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Maalaoui ACTA LAYAUT Acta Geologica Polonica, Vol. 66 (2016), No. 1, pp. 43–58 DOI: 10.1515/agp-2016-0002 The lower and middle Berriasian in Central Tunisia: Integrated ammonite and calpionellid biostratigraphy of the Sidi Kralif Formation KAMEL MAALAOUI1, 2 and FOUAD ZARGOUNI 1 1 Department of Geology, Faculty of Sciences of Tunis, Science University of Tunisia, Tunis 2092 El Manar-I, Tunisia. 2 Geological Survey, National Office of Mines.24, Street of Energy, 2035-Charguia-Tunis.BP: 215-10801Tunis Cedex- Tunisia. E-mails: [email protected]; [email protected] ABSTRACT : Maalaoui, K. and Zargouni, F. 2016. The lower and middle Berriasian in Central Tunisia: Integrated ammonite and calpionellid biostratigraphy of the Sidi Kralif Formation. Acta Geologica Polonica, 66 (1), 43–58. Warszawa. The lower and middle Berriasian sedimentary succession of the Sidi Kralif Formation has been a subject of bios- tratigraphic study in two key sections in Central Tunisia. Our contribution is an attempt to better define the basal Berriasian interval, between the Berriasella jacobi Zone and the Subthurmannia occitanica Zone. Zonal schemes are established using ammonites and calpionellids, and these permit correlation with other regions of Mediterranean Tethys and beyond. The use of biomarkers afforded by microfossil groups has allowed charac- terization and direct correlation with four widely accepted calpionellid sub-zones, namely Calpionella alpina, Remaniella, Calpionella elliptica and Tintinopsella longa. The two ammonite zones of Berriasella jacobi and of Subthurmannia occitanica are recognised on the basis of their index species. The parallel ammonite and cal- pionellid zonations are useful as a tool for correlation and calibration in time and space, thus allowing a better definition of a J/K boundary. The presence of four Berriasian calpionellid bioevents is recognised: (1) the ‘ex- plosion’ of Calpionella alpina, (2) the first occurrence of Remaniella, (3) the first occurrence of Calpionella el- liptica and (4) the first occurrence of Tintinopsella longa. The last is here documented as coeval with the pres- ence of Subthurmannia occitanica, which marks the lower/middle Berriasian boundary. Key words: Ammonite; Calpionellids; Berriasian; Bioevents; Biostratigraphy; Tunisia. INTRODUCTION boundary (Wimbledon et al. 2011), in an interval strad- dling the traditional base of the Berriasian Stage, the In spite of intensive studies during recent decades, lower boundary of the Cretaceous. Successions across the formal definition of the Jurassic/Cretaceous bound- this critical interval, spanning the upper Tithonian and ary is still a problem, and it is the only Phanerozoic sys- lower Berriasian, are known in Tunisia, in south-west- tem boundary for which a GSSP has not been fixed (e.g., ern Mediterranean Tethys. Many good sections are well- Remane 1991; Zakharov et al. 1996; Wimbledon 2008; exposed in the central part of the country. Pessagno et al. 2009; Wimbledon et al. 2011; Wimble- The present paper provides a biostratigraphic report don et al. 2014). There is a number of biological mark- on the lower and middle Berriasian (Lower Cretaceous) ers which may potentially be used as a marker for this succession of central Tunisia. Two sections, represen- 44 KAMEL MAALAOUI AND FOUAD ZARGOUNI Italy Iberia N Africa Dj. Touila Zeroud Oued Djebe Touati N T allit J .362 EBE al K horshif L 478 EL Dj. Bou Gobrine Dj. M Guefaiat NAR 494 Ali Djeridi Dj. Nara 564 Kef Khoudja .568 0 5 4 539 Kef Krakrmat 1Km Kef el Hassine 0 SK Dj .Attaris f ha l i Sebkhet K id. el 602 S .705 Bahira J . .570 .667 .474 b u .645 rro .661 a h .565 K .480 el .408 Dj. Akhouta .393 440 . O. a O. Tebag O. Ne J. kh Ti hala la .330 Jh. Sidi K alif 660 Key 40 Neogene Thrust fault O.en Nakhla 400 640 Cenomanian to Paleocene Elevation h Alla Dj. Faid Barremian (Boudinar Formation) Nasr Creek e Valanginian-Hauterrivian ed SF A X Pist (Meloussi Formation) Gravel road Upper Tithonian-Upper Berriasian: (Sidi kralif Formation) Location of studied sections Jurassic dolomitic (Nara Formation) Triassic Text-fig. 1. Geological map of Central Tunisia (after Guiraud 1968, simplified) and location of the measured sections: SK - Sidi Kralif Section; N - Nara Section 45 BASAL CRETACEOUS BIOSTRATIGRAPHY IN TUNISIA Text-fig. 2. A – Panoramic view of the Jebel Sidi Khalif; B – The Nara section 46 KAMEL MAALAOUI AND FOUAD ZARGOUNI tative for the Sidi Khalif and Nara Hill ranges (Text-figs for calpionellids. The calpionellids were studied in thin 1, 2) were selected. The Berriasian of these ranges is rep- sections (25 in total) studied under an OLYMPUS BH- resented by marls, marly limestones and micritic lime- 2 transmitted light microscope, and photographed with stones of the Sidi Kralif Formation (Burollet 1956). Nikon COOLPIX L310 camera. All fossils described are The formation is underlain by dolostones of the Nara stored in the collections of the Geological Survey of the Formation and overlain by the massive dolostone-sand- National Office of Mines of Tunisia. stone of the Meloussi Formation. There is extensive bibliography on the geology of central Tunisia (e.g. Breistroffer 1937; Castany 1951; GEOLOGICAL SETTING Arnould-Saget 1951; Burollet 1956; Bonnefous 1972; Guirand 1968; M’Rabet 1987). The biostratigraphy of The study area is a part of the foreland of the the Sidi Kralif Formation was studied by Bismuth et al. Tunisian Maghrebide Chain, in the northernmost part (1967), Memmi (1967) and Busnardo et al. (1976, of the structure known as the N-S Axis (Text-fig. 1), 1981). Bismuth et al. (1967) recognised four calpi- which limits the western part of the Sahel plains (Cas- onellids zones in the Sidi Kralif Formation, although did tany 1951; Burollet 1956). The axis is a N-S anticline not calibrate them to the ammonite zonation. Memmi that interferes locally with NE-SW folds (Castany (1967) recorded a succession of upper Tithonian and 1951; Burollet 1956; Richert 1971; Ouali 2007). It is a Berriasian ammonites in the Sidi Kralif Formation in the major palaeogeographical limit that has been inter- northern part of Jebel Nara and at Chaabet Attaris. preted as having been a shoal at different times during Both calpionellid and ammonite assemblages were the Mesozoic (Burollet 1956; M’Rabet 1987; Soussi et analysed by Busnardo et al. (1976, 1981). These authors al. 2000). During late Jurassic to early Cretaceous characterized the Beriasella jacobi Zone; the Pseudo- times, Central Tunisia experienced continuous and reg- subplanites grandis Zone was difficult to define, but ular sedimentation with a relatively slow subsidence in seemingly ammonites were seen as different compared an infra-neritic depositional environment (Burollet, to the B. jacobi Zone assemblage. In the Nara Range, 1956). The evolution of the sedimentation of the Sidi they recognised a P. grandis Zone interval with calpi- Kralif Formation reflects the geological history of cen- onellids. The Subthurmannia occitanica Zone of the tral Tunisia during J/K boundary times. Its lower part middle Berriasian was also characterized by calpionel- was deposited in relatively deep water with a marly- lids. The middle/upper Berriasian boundary could not be limestone sedimentation, whereas its upper part shows accurately determined because the fauna was found to essentially clay sediments and indicates shallower wa- be very rare. ters. The decrease in depth is related to an increase in Both calpionellids and ammonites are critical in at- clastic sediments not compensated by subsidence, tempts to define the Jurassic–Cretaceous boundary which explains the diachronism of this formation (Bus- (Wimbledon et al. 2011). Ammonites and calpionellids nardo et al. 1981). In fact, central Tunisia was an ex- are treated in both sections studied herein, with the aim ternal carbonate platform during the early Tithonian, of calibration and correlation with other key sections in except for the Chotts region (the salt-lake area) that cor- the Tethyan Realm: e.g., Msila area in the internal Pre- responds to a littoral platform (Bonnefous 1972). Dur- rif of Morocco (Benzaggagh et al. 2010); Le Chouet in ing the late Tithonian, the first clay deposits arrived on SE France (Wimbledon et al. 2013); Puerto Escano in this platform in a prodeltaic situation. In late Tithon- Spain (Pruner et al. 2010); Fiume Bosso in central Italy ian to mid Berriasian times the deposits prograded to- (Housa et al. 2004); Brodno in Western Carpathians, wards Jebel Meloussi and Jebel Bouhedma. Jebel Sidi Slovakia (Housa et al.1999); Nutzhof in Austria Khalif and areas further north were still on an external (Lukeneder et al. 2010). All these sections have been carbonate platform with marly limestone sedimentation discussed recently by Michalik and Rehakova (2011). (Busnardo et al. 1981; M’Rabet 1987). MATERIAL AND METHODS AMMONITE AND CALPIONELLID RECORD IN THE STUDIED SECTIONS Our detailed biostratigraphic survey has been on two sections: at Sidi Khalif (the type section of the Sidi The Sidi Kralif Formation (Text-fig. 2) consists of Kralif Formation), and at Nara (Memmi 1967), locali- clays and dark grey or black marls with a green or ties which are c. 18 km apart. Both sections were col- bluish patina, often fissile, with a number of limestone lected for ammonites, and limestone beds were sampled or sandstone beds (M’Rabet 1987). It has two informal 47 BASAL CRETACEOUS BIOSTRATIGRAPHY IN TUNISIA members (see Busnardo et al. 1976); (1) the lower com- The Berriasian of the Sidi Khalif section is c. 368 m posed of calcareous marls, with pyritic ammonites, thick. The succession is divided into two members; the belemnites, calpionellids, rare bivalves and brachiopods, lower, spanning beds SK2–SK42, and the upper, beds and (2) the upper, composed of clays and marls, with nu- SK43–SK47. The lowermost part of the succession merous limestone beds, rich in bivalves, gastropods, bra- consists of alternating beds of marls and limestones of chiopods, echinoids, and ammonites, and rare calpi- very irregular thickness.
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