Figure
1.
Location of the study area with wells and correlation lines on a simplified geologic map of North-Central Tunisia.
| Citation: | Imen Marco, Ferid Dhahri, Taoufik Haji, Noureddine Boukadi. Aptian-Albian Transition in Central Tunisia: Tectonosedimentary and Paleogeographic Records. Journal of Earth Science, 2014, 25(5): 787-798. doi: 10.1007/s12583-014-0478-7
|
The Tunisian Atlas corresponds during Cretaceous times to a basin characterized by dominant N to NE-trending extensional tectonics regime subsequent to the break-up of Gondwana and plates convergence. During the Aptian–Albian times halokinesis movements and magmatism occurred in concurrence with the African rifting (Guiraud et al., 2005) and leaded to the establishment of paleoreliefs as much as tilted blocks and half grabens in central Tunisia (Gharbi et al., 2013; Jaillard et al., 2013; Rigane et al., 2010; Zouari et al., 1999; Boukadi and Bédir, 1996; Boukadi et al., 1992; Martinez et al., 1991; Burollet and Ellouz, 1986). The Aptian–Albian magmatic events are attributed to Cretaceous mantle plume activity highlighted also in the eastern Mediterranean (Segev et al., 2005), in Central Africa (Guiraud et al., 1992; Maurin and Guiraud, 1990) and correlated with these highlighted in the Tunisian eastern margin (Laridhi-Ouazaa and Bédir, 2004).
In this paper we use data from petroleum wells of Central Tunisian atlas, to illustrate the Aptian–Albian tectonosedimentary and paleogeographic records with emphasis to the general evolution of the Atlassic chain of Tunisia. The study area covers large part of central Tunisia and match with the northern part of the central Atlassic domain (Fig. 1). The Zaghouan thrust, the Mrhila-Cherichira fault and the N-S axis constitutes three main paleogeographic faults that underlain this area and was controlled the structure and the deposition distribution since Mesozoic times. Despite the Triassic evaporates, the earliest series are Jurassic–Lower Cretaceous in age. Alongside the study area, outcropping series are from Jurassic to recent (Fig. 1). Their outcrop is linked to the hanging walls of paleogeographic faults of the Zaghouan thrust and the N-S axis. The Triassic evaporites occur mainly along thinned and weakened cover structures as much as Koudiat Halfa, Koudiat Hamra, the N-S axis and Cherichira fault.
Along the central atlas of Tunisia, the Aptian–Albian period shows remarkable tectono-sedimentary records and deserves detailed investigations. This work based on lithostratigraphic correlation of the Aptian–Albian series in central Tunisia attempt to offer new precisions on the Aptian–Albian transition with emphasis of tectonic and paleogeographic controls.
In Central Tunisia a shallow marine environment zone was established during the Lower Aptian (Ben Ferjani et al., 1990). This zone acknowledged as the "Central Tunisian Platform" extend to the south until the Gafsa Basin with a broad shallowmarine area and it is characterized to the north by an emerged land subsequent to the Aptian regression called the Kairouan Island southern Kairouan (Marie et al., 1982; Burollet, 1956). This area is acknowledged as a hemipelagic transition zone between the shallow marine domain and the Tunisian Trough northward (Fig. 2). During the Upper Aptian this area is characterized by shallow marine environment and by the establishment of a carbonate platform facies (Lehmann et al., 2009). An uppermost Aptian generalized marine regression enlarges emerged area leading to Aptian–Albian series thickness reduction in central and southern Tunisia (Marie et al., 1982; Burollet et al., 1983). Reefal limestones occur along subemerged uplifted basins and karstification can take place in emerged carbonated surfaces. These conditions are favorable for formation of potential Aptian reservoirs rock in central Tunisia and for mineralization as much as the Pb-Zn deposits of Jebel Trozza which was the basis for old mining operations.
During the Albian–Cenomanian times, the North-Central Tunisia constitutes an open marine environment dotted with Triassic dome heights (Lehmann et al., 2009). An Upper Albian transgression (Bismuth, 1973) leads to clay and carbonates deposition which came to overlain the Aptian carbonated Serj Formation. Some local anoxic basin are established and seems to be favorable for source rock formation in correlation with the Aptian Oceanic Anoxic Event well known at Tethyan scale and in central Tunisia (Lehmann et al., 2009; Heldt et al., 2008).
The Aptian deposition in Central Tunisia is mainly characterized by carbonate and detritic facies (Figs. 2 and 3) which evolves along paleohighs to reef carbonate facies of the Serj Formation then to open marine facies to the north (claystones and marlstones). This deposition is especially thick in north Central Tunisia with a Lower Aptian hemipelagic facies subsequent to the sea level rise and an Upper Aptian shallow marine environment characterized by carbonate platform facies (Lehmann et al., 2009).
The Serj Formation deposited in widespread carbonate platform at central Tunisia scale, outcrops in many localities. It shows considerable variations in thickness to reach 450–600 m around subsident areas and became thin along the N-S axis (W8 and W9) and missing around the Kairouan Island. It comprises three units: limestones (base unit), an alternation of marl and limestones (middle unit) and limestones, dolomite and some clay (top unit).
The Early Albian deposition took place in marine domain to the north and in the Gafsa Basin but is absent along emerged areas of Central Tunisia and Saharan platform. During the Albian–Cenomanian times, sedimentation is diverse with three partial equivalent formations reaching the lowermost Turonian age: the Zebbag Formation in the southern and South-Central Tunisia with limestones, marls, dolomites and gypsum deposits, and the Fahdene and Bahloul formations to the north with marls and limestones deposits (Fig. 4).
The complete Albian series in Central Tunisia (Fahdene Formation) is crossed by two wells northward Jebel Mrhila (Fig. 1) and it accomplish 1 600 m thick and it is comprised of alternating limestones and marls evolving to argillaceous facies upward. This Formation was defined firstly in the Oued Bahloul anticline core by Burollet (1956) within an Albian–Cenomanian age, then described by M'Rabet in 1981 within a 1 400 m thick Albian series in Koudiat el Baïda (Jebel Mrhila), and revised later by Zghal (1994) who divided this Formation into four units: 1) the Fahdene lower clays Lower Albian in age, 2) the Allam limestones Middle Albian in age, 3) the Fahdene middle clays Upper Albian in age and 4) the Mouelha limestones and the lower part of the uppermost clays, Upper Albian in age.
According to Zghal et al. (1997), the complete Albian sequence can be subdivided to five terms: 1) an alternations of Lower Albian marls and argillaceous limestones at the base, 2) Lower to Middle Albian carbonated sequence (marls then limestones), 3) Middle Albian alternation of marls and sandstones, 4) alternation of marls (unit F0, Upper Albian), limestones (unit F1, Upper Albian) and argillaceous limestones (unit F2A, Uppermost Albian-Lowermost Vraconian), 5) the term 5, Vraconian in age is comprised of a clayey sequence within a bioclastic limestone layers at the base. The uppermost Cenomanian is mainly comprised of marly limestones (unit F2B).
The study area makes part of central Tunisia which is an intensively fractured and folded Atlassic domain with SE-vergent anticlines alternating with large synclinal basins (Figs. 5 and 6). This domain is also characterized by some NW-SE and E-W grabens corresponding to subsident zones bordered by active ancient faults occurred since the Lower Cretaceous. These grabens are probably structured since the Aptian–Albian times and evolved during the Neogene and Quaternary tectonic events.
The study area is particularly underlined by the ENE-WSW Mrhila-Cherichira strike-slip fault system (Fig. 5) comprised of a successions of E-W dextral strike slips relayed by N60 restraining bends which contributes to the east-verging thrusts and to the Triassic extrusion along the structures of Chaambi, Koudiat Halfa, and Cherichira (Haji et al., 2013; Boukadi, 1994). However this fault has significant impact on the distribution of sedimentation and subsidence with some progressive sedimentary gaps (Haji et al., 2013; Boukadi, 1994).
Foussana and Rohia-Sbiba grabens are two main NW-SE oriented grabens clipped by the Mrhila-Cherichira fault where the junction matches respectively with the Triassic evaporites extrusion of Jebel Chaambi and Koudiat Halfa. The Rohia-Sbiba graben end at the level of the Mrhila fault to the south but the Foussana-Kasserine graben extend southern this fault testifying the importance of the Kasserine regional fault (Figs. 5 and 6).
The Tethyan realm is characterized during Early Cretaceous by extensional tectonics related to the NW-SE Tethys opening started since the Late Permian and leading to rifts, horsts, grabens and tilted blocks (Dhahri and Boukadi, 2010; Brunet and Cloetingh, 2003; Piqué et al., 1998; Soyer and Tricart, 1987; Dercourt et al., 1986). Since the Aptian main tectonic and eustatic events occurs in both Tethys margins. Olivet et al. (1984) highlighted a southeastern drift of the Iberian Peninsula during the Uppermost Aptian–Upper Albien. In the northern Tethyan margin Graziano (2000) describe a syn-sedimentary tensile tectonics, at the end of the Early Aptian, that he link to the onset of the Austrian orogenic phase on the distant Adria plate margin and responsible to the establishment of the central and eastern Alps.
In Tunisia, except scarce local compressional structures highlighted in Central Tunisia (Bouaziz et al., 2002; Rabhi and Ben Ayed, 1990), the Aptian–Albian tectonics is mainly extensional and engenders an important hiatus (Rigane et al., 2010; Bouaziz et al., 2002; Soyer and Tricart, 1987). Martinez et al. (1991) point out an NE-SW extension of the Tunisian margin during the Aptian resulting from the dextral slip of the Gibraltar-Messine transform fault and engendering strike-slips and normal faults respectively along NE-SW and NS accidents. During the Aptian times Triassic salts started to grow up in Tunisia (Snoke et al., 1988) and the most important halokinesisevent seems to be experienced during this period and played an important role in the tectono-sedimentary evolution of Tunisia (Boukadi et al., 1992). Horst and grabens created are disturbed by Triassic ascension along extensional zones which uplift some domes and tilted blocks. This configuration stimulates differential subsidence until the Cenomanian times in Central Tunisia (Soyer and Tricart, 1987)
Fourteen petroleum exploration wells drilled in the study area were studied (Fig. 1). Stratigraphic columns were analyzed and compared to correlate and point out the evolution of the Aptian-Albian series along the studied area based on three correlation lines (Figs. 7, 8 and 9). We focused especially to the Aptian-Albian transition; hence post-Cenomanian series are not drawn in some stratigraphic columns.
Figure 7 illustrates the first correlation line drawn for the eastern part of the study area. This correlation comprises four lithostratigraphic columns respectively of W2, W1, W4 and W7 wells. W2 is drilled near the northeastern edge of the Rohia graben, W1 and W4 are drilled in the northern block of the Sbiba graben and the W7 is drilled southern the Mrhila-Cherichira fault, westward the NS axis (Fig. 5).
These wells are going throw the most of the Cretaceous series. They show considerable thick variations especially for the Upper Cretaceous series as demonstrated by Haji et al. (2013), Zouaghi et al. (2011) and Zghal et al. (1997). We note the lack of the Uppermost Aptian and the Lowermost Albian deposition (Fig. 7). The Serj Formation make about 622 m in the Massanerh structure (W2), 433 m in the Oued Bahloul (W1), 736 in Argoub el Gara (W4) and is totally missing in the Zaouia and the NS axis area (Fig. 6, section Ⅰ). These thickness variations are also shown in the section Ⅰ of Fig. 6 where the paleogeographic faults of the N-S axis, Trozza, Bahloul and Ballouta impacted highly the distribution of Cretaceous deposition.
The Fahdene Formation Albian–Cenomanian deposition makes about 850 m in Massanerh structure, 416 m in the Oued Bahloul and is totally missing in Argoub el Gara and the Zaouia area. In Argoub el Gara the Turonian series overlays unconformably the Serj Formation. Comparing to the domain situated to the south of the Mrhila-Cherichira fault, the Massanerh, Oued Bahloul and Argoub el Gara area seem to be subsident during the Aptian with marls dominated deposition. These conditions persist during the Albian times for the Massanerh and Oued Bahloul and not for the Argoub el Gara area. This can be explaining by the fact that this later is located in the uplifted side of a tilted block made by the normal slip of faults during the Upper Cretaceous.
The missed stratigraphic units are possibly eroded subsequently to the combination of two factors: 1) an Aptian tectonic controversial event (Bouaziz et al., 2002; Graziano, 2000; Martinez et al., 1991; Rabhi and Ben Ayed, 1990; Snoke et al., 1988; Soyer and Tricart, 1987) engendering an important hiatus and 2) an uppermost Aptian regression responsible ofemersion an erosion of considerable area especially in the Central Tunisian Platform.
Figure 8 illustrates the second correlation line which is mainly oriented NS. It comprises five wells, respectively from south to north, W14, W13, W12, W11 and W5. The first three wells are drilled northern the Mrhila-Cherichira fault and the others are southward (Fig. 5).
Unluckily the Serj Formation is not fine correlated because the final depth of at least three wells doesn't across overall this formation. This correlation line shows the lack of the Upper Aptian and the Lower–Middle Albian series. The Albian deposition ranges from 300 to 500 m thick and shows a progression from shallow marine platform facies to the south, to an open marine facies to the north (Fig. 8) with rich coquina level especially around Tamesmida structure (W12 and W11 wells). The Fahdene Formation overlay unconformably the Serj Formation and outcrops in Khechem el Kelb (W13) and Assilet (W5) areas (Fig. 5) where it is partially eroded and respectively about 731 and 625 m thick (Fig. 8). But it is remarkably thick when it doesn't outcrops preserving its total deposition around Khechem el Kelb (W14) and Tamesmida (W12 and W11) areas exceeding 1 000 m thick. In fact, Tamesmida area, located northward the Mrhila-Cherichira fault, constitutes an AlbianCenomanian subsiding basin subsequently to the normal slip of the northern block of this main paleogeographic fault (Haji et al., 2013) (Fig. 5). And Khechem el Kelb constitutes an NE-SW anticline with a southeastern subsiding flank affected by NE-SW normal fault system (Zouaghi et al., 2011).
Figure 9 illustrates the third correlation line which is mainly oriented NE-SW. It comprises seven wells, respectively from southwest to northeast, W12, W11, W10, W6, W3, W2 and W1 (Fig. 5). Except W10 which is drilled close to the Mrhila fault, the other wells are drilled northern the Mrhila-Cherichira fault.
The thicker Aptian series seems to be deposited around Tamesmida and Massannerh areas where the Serj Formation exceeds 574 m thick. In these localities, the Lower Aptian deposition is mainly marls and clays dominated. Middle and Upper Aptian deposition is for the most wells from carbonates platform facies (limestones and dolomites). The Fahdene Formation overlays unconformably the Aptian deposition and shows, from southwest to northeast, significant thick variations (Figs. 6 and 9). Two subsiding basins separated by relative uplifted block can be defined respectively in TamesmidaDerneya (W12-W11) area to the southwest and in Ksar Tlili-Massanerh (W3-W2) to the northeast. This structuring is due to the normal slip of the NW-SE oriented fault. In fact, the subsidence of Tamesmida-Derneya block is due to both normal slips of NW-SE faults and Mrhila-Cherichira one's, this why it seems to be the most subsiding area.
Compare to the Serj Formation defined in Jebel Serj (Tlatli, 1980; Burollet, 1956), the Aptian series crossed by the studied wells records some comments on lithology and thickness. In fact, to the north, the Aptian deposition seems to be dominated by claystones and marlstones testifying open marine facies and fluctuate progressively to the south, to carbonate and detritic facies of shallow marine platform. This progressive facies variation is notable around the Mrhila-Cherichira fault which can underline the transition zone between the open marine environment to the north and the platform domain to the south.
The Aptian series are characterized, in Tunisia, by several variations in subsidence rates and records discrete unconformity between Albian and Aptian in central and southern Tunisia (Ouahchi et al., 1998; Zghal et al., 1997; Ben Ferjani et al., 1990). The Upper Aptian regressions were sustained until the beginning of Albian with a low sea level stand. In Central Tunisia discordances occurs specially around and upward uplifted blocks and emerged land subsequent to the uppermost Aptian marine regression (Marie et al., 1982). Along these areas, reef and dolomitic Aptian facies are overlaid by the Albian–Cenomanian open marine facies with rich organic matter rocks. Subsequently Aptian rocks are usually associated to mineralization and Hydrocarbure reservoirs as much as the three producing oil fields of Douleb, Semmama and Tamesmida in Central Tunisia. In addition, the Aptian series overlay in several places the breccias cap rock of the some diapirs in North-Central Tunisia (Snoke et al., 1988).
In the studied area, the Albian deposition is not complete as documented in northern Tunisia. This deposition which is mainly clayey northward and carbonated southward makes part of the Fahdene Formation and overlay unconformably the Aptian deposition by Lower to Upper Albian deposition (Figs. 7, 8 and 9).
The Aptian–Albian transition is underlined by an evident hiatus starting from Middle to Upper Aptian and reaching the Upper Albian. This hiatus seems to be regional and it is subsequent to the total absence of the Lower and Middle Albian series in the platform domain of the Central Tunisia. This event is documented by major emersion surface in outcropping series and so highlighted in petroleum exploration wells. It can be related to both Aptian tectonic activity known at Tunisian (Bouaziz et al., 2002; El Euchi et al., 2002; Boukadi et al., 1992; Rabhi and Ben Ayed, 1990; Snoke et al., 1988; Soyer and Tricart, 1987) and Tethyan scale (Graziano, 2000) and eustatic events (Burollet et al., 1983). At the study area scale, the Aptian–Albian hiatus is more significant in W14 and W13 (Middle Aptian–Upper Albian) due to their location in a platform domain southward the Mrhila-Cherichira fault (Fig. 5). Northern this fault (W12, W11 and W5 wells) the Aptian– Albian hiatus still evident but less spread.
Concerning the structural configuration, the study area is affected by the Mrhila-Cherichira fault which occur normal slip during the Upper Cretaceous leading the subsidence of its northern block (Haji et al., 2013). This zone is also affected by NW-SE normal faults which makes a succession of NW-SE oriented grabens, horsts and tilted blocks especially northern the Mrhila-Cherichira fault (Zouaghi et al., 2011; Zghal et al., 1997). This configuration allows differential deposition with local subsiding depocenters (e.g., Massanerh and Oued Bahloul area) and relative uplifted blocks (Argoub el Gara area). Finally, it seems that the Aptian–Albian deposition in Central Tunisia is underlined by a regional hiatus and mostly controlled in thickness and facies by structural configuration, halokinesis and large variations in subsidence. It shows a lateral transition, from platform facies to south to, open marine facies to the north. The basin deepening northward is controlled by the normal slip of the paleogeographic fault of Mrhila-Cherchira and lead to the deposition of Fahdene source rock facies.
ACKNOWLEDGMENTS: We thank the anonymous reviewers and the Editorial Committee of Journal of Earth Science for their constructive criticisms and useful comments.| Ben Ferjani, A., Burollet, P. F., Mejri, F., 1990. Petroleum Geology of Tunisia. ETAP, Tunis. 194 |
| Bismuth, H., 1973. Réflexions Stratigraphiques sur l'Albo-Aptien dans la Région des Djebels Douleb et Semmama et son Environnement (Tunisie Centre-Nord). In: Solignac, M., ed., Livre Jubilaire. Annales des Mines et de la Géologie (Tunisia), 26: 179–212. |
| Bouaziz, S., Barrier, E., Soussi, M., et al., 2002. Tectonic Eevolution of the Northern African Margin in Tunisia from Paleostress Data and Sedimentary Record. Tectonophysics, 357: 227–253 doi: 10.1016/S0040-1951(02)00370-0 |
| Boukadi, N., 1994. Structuration de l'Atlas de Tunisie: Signification et Cinématique des Noeuds et Zones d'Interférences Structurales au Contact de Grands Couloirs Tectoniques: [Dissertation]. Univ. Tunis Ⅱ, Fac. Sc. Tunis, Tunis. 249 http://www.researchgate.net/publication/284882799_Structuration_de_l'Atlas_de_Tunisie_Signification_des_noeuds_et_des_zones_d'interferences_structurales_au_contact_des_grands_couloirs_tectoniques |
| Boukadi, N., Bédir, M., 1996. Halokinesis in Tunisia: Tectonic Context and Chronology of Events. Comptes Rendus de l'Académie des Sciences Paris, 322(Série Ⅱa): 587–594 http://www.researchgate.net/publication/279547956_Halokinesis_in_Tunisia_Tectonic_context_and_chronology_of_events |
| Boukadi, N., Zargouni, F., Ruhland, M., 1992. Kinematic and Tectonic Evolution of the Bayonet-Fault System in the Tunisian Atlas: Transtension, Halokinesis and Transpression. Comptes Rendus de l'Académie des Sciences Paris, 315(Série Ⅱ): 1760–1775 http://www.researchgate.net/publication/281468089_Kinematic_and_tectonic_evolution_of_the_bayonet-fault_system_in_the_Tunisian_Atlas_transtension_halokinesis_and_transpression |
| Brunet, M. F., Cloetingh, S., 2003. Integrated Peri-Tethyan Basins Studies (Peri-Tethys Programme). Sedimentary Geology, 156: 1–10 doi: 10.1016/S0037-0738(02)00279-8 |
| Burollet, P. F., 1956. Contribution à l'Etude Stratigraphique de la Tunisie Centrale. Ann. Mines, Géol. Tunis, 18: 350 http://www.researchgate.net/publication/303602546_Contribution_a_l'etude_stratigraphique_de_la_Tunisie_centrale |
| Burollet, P. F., Memmi, L., M'Rabet, A., 1983. Le Crétacé Inférieur de Tunisie: Aperçu Stratigraphique et Sédimentologique. Zitteliana, 20: 255–264 |
| Burollet, P. F., Ellouz, N., 1986. L'évolution des Bassins Sédimentaires de la Tunisie Centrale et Orientale. Bulletin du Centre de Recherche, Pau-SNPA 10: 49–68 |
| Dercourt, J., Zonenshain, L. P., Ricou, L. P., et al., 1986. Geological Evolution of the Tethys Belt from the Atlantic to the Pamirs since the Lias. Tectonophysics, 123(1–4): 241–315 http://www.mendeley.com/research/geological-evolution-tethys-belt-atlantic-pamirs-since-lias/ |
| Dhahri, F., Boukadi, N., 2010. The Eevolution of Pre-Existing Structures during the Tectonic Inversion Process of the Atlas Chain of Tunisia. Journal of African Earth Sciences, 56: 139–149 doi: 10.1016/j.jafrearsci.2009.07.002 |
| El Euchi, H., Ouahchi, A., M'Rabet, A., 2002. The Tunisian Aptian-Albian Carbonate Platform: Dynamics and Petroleum Systems. Proceeding of the 8th Tunisian Petroleum Exploration and Production Conference, Tunis. 47 |
| Gaaya, A., Ghenima, R., 1998. Sources Rocks and Related Petroleum Systems in Tunisia. Revue Tunisienne de l'énergie, 98: 33–45 |
| Gharbi, M., Masrouhi, A., Espurt, N., et al., 2013. New Tectono-Sedimentary Evidences for Aptian to Santonian Extension of the Cretaceous Rifting in the Northern Chotts Range (Southern Tunisia). Journal of African Earth Sciences, 79: 58–73 doi: 10.1016/j.jafrearsci.2012.09.017 |
| Graziano, R., 2000. The Aptian-Albian of the Apulia Carbonate Platform (Gargano Promontory, Southern Italy): Evidence of Palaeoceanographic and Tectonic Controls on the Stratigraphic Architecture of the Platform Margin. Cretaceous Research, 21: 107–126 doi: 10.1006/cres.2000.0201 |
| Guiraud, R., Bosworth, W., Thierry, J., et al., 2005. Phanerozoic Geological Evolution of Northern and Central Africa: An Overview. Journal of African Earth Sciences, 43: 83–143 doi: 10.1016/j.jafrearsci.2005.07.017 |
| Guiraud, R., Binks, R. M., Fairhead, J. D., et al., 1992. Chronology and Geodynamic Setting of Cretaceous-Cenozoic Rifting in West and Central Africa. Tectonophysics, 213: 227–234 doi: 10.1016/0040-1951(92)90260-D |
| Haji, T., Dhahri, F., Marco, I., et al., 2013. New Insights on the Tectonic and Paleogeographic Evolution of the Central Atlasic Domain of Tunisia. Arab J Geosci, 7(4): 1605–1616 http://www.researchgate.net/profile/Taoufik_Haji2/publication/257785762_New_insights_on_the_tectonic_and_paleogeographic_evolution_of_the_central_Atlasic_domain_of_Tunisia/links/0deec537b325e0bd0e000000.pdf |
| Heldt, M., Bachmann, M., Lehmann, J., 2008. Microfacies, Biostratigraphy, and Geochemistry of the Hemipelagic Barremian-Aptian in North-Central Tunisia: Influence of the OAE 1a on the Southern Tethys Margin. Palaeogeography, Palaeoclimatology, Palaeoecology, 261: 246–260 doi: 10.1016/j.palaeo.2008.01.013 |
| Jaillard, E., Dumont, T., Ouali, J., et al., 2013. The Albian Tectonic "Crisis" in Central Tunisia: Nature and Chronology of the Deformations. Journal of African Earth Sciences, 85: 75–86 doi: 10.1016/j.jafrearsci.2013.04.008 |
| Laridhi-Ouazaa, N., Bédir, M., 2004. Les Migrations Tectono-Magmatiques du Trias au Miocène sur la Marge Orientale de la Tunisie. Africa Geosciences Review, Ⅱ(3): 179–196 |
| Lehmann, J., Heldt, M., Bachmann, M., et al., 2009. Aptian (Lower Cretaceous) Biostratigraphy and Cephalopods from North Central Tunisia. Cretaceous Research, 30: 895–910 doi: 10.1016/j.cretres.2009.02.002 |
| Marie, J., Trouve, P. H., Desforges, G., et al., 1982. Nouveaux Eléments de Paléogéographie du Crétacé de Tunisie. Cretaceous Research, 3(1–2): 167–170 |
| Martinez, C., Chikhaoui, M., Truillet, R., et al., 1991. The Geodynamical Framework of the Albo-Aptian Distension in Northern and Central Tunisia: Eocretaceous Structurations of the Tunisian Atlas. Eclogae Geologicae Helvetiae, 84: 61–82 |
| Maurin, J. C., Guiraud, R., 1990. Relationships between Tectonics and Sedimentation in the Barremo-Aptian Intracontinental Basins of Northern Cameroon. In: Kogbe, C. A., Lang, J. eds., African Continental Phanerozoic Sediments. Journal of African Earth Sciences, 10: 331–340 |
| Olivet, J. L., Bonnin, J., Beuzart, P., et al., 1984. Cinématique de l'Atlantique Nord et Central. CNEXO, ed., Rapport Sci. Techn., 54: 108 |
| Ouahchi, A., M'Rabet, A., Lazreg, J., et al., 1998. Early Structuring, Paleo-Emersion and Porosity Development: A Key for Exploration of the Aptian Serdj Carbonate Reservoir in Tunisia. Proceedings of the 6th Tunisian Petroleum Exploration and Production Conference. ETAP's Memoir Series 12. ETAP, Tunis. 267–284 http://www.researchgate.net/publication/313650401_Early_structuring_paleo-emersion_and_porosity_development_a_key_for_exploration_of_the_Aptian_carbonate_reservoirs_in_Tunisia |
| Piqué, A., Brahim, L. A., Ouali, R. A., et al., 1998. Structural Evolution of the Magreb Atlasic Domains during Mesozoic and Cenozoic Times: The Role of Inherited Structures during the Deformation of the North African Margin. Bulletin de la Société Géologique de France, 169: 797–810 http://www.researchgate.net/publication/285744534_Structural_evolution_of_the_Maghreb_Atlasic_domains_during_Mesozoic_and_Cenozoic_times_The_role_of_inherited_structures_during_the_deformation_of_the_North_African_margin |
| Rabhi, M., Ben Ayed, N., 1990. Mise en Evidence d'une Tectonique Compressive d'âge Aptien Supérieur en Tunisie Centrale. Notes Serv. Géol., Tunise. 56 http://www.researchgate.net/publication/316991270_Mise_en_evidence_d'une_tectonique_compressive_d'age_Aptien_superieur_en_Tunisie_centrale |
| Rigane, A., Feki, M., Gourmelen, C., et al., 2010. The "Aptian Crisis" of the South-Tethyan Margin: New Tectonic Data in Tunisia. Journal of African Earth Sciences, 57: 360–366 doi: 10.1016/j.jafrearsci.2009.11.005 |
| Segev, A., Weissbrod, T., Lang, B., 2005. 40Ar/39Ar Dating of the Aptian-Albian Igneous Rocks in Makhtesh Ramon (Negev, Israel) and Its Stratigraphic Implications. Cretaceous Research, 26: 633–656 doi: 10.1016/j.cretres.2005.03.003 |
| Snoke, A. W., Schamel, S., Karasek, R. M., 1988. Structural Evolution of Djebel Debadib Anticline: A Clue to the Regional Tectonic Style of Tunisian Atlas. Tectonics, 7: 497–516 doi: 10.1029/TC007i003p00497 |
| Soyer, C., Tricart, P., 1987. The Aptian crisis in Central Tunisia: A Paleostructural Approach at the Atlas and North-South Axis Junction. Comptes Rendus de l'Académie des Sciences Paris, 305(Série Ⅱ): 301–305 http://www.researchgate.net/publication/279551599_The_Aptian_Crisis_in_central_Tunisia_a_paleostructural_approach_at_the_Atlas_and_North-South_Axis_junctionLa_crise_aptienne_en_Tunisie_centrale_approche_paleostructurale_aux_confins_de_l'Atlas_et_de_l |
| Tlatli, M., 1980. Etude des Calcaires de l'Albo-Aptien des Djebels Serdj et Bellouta (Tunisie Centrale): [Dissertation]. Université de Marseille. 187 |
| Zghal, I., 1994. Etude Microbiostratigraphique du Crétacé Inférieur de la Tunisie du Centre Ouest: [Dissertation]. Université Tunis Ⅱ, Tunisia. 393 |
| Zghal, I., Ouali, J., Bismuth, H., 1997. Syn-Sedimentary Tectonics in Central Tunisia (Jebel Mrhila area) during the Aptian-Albian. Comptes Rendus de l'Académie des Sciences Paris, 326: 187–192 http://www.ingentaconnect.com/content/els/12518050/1998/00000326/00000003/art89034 |
| Zouaghi, T., Ferhi, I., Bedir, M., et al., 2011. Analysis of Cretaceous (Aptian) Strata in Central Tunisia, Using 2D Seismic Data and Well Logs. Journal of African Earth Sciences, 61: 38–61 doi: 10.1016/j.jafrearsci.2011.05.002 |
| Zouari, H., Turki, M. M., Delteil, J., et al., 1999. Tectonic Transtension of Tunisian Palaeo-Margin during Aptian-Campanian. Bulletin de la Société Géologique de France, 170(3): 295–301 http://www.researchgate.net/publication/279567899_Tectonic_transtension_of_Tunisian_palaeo-margin_during_Aptian-Campanian |
Figures(9)
Copyright © 2013-2020 Journal of Earth Science 鄂ICP备15021562号-2
Tel: +86-27-67885075 Fax: +86-27-67885075 E-mail: xbb@cug.edu.cn
Address: Editorial Office of Journal, China University of Geosciences, Yujiashan, Wuhan, Hubei 430074, P. R. China
Supported by:
Beijing Renhe Information Technology Co. Ltd
E-mail:
info@rhhz.net
Imen Marco, Ferid Dhahri, Taoufik Haji, Noureddine Boukadi. Aptian-Albian Transition in Central Tunisia: Tectonosedimentary and Paleogeographic Records. Journal of Earth Science, 2014, 25(5): 787-798. doi: 10.1007/s12583-014-0478-7
DownLoad:
DownLoad:
