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U–Pb LA-ICP-MS Detrital Zircon Ages from the Cambrian of Al

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U–Pb LA-ICP-MS Detrital Zircon Ages from the Cambrian of Al Journal of African Earth Sciences 79 (2013) 74–97 Contents lists available at SciVerse ScienceDirect Journal of African Earth Sciences journal homepage: www.elsevier.com/locate/jafrearsci U–Pb LA-ICP-MS detrital zircon ages from the Cambrian of Al Qarqaf Arch, central-western Libya: Provenance of the West Gondwanan sand sea at the dawn of the early Palaeozoic ⇑ Muftah Mahmud Altumi a, Olaf Elicki b, , Ulf Linnemann c, Mandy Hofmann c, Anja Sagawe c, Andreas Gärtner c a Libyan Petroleum Institute, Gergarsh Road, 6431 Tripoli, Libya b Freiberg University, Geological Institute, Bernhard-von-Cotta Street 2, 09599 Freiberg, Germany c Senckenberg Natural History Collections Dresden, Museum of Mineralogy and Geology, GeoPlasmaLab, Königsbrücker Landstraße 159, 01109 Dresden, Germany article info abstract Article history: Detrital zircons from various stratigraphic levels of the sandstone-dominated Cambrian Hasawnah For- Received 4 April 2012 mation of the Al Qarqaf Arch type area (central-western Libya, Saharan Metacraton area) were geochro- Received in revised form 3 November 2012 nologically investigated for the first time by LA-ICP-MS techniques for U, Th, and Pb isotopes. Of 720 Accepted 5 November 2012 analyzed grains, 329 were concordant. Of the total, about 60% of the U–Pb zircon ages are Neoproterozoic Available online 29 November 2012 and earliest Cambrian and cluster at c. 700–680, 670–650, 615–610, 590, 570–560, and c. 540–525 Ma. These zircon populations are interpreted as detrital material derived from the Pan-African and possibly Keywords: to a smaller proportion from the Cadomian orogen situated marginal to northwestern Gondwana. A Hasawnah Formation few slightly older Neoproterozoic ages (c. 950–750 Ma) point to rifting events related to the dispersal Libya Geochronology of the Rodinia supercontinent. A minority of zircons became formed during the configuration of Rodinia Cambrian and cluster around the Mesoproterozoic–Neoproterozoic boundary (1039 ± 11, 1006 ± 12 and Gondwana 993 ± 13 Ma). Further, some early Mesoproterozoic zircon ages had been found (1592 ± 39 and Saharan Metacraton 1475 ± 20 Ma). The potential source area for the Mesoproterozoic zircons is interpreted to have been far distant from the Al Qarqaf Arch, probably concealed within the Arabian–Nubian Shield or situated in Chad, or in the Congo and Tanzania cratons. There is still no evidence for the existence of massive Mes- oproterozoic crust in the Saharan Metacraton area. A considerable proportion (28%) of zircons represents Palaeoproterozoic populations at c. 2.4–2.3 Ga, and c. 2.2–1.6 Ga. Less than 5% of all zircons are Archaean in age (c. 3.4–3.25 Ga, c. 2.95–2.7 Ga, c. 2.6–2.5 Ga). A potential source area for Palaeoproterozoic and Archaean zircon grains is the West African Craton and the western part of the Saharan Metacraton. The best candidates for the main source region for the sandstones of the Hasawnah Formation in the Al Qarqaf Arch type area are the Neoproterozoic–early Cambrian orogens of the Pan-African cycle in the Trans-Saharan Belt (Pharussian and Dahomeyean belts) and of the peri-Gondwanan terranes (Cado- mia). This conclusion is in accordance with published data from the Hoggar (Tassilis, Algeria) and from southwestern (eastern Murzuq Basin) and southeastern Libya (Al Kufrah Basin). In comparison to the strong input of Neoproterozoic zircon grains, input from the Palaeoproterozoic and Archaean sources of the cratonic basement (Saharan Metacraton and West African craton) is relatively limited. The exact source of the exotic Mesoproterozoic zircons remains problematic. The presented data lead to the conclus ion that the centre of early Palaeozoic thermal subsidence in central-northern Africa has to be located in the region of the Saharan Metacraton. The distinct unconformity at the base of the Cambrian Hasawnah Formation indicates major uplift and considerable denudation in the latest Neoproterozoic to early Cam- brian time interval. Because of the conspicuous maturity of the Hasawnah Formation siliciclastic depos- its, a coeval intense chemical weathering under warm to humid climatic conditions in low to moderate southern latitudes and the formation of a Gondwanan peneplain is indicated. Ó 2012 Elsevier Ltd. All rights reserved. ⇑ Corresponding author. Tel.: +49 (0)3731 39 2435; fax: +49 (0)3731 39 12435. E-mail addresses: [email protected] (O. Elicki), [email protected] (U. Linnemann). 1464-343X/$ - see front matter Ó 2012 Elsevier Ltd. All rights reserved. http://dx.doi.org/10.1016/j.jafrearsci.2012.11.007 M.M. Altumi et al. / Journal of African Earth Sciences 79 (2013) 74–97 75 1. Introduction 2. Geological setting The late Proterozoic to early Phanerozoic represents a period of The Neoproterozoic to earliest Palaeozoic structural evolution fundamental reorganization of geological processes and of sedi- of northeastern Africa is mainly characterized by two tectonic mentological, palaeogeographic, structural, climatic and evolution- phases following the breakup of the late Precambrian superconti- ary settings. One focus of these dramatic changes in Earth history is nents Rodinia and Pannotia: the Pan-African amalgamation and in the origination and early evolution of the northern margin of the the ‘‘Infracambrian’’ extension (Craig et al., 2008; Johnson et al., Gondwana palaeosupercontinent. With the aim of developing a 2011). During the first of these intervals a few palaeooceans had comprehensive model for the dynamic evolution of the northern been closed, among which the Trans-Saharan Ocean was most Gondwanan margin in the Ediacaran to early Palaeozoic, investiga- important with respect to present southern Libya (Schandelmeier tions have been significantly intensified during the last decade. and Wipfler, 1999). Whereas data from northwestern Africa, the Near East, western In Libya, early Palaeozoic rocks are mainly exposed at the mar- and central Europe and the Sinai Peninsula and Israel have already gins of large intracratonic basins in the central-western to south- been published, data from central-northern Africa is limited. western region of the country (Ghadamis Basin, Murzuq Basin), Hence, there is a significant knowledge gap to be filled in order in the southeast (Al Kufrah Basin), and in the Tibesti Mountains to create a consistent reconstruction of the entire palaeogeograph- in the south (Al Festawi, 2001; Tawadros, 2001). One of the most ic region. important outcrop areas is in the Jebel Hasawnah (also called Jebel In extensive areas of northern Africa the Precambrian igneous Fezzan or Jebel Al Qarqaf) of the Al Qarqaf Arch (AQA; Fig. 1), a and/or metamorphosed basement is nonconformably covered by prominent southwest-trending uplift structure in Libya, mainly a Cambrian–Ordovician sandstone blanket (Beuf et al., 1971; formed by Caledonian and Hercynian movements (Al Festawi, Tawadros, 2001, 2012; Hallett, 2002; Squire et al., 2006; Linne- 2001). The amplitude of the uplift is about 6000 m (up to 800 m mann et al., 2011). This phenomenon is also known from other elevation at present surface) in the AQA area relative to the base- time-equivalent regions of the world (e.g. Middle East and North ment level in the northern Ghadamis Basin area where this level America: Powell, 1989; Sharland et al., 2001; Khalifa et al., 2006; is about 5200 m below surface (Hallett, 2002). Following Al Fasa- Shinaq and Elicki, 2007; Hagadorn, 2011). Such regions offer an twi et al. (2003), the AQA was a topographic high already in late excellent opportunity to study such fundamental geological pro- Cambrian to early Ordovician time. Tectonic activity during the cesses as tectonic evolution, depositional history, erosion and Mesozoic and Cenozoic modified the region to various extents. transportation from source areas, palaeoclimate, and structuring The last tectonic uplift of significant amplitude was during the Al- of early life systems of this time window. In some regions there pine phase of deformation and is indicated by apatite fission track is also some economic aspect where included sediments, as in Li- data (Craig et al., 2008). The AQA largely separates the Ghadamis bya, are significant elements of source rock or reservoir architec- Basin in the northwest from the Murzuq Basin in the south ture or if they denote important aquifers (Binsariti and Saeed, (Fig. 1) and represents the northernmost basement outcrop of 2000; Hallett, 2002; Craig et al., 2008, 2009). the so-called Saharan Metacraton (Abdelsalam et al., 2002; East This paper is stratigraphically and regionally focussed on such a Saharan Craton sensu Bertrand and Caby, 1978) in this part of Afri- sedimentary cover: the Cambrian Hasawnah Formation of the Al ca (Conant and Goudarzi, 1967; Tawadros, 2001). Qarqaf Arch area of central-western Libya. The first detailed geo- Palaeogeographically, the study area was situated at the wes- logical investigation of the area was undertaken early in the second tern margin of the Gondwana palaeocontinent, which was in low half of the last century (Massa and Collomb, 1960; Collomb, 1962; to moderate southern latitudes at the beginning of the Cambrian Hecht et al., 1963; Goudarzi, 1970; Jurák, 1978) for mapping and and migrated southward during Cambrian and Ordovician time exploration of natural resources. A second, important increase in (e.g. Scotese, 2009; Torsvik and Cocks, 2009). knowledge has been published since the 1980s and has continued The first geochronological data for basement granitoids from until recent time mainly due to oil exploration activities in Palae- various regions of the AQA were published by Schürmann (1974), ozoic basins in the region (Salem and Busrewil, 1980; Salem and who presented ages of 640–549 Ma (Rb/Sr) and 541–491 Ma (K/ Belaid, 1991; Salem et al., 1991a,b,c, 2003, 2008a,b,c; Klitzsch Ar) for muscovite granites. These are consistent with additional and Thorweihe, 1999; Sola and Worsley, 2000; Tawadros, 2001; data (K/Ar ages of 554–520 Ma) later reported by Jurák (1978). Hallett, 2002; Salem and Oun, 2003; Salem and El-Hawat, 2008).
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