2,56 AOS3E 55 3,82 SC12D 64 6,22 CH1-F 38,8 1,31 TL3-H 47 2,35 1153-J 71,5 8,33 AOS5A 54,4 3,77 SC12F 52,3 2,8 CH1-H 37,9 1,28 SC12G 49,5 2,44 CH1-G 64 6,37 TL3-K 46,6 2,77		252 360 355 350 0,87 0,775 0,789 0,717 0,715 0,781 0,815 0,809 0,717 0,815 0,786 0,802 0,745 0,83 0,803 0,749 0,751 0,797 0,79 0,806 0,827 0,754 0,777 0,87 0,843 0,77 0,717 0,754 0,831 0,746	1.059 0.426 686 276 1.177 0.41 1130 394 2.276 0.701 1065 328 0.471 0.101 46201,6 157369,9 79475,1 86327,5 120399,0 379655,5 47092,6 28513,1 123516,5 100000,8 368565,3 48729,7 95782,6 63086,4 168335,8 108423,6 205297,8 93130,9 57756,0 317447,5 180770,1 127741,1 123871,0 58868,8 17656,2 151382,1 392039,3 222394,6 88950,2 21915,9	7.064 6849 7.016 6849 6.111 6849 5.996 3,8 11,4 7,2 6,3 10,4 29,6 8,2 2,7 7,1 7,6 29,6 13,1 6,4 11,2 27,7 9,6 10,1 5,4 5,5 50,1 19,1 11,0 8,0 5,6 9,4 24,6 26,1 22,1 6,2 3,6	86 6 46 73 11,9 25,5 6,9 20,9 31,9 40,2 2,9 3,2 25,1 20,3 47,8 11,1 21,9 22,6 28,6 13,1 12,5 17,1 16,8 31,7 9,4 9,6 27,5 17,0 7,6 25,6 23,4 12,8 8,5 8,2	315 ± 24 20 359 ± 27 20 355 ± 25 20 497 ± 61 7,0 103,0 5,3 33,8 20,3 403,0 266,0 1,4 35,2 9,5 167,0 5,3 34,3 12,5 318,0 232,0 5,6 25,4 13,3 391,0 241,0 3,4 36,9 12,9 125,0 360,0 6,0 141,0 5,1 19,6	6,7 18,4 9,0 11,6 18,3 42,5 11,0 3,5 13,4 12,6 42,4 15,8 12,0 16,7 37,1 14,6 13,1 9,7 9,6 60,9 23,3 13,3 14,9 9,7 12,3 33,7 31,8 26,3 8,2 5,7	7 7 12 2	57 71 74 62 55 35 68 77 66 26 67 31 61 130 80 50 64 80 69 50 55 102 48 90 32	11.5 ± 0.29 64 11.5 ± 0.19 100 11.2 ± 0.41 27 -107 66 92 93 87 77 95 43 84 81 92 32 89 38 47 82 101 63 54 78 89 58 14 71 63 43	2.3 1.9 2.1 -	1.95 ± 0.18 1.76 ± 0.16 1.97 ± 0.11 1.75 ± 0.13 7 5 8 7 6 7 3 6 4 14 3 4 8 5 1 11 5 9
	TL3	gabbro 3163-A AOS5D CH1-J 3163-E AOS5F SC15A CH1-K GH20-A 3163-I SC15B GH20-C 3163G AOS2A SC15F CH3-C GH20-D AOS2B SC15G CH3-F GH20-F	25°32'51.89"N 3°10'37.45"W 27°21'31.99"N 54,1 3,6 48,7 2,8 50,6 3,96 66 7,11 48,2 2,27 59,7 4,73 40,7 1,74 36,4 1,14 65,6 6,26 56,5 3,7 37,4 1,28 96,1 17,27 58,6 4,48 48,3 2,27 50,5 3,04 37,4 1,28 62,7 6,65 56,5 3,99 35,5 0,96 41,1 1,58		381 0,809 0,736 0,761 0,827 0,754 0,833 0,723 0,702 0,847 0,782 0,703 0,875 0,783 0,747 0,789 0,703 0,812 0,828 0,717 0,745	206 0.818 0.376 44 447 207 717183,1 59629,6 141712,3 288616,5 175595,4 141643,9 190623,3 58542,3 470679,8 16790,6 74174,8 549045,6 252824,1 50901,3 119938,2 54325,7 219640,8 234089,4 191786,5 34723,6	3012 6.052 3012 37,7 17,5 5,0 16,9 29,5 10,6 19,0 5,8 17,8 3,6 12,9 25,0 31,0 5,6 4,2 5,9 23,1 25,4 13,4 4,1	66 1,9 16,4 6,5 1,4 24,2 16,3 10,3 5,2 25,6 8,7 6,9 22,0 12,2 19,5 5,9 5,1 16,3 23,6 11,3 5,3	10 237 ± 21 20 27,2 263,0 4,5 17,6 195,0 382,0 14,9 129,6 24,6 126,0 26,5 NA 400,0 90,0 3,7 31,4 105,0 340,0 4,2 30,5	38,3 23,5 6,6 17,4 36,9 17,5 21,6 8,1 24,1 6,7 14,7 30,3 37,2 11,0 5,7 7,3 27,8 33,8 16,1 5,7	8	155 178 137 67 73 60 162 21 42 150 39 175 61 57 99 51	--	29 191 52 80 85 166 27 59 191 72 52 87 172 81 69 68	-	2.12 ± 0.19 2 19 4 8 6 18 6 11
		AL10-A AOS2C CH3-A GH20-H AL10-E AOS2D T233-B CH3-G GH20-G AL10-C T233-H AL10-L AL10-J AL10-I AL10-B TAS29A GH3-F TCH7D GH3-E TCH7C T233-F GH3-C TCH7A TCH7B T233-D T233-G GH3A GH3B * Rs (sphere equivalent radius46 47 54,7 35,1 39,3 43,8 52,5 59,2 39,2 50,5 55,5 44,1 37,2 45,5 39 66,7 99 64,6 57,9 63,6 49,7 71,5 49,4 68,7 49,3 58,8 66,1 91,1	2,4 2,35 4,25 1,22 1,18 1,96 3,31 6,11 1,52 3,53 4,01 1,57 1,22 2,02 1,39 5,97 19,03 6,31 4,06 6,25 2,85 8,99 2,8 8,03 1,4 4,58 7,49 21,74	0,755 0,777 0,79 0,663 0,701 0,756 0,833 0,793 0,711 0,765 0,803 0,679 0,724 0,76 0,726 0,815 0,883 0,838 0,784 0,823 0,786 0,842 0,802 0,833 0,678 0,822 0,823 0,876	405681,5 47197,6 93992,9 37173,2 675195,0 77464,5 87654,0 71843,0 54027,8 229447,2 163091,7 1341456,8 231868,3 395904,9 557702,2 168827,7 21444,4 106663,8 230520,3 318644,3 127884,5 56806,1 194360,7 137470,0 263063,3 55323,1 292746,2 172995,7	22,5 14,8 5,7 9,5 76,1 20,3 9,1 3,7 11,1 11,1 35,9 34,3 7,9 22,4 20,6 14,1 1,7 13,5 6,5 43,4 12,9 4,5 59,4 19,1 27,0 6,5 8,1 4,7	20,6 11,6 5,5 6,2 26,7 30,6 2,6 5,0 7,0 11,9 12,9 31,1 10,0 14,9 11,6 5,4 0,4 8,9 3,8 11,1 3,2 3,5 34,9 23,5 7,2 1,9 5,6 4,6	31,8 152,0 3,2 37,8 31,3 179,0 12,9 2,7 34,3 29,3 9,4 59,4 37,4 41,0 37,5 12,1 2,2 267,0 10,8 229,0 12,5 8,9 179,0 339,0 30,6 14,3 12,7 6,4	27,7 18,8 7,0 11,2 82,8 29,1 9,8 4,9 13,1 14,2 39,0 42,2 10,5 26,3 23,7 15,4 1,8 17,8 7,5 47,9 13,7 5,4 69,2 27,5 29,0 7,0 9,6 5,9		121 111 27 67 74 122 34 134 35 263 182 124 195 90 98 256 77 88 75 65 253 243		27 41 161 96 29 89 48 43 175 388 111 269 59 164 67 98 252 29 50 111 79	2 11 2 12 8 9 5 26 5 8 2 4 25 22

Table S3 :

 S3 Results from forward modeling of central RS samples

	Equivalent sphere radius = 55 µm
	eU (ppm)	AHe age (Ma)	HT1	HT2	HT3	HT4	HT5
	5	45	37	42	42	45	79
	10	55	46	58	55	54	85
	15	78	54	81	81	61	88
	20	125	63	106	112	67	90
	30	165	82	137	151	75	92
	40	180	99	152	171	81	94
	60	190	120	167	189	90	95

HT: Thermal History eU: efficient Uranium

Acknowledgements

We thank Eric Douville for accessing the ICP-MS (LSCE, Gif-sur-Yvette) and Louise Bordier for the U-Th measurements. This work has been supported by the Académie Hassan II des Sciences, Casablanca, Morocco. We acknowledged P.F. Green and an anonymous reviewer for the remarks and comments that greatly helped clarifying and precising numerous points in the present manuscript.