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, The geology of the Guemassa Massif is similar to the Central Jebilet domain (Figure 1B)
, the Jebilet area was a basin filled with syn-to post-rift sediments (the Sarhlef and Teksmin formations, respectively) intruded by shallow sills and dykes and deeper plutonic laccoliths originating from a tholeitic bimodal magmatism (e.g., the mafic/ultramafic Kettara and Sarhlef intrusions) and from a calc-alkaline magmatic suite (e.g., the Oulad-Ouaslam granodiorite) respectively; ii) from 325 to around 310 Ma, a first Hercynian event (D1) is marked by the emplacement of shallow thin skinned nappes with syn-sedimentary breccias. The internal strain is very low and no regional foliation/cleavage (S1) is reported; iii) from ca. 310 Ma to 280 Ma, the main Hercynian deformation (D2), which is polyphased and characterized by a first regional metamorphism (M2a), locally reaches the amphibolite facies (Grt-St) and a second HT/BP "contact" metamorphism in the syn-to post tectonic hornfels facies (M2b, biot + Crd + And) is associated with the leucogranite emplacement around 295 Ma. The successive foliations (S2a and S2b), sub-vertical and oriented N0/30, marked a homoaxial progressive and continual strain regime from a coaxial to a non-coaxial transpression with a broad horizontal NW-SE-trending shortening axis. Last, the D2 increments correspond to a right-lateral transpression accommodated and located along the vertical and conjugate ductile shear zones as the sinistral MSZ (Figure 1B). Therefore, the tectonic scenario proposed by Hibti, Both Massifs host the major MSD of the Occidental Meseta. Thus, recent advances in the tectono-metamorphic and magmatic history of the Jebilet [26,28] may help better constrain the Guemassa Massif evolution. Based on petro-structural data, new absolute dating and thermal investigations, these authors improve the time constraints and the succession of the deformational events as follows: i) from 370 to 325 Ma (D0 of Delchini, 1993.
, The lithologies encountered are pelites alternating with sandy-to pure limestones intruded by felsic and basic sills and dykes (Figure 2). Major volcanic rock bodies correspond to rhyolitic domes and plugs. Many outcrops of the Imarine Massif present soft-sediment deformation as slumps and convolutes (Figure 3A,B), suggesting slope instabilities within syn-rift sediments. These soft sediment structures are cross-cut by a sub-vertical foliation (S1) which is often oblique with respect to the axial plane of isoclinal folds (Figure 3B). This suggests that most isoclinal and disharmonic folds are slumps, and therefore, that they pre-date the development of the planar axial foliation. This S1 foliation is well-developed though the N'Fis block, with a sub-vertical dip and a NW-SE orientation (Figure 2), Surface Structural Data The surface outcrops of the N'Fis block and Souktana Massif have been mapped and studied in terms of the strain analysis and micro-tectonics (Figures, vol.2
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