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Palygorskite Genesis Through Silicate Transformation in Tunisian

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Palygorskite Genesis Through Silicate Transformation in Tunisian ClayMinerals (2003)38, 187–199 Palygorskitegenesisthroughsilicate transformationinTunisiancontinental Eocenedeposits 1 2 2, F. JA M O USSI ,A.BENABOUD A ND A . LO´ PEZ-GALINDO * 1 Laboratoire‘ Ge´oressources’, INRST BP95,2050 Hamam-Lif,Tunisia, and 2 InstitutoAndaluz de Ciencias de la Tierra,CSIC-Universidad de Granada, Facultad de Ciencias, Fuentenueva s/ n,18002 Granada,Spain (Received 30 April 2002; revised 21 October 2002 ) ABSTRACT:The mineralogical and geochemical characteristics of Eocene continental sediments in south central Tunisia (Chebket Bouloufa and Jebel Hamri) and in north central Tunisia (Jebel Lessouda and Jebel Rhe´ouis), which contain considerable amounts of palygorskite, were studied. The clay fraction of the sediments also comprises illite, kaolinite, Mg smectite and Al smectite, together with carbonates (calcite and/or dolomite), quartz, gypsum and feldspars, all of which are present in extremely variable proportions. The textural characteristics of the samples containing most palygorskite, as well as the chemical composition of the fibres and the contents of certain trace and rare earth elements suggest that the genesis of this fibrous clay is intimately linked to the diagenetic transformation of illite, mixed- layered minerals and/or Al smectite, as has also been observed in contemporaneous deposits in Morocco. KEYWORDS:palygorskite,illite, Tunisia, Eocene. Withthe aim of drawinga mapof potentiallyuseful ContinentalEocene facies, studied by numerous claysin Tunisia, a systematicsurveyof the authors,are deposited in two main areas: in central Palaeozoicto Quaterna rysediment shasbeen Tunisia,around the so-called ‘ Kasserineisland’ performedover the last few years by one of the (Burollet,1956), and to the south of the Gulf of authors(F.J.).The survey showed numero us Gabe`sand the northern part of Jeffara. In central palygorskite-richEocenelevels that might be of Tunisia,Truc (1981) and Zouari (1984) found economicinterest. Eocenesediments at Jebel (J.) Chaambi and Sassi InTunisia, Eocene sediments present important et al.(1984)found them on the south-eastern flank faciesvariations from South to North, changing ofthe J. Kebar.In the J. Lessouda and Koumine, fromcontinental to deep marine deposits (Bishop, Kadri et al.(1986)and Kadri (1988) detected the 1988;Jamoussi et al.,2001a; Fig. 1). These samefacies, but Jamoussi (2001) pointed out that changesin facies and thickness are mainly due to theywere not immediately above the Ypresian Alpineco mpressivetec tonicev entsand th e carbonatebar. In the northern area of the Chotts halokineticmov ementso fTriassicmateri als belt,Abdeljaoued (1983, 1991, 1997) defined the affectingthe Central Atlas domain during the continentalformation of Bouloufa, dated by bulimes Eocene(Be ´dir,1995; Boukadi & Be´dir,1996). (continentalgastropods) as Lower Eocene; in J. Rhe´ouisand Boudinar, around the Kasserine island, continentaldeposits were also discovered and in J. *E-mail: [email protected] Chamsisuch sedimen tshave been suspec ted DOI: 10.1180/0009855033820088 (Jamoussi,2001; Jamoussi et al.,2001a). Finally, # 2003The Mineralogical Society 188 F. Jamoussi et al. Tunis IA R E G L A Mahdia J. Rhéouis * J. Lessouda Sfax Kerkennah * Island *J. Boudinar Gafsa J. Hamri J. Bouloufa ** Jerba Gabès N Medenine 0 50 100 km Emerged area Phosphate deposits A Y B Tidal zone (Sebkha) LI Supratidal to tidal zone Nummulitic limestone Marine deposits * Sectionsinvestigated FIG.1. Lithofacies map of the Lower Eocene in Tunisia (modified from Jamoussi et al.,2001) and the locations of the sections studied. thefirst oil drilling carried out in the southern part samplesin Tunisia. The better sequences are ofthe Gulf of Gabe `s,as well as some drilling in the locatedin some of the above-mention edareas northernpart of Jeffara, found continental Eocene (ChebketBouloufa, J. Hamri,J. Lessoudaand J. depositsknown as the Tanit Formation (Pochitaloff, Rhe´ouis).Some samples from J. Boudinarwere also 1968).The mineralogy of someof these deposits has studied. beendescribed by, among others, Abdeljaoued (1997),Srasra et al. (1995),Ben Aboud (1998), GEOLOGICALSETTING Hachi(1998), Ben Aboud et al.(1999),Fakhfakh (1999)and Jamoussi (2001). Theend of the Cretaceous is marked in central and Inthis paper we study the mineralogy, geochem- southernTunisia by important palaeogeograph ical istryand microtexture of palygorskite-ric hEocene andsedimentological modifications. Marine sedi- Palygorskite in Tunisian sediments 189 mentation,represented by white limestones with synsedimentaryinfluences on the distribution of inoceramidsand echinoderms, known as the Abiod faciesand their thickness from Upper Cretaceous Formation(Burollet, 1956), changes towards a more untilMiddle Miocene (Kadri, 1988). The sequence, detrital,clayey sediment during the Palaeocene. ~20m thick,is made up of alternating white, red Aftercompressive tectonic movements of transverse andgreen marls, with fine intercalations of gypsum. faultsduring the Upper Cretaceous (Zargouni, Althoughthe presence of bulimes in these 1985;Boukadi, 1994; Be ´dir,1995) some emerged continentalEocene deposits clearly indicates a areasappeare d,such as the above-me ntioned LowerEocene age, recurrenc esof continent al KasserineIsland. faciesseem to be diachronic and closely influenced Tertiarysequences are particularly well repre- bylocal tectonic conditions of the geological sentedin the North Chain of theChotts, and include substratum.The mineralogy of the clay fraction, severallithostratigraph icunits, such as Beglia and andparticularly the presence of palygorskite, could SeguiFormations, consisting of sand, clay and bean element of identification and inter-relation- conglomerates.One particular lithological member shipbetween these series, which have been marked wasdefined by Abdeljaoued (1983) as theBouloufa bycompressive movements and halokinetics of Formation,extending over a widearea on the Triassicrocks. southernedge of the Gafsa-Metlaoui phosphate basin.This formation appears, in most cases, as METHODOLOGY calcretesand dolocretes, with vacuolar appearance. At J.Chambi, Sassi et al.(1984)found one faunal Themineral phases were determined by X-ray assemblageconsisting of continental gastropods diffraction(XRD), usingPhilips PW 1710and (Romanellahopii , Vidaliella)andhelicids SiemensKristalloflex 810 diffractometers, Cu- Ka (Paleocyclotus )thatallowed this formation to be radiationat a scanspeed of 2 to6º 2 y min –1. datedas Lutecian-Bartonia n. Analysiswas performed on both the whole sample Themost repres entativesequenceso fthe andthe clay fraction. Oriented aggregates were BouloufaFormation crop out 25 km northwest of preparedfor clay mineral analysis and were then El Hammatown, at J. Bouloufa and J. Hamri. They treatedwith ethylene glycol, dimethyl-sulphoxi de are~150 m thickand are made up of alternating andheating to 550º C for1 h.The reflecting powers conglomerates,marls and limestones, white and red ofSchultz (1964), Biscaye (1965) and Barahona incolour, with some gypsum and silex nodules. (1974)were used to quantify the different mineral TheEocene deposit located at J. Rhe ´ouis,close phasesdetected, as well as the chemical composi- toa Triassicdiapir (Soussi et al.,1996),is situated tionsof samples (Lo ´pez-Galindo et al., 1996). incentral Tunisia, 10 km to the south of Fa ˆõ d, on Majorele mentswe rea nalysedb yatomic theboundary between the Sidi Bouzid and J. absorptionspectrometry, using Perkin Elmer equip- Goubrar1:50,000 topographic maps. It appears in mentwith acetylene or protoxide acetylene flame t. theintersection of NE –SW structuresof the North– Traceand rare earth elements ( REE)weremeasured SouthAxis, known as J. Goubrarand Boudinar, and usingan ICP-MS PerkinElmer SCIEX Elan-5000 the NW –SE foldof J. Ksa ¨õ ra(Boukadi and Be ´dir, device.The detection limits of the elements were 1996).Triass ichaloki neticmoveme ntsalo ng 10 ppb for REE andTh, 100 ppb for transition transversefaults led to cropping out of these elementsand Cs, Rb, Sr, Ba and Pb, and 1000 ppb structures,particularly during the Eocene (Boukadi for Li and B. andBe ´dir,1996). The sequence is ~40 m thick,and Thescanning electron microscope (SEM) obser- ismade up of white and grey limestones and marly vationswere performed using a ZeissDSM 950 limestones,marls and clayey marls. Some fine (equippedwith LINK microanalysissystem). The gypsumintercalations appear occasionally. transmissionelectron microscope (TEM) observa- Finally,J. Lessoudais situated ~10 km to the tionsand microanalyses were carried out on the Northof Sidi Bouzid town, at the western part of clayfraction of selected samples, using a Philips theNorth– South Axis. It constitu tesa N40E CM 20(equipped with an EDAX microanalysis anticlinesuperimposed on an Upper Cretaceous system). diapiricdome (Creuzot and Ouali, 1989), emerging Factoranalysis (Principal Components Analysis, inthe centre of a vastplain. It is fractured by km- PCA) wasused to establish the relation between the long N –S, NW –SE and E –Wfaults,which have differentminerals and major and trace element 190 F. Jamoussi et al. contents.The factors (principal components, Pcs) Two clearlydistinguished groups of palygorskite- weresele ctedfo reigenvalues>1(Swan & richoutcrops can be established: those located in Sandilands,1995) applying a Varimaxrotation. southcentral Tunisia (J. Bouloufa and J. Hamri), whichcontain considerable amounts of quartz, calciteand kaolinite, and those located in north R E S U L T S centralTunisia (J. Rhe ´ouisand J. Lessouda),
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