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Palynological and Palynofacies Analyses of Upper Cretaceous Deposits in the Hateg Basin, Southern Carpathians, Romania

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Palynological and Palynofacies Analyses of Upper Cretaceous Deposits in the Hateg Basin, Southern Carpathians, Romania Cretaceous Research 104 (2019) 104185 Contents lists available at ScienceDirect Cretaceous Research journal homepage: www.elsevier.com/locate/CretRes Palynological and palynofacies analyses of Upper Cretaceous deposits in the Hat¸ eg Basin, southern Carpathians, Romania * Daniel T¸abar a a, , Hamid Slimani b a “Al. I. Cuza” University of Ias¸ i, Department of Geology, 20A Carol I Blv., 700505 Ias¸ i, Romania b Geo-Biodiversity and Natural Patrimony Laboratory (GEOBIO), “Geophysics, Natural Patrimony and Green Chemistry” Research Center (GEOPAC), Scientific Institute, University Mohammed V in Rabat, Avenue Ibn Batouta, P.B. 703, 10106, Rabat-Agdal, Morocco article info abstract Article history: We present biostratigraphical and palaeoenvironmental analyses based on palynology and palynofacies Received 22 January 2019 of marine and terrestrial deposits that crop out in the central and northwestern part of the Hat¸ eg Basin. Received in revised form Samples were collected from the Rachitova and Sînpetru formations. The former yielded well-preserved 9 July 2019 palynological assemblages of both terrestrial and marine origin, represented mainly by diverse spore and Accepted in revised form 12 July 2019 pollen associations, but with dinoflagellate assemblages of low diversity and low to moderate abun- Available online 18 July 2019 dance. The terrestrial palynoflora is dominated by fern spores and subordinate gymnosperm and angiosperm pollen. This assemblage is indicative of a vegetation of subtropical to warm-temperate Keywords: fl Palynology climate and suggests uvial to coastal habitats, as well as well-drained and higher altitude areas. The e Palynofacies Rachitova Formation is here dated as Santonian early late Campanian, based on the dinocyst species Palaeoenvironment Isabelidinium microarmum and some fern spores and early angiosperm pollen. The Sînpetru Formation, SantonianeMaastrichtian previously dated as Maastrichtian, yielded only terrestrial palynoflora, but with a low content in paly- Southeastern Europe nomorphs. Nevertheless, its palynological assemblage, composed of Maastrichtian pollen and spores, indicates lowland or coastal habitats and warm and humid climatic conditions, alternating with periods of arid climate. The palynofacies constituents used to reconstruct the depositional environments suggest that during the Santonianeearly late Campanian, strata were laid down in an inner-outer neritic envi- ronment (with some fluctuations of water depth). This succession is followed by a deltaic to pond or lake depositions during the Maastrichtian, as indicated by the presence of large translucent phytoclasts in these deposits. A new dinocyst subspecies, Isabelidinium microarmum subsp. bicavatum, which is a distinguishable bicavate cyst, is described herein; this represents a possible key taxon for the lower to lower upper Campanian. © 2019 Elsevier Ltd. All rights reserved. 1. Introduction 2016). The megaflora is rare, being represented by ferns (Asple- nium foersteri), monocotyledons (Sabalites longirhachis) and di- The Maastrichtian terrestrial strata exposed in the Hat¸ eg Basin cotyledons (Araliaephyllum sp., Myrica primigenia and (western part of the southern Carpathians, Romania), are well Proteophyllum decorum). The mesoflora recorded from the north- known for their palaeontological content, comprising mainly western part of the basin includes fruits and seeds (aff. Klikovis- various species of dinosaur (including egg nests), mammals and permum and aff. Eurya) that belonged to plants of the Normapolles other vertebrates (Csiki and Grigorescu, 2000; Grigorescu, 2010; complex (May Lindfors et al., 2010). Csiki et al., 2010; Botfalvai et al., 2017; Csiki-Sava et al., 2018). The first palynological study on Maastrichtian successions of the Mega- and mesofloral remains from the Maastrichtian deposits of Hat¸ eg area were carried out by Stancu et al. (1980) and Antonescu the Hat¸ eg Basin have previously been described by Marg arit and et al. (1983), who recorded terrestrial palynomorphs such as fern Marg arit (1967), May Lindfors et al. (2010) and Popa et al. (2014, spores (Polypodiaceoisporites, Leiotriletes), Normapolles pollen (Trudopollis, Oculopollis) and a few gymnosperms. Other palyno- logical studies of the same deposits have highlighted an assemblage * Corresponding author. with numerous fern spore taxa (inclusive of freshwater ferns) and E-mail addresses: [email protected] (D. T¸abara), [email protected] various species of angiosperm pollen (Normapolles group), (H. Slimani). https://doi.org/10.1016/j.cretres.2019.07.015 0195-6671/© 2019 Elsevier Ltd. All rights reserved. 2 D. T¸abar a, H. Slimani / Cretaceous Research 104 (2019) 104185 D. T¸abar a, H. Slimani / Cretaceous Research 104 (2019) 104185 3 indicating a subtropical climate (Van Itterbeeck et al., 2005; Csiki of the Hat¸ eg Basin and terrestrial strata (Sînpetru Formation) in the et al., 2008). central part (Fig. 1). In the deeper parts of the Hat¸ eg Basin, outcropping Maas- trichtian terrestrial successions rest on CenomanianeCampanian 3.1. Rachitova Formation strata that are mainly marine (Grigorescu and Melinte, 2001; Melinte-Dobrinescu, 2010). Based on the lithological and sedi- This unit was first described by Grigorescu and Melinte (2001), mentological characteristics of these marine strata in the north- the stratotype being located in the Rachitova Valley (Fig. 1B). The western Hat¸ eg area, Melinte-Dobrinescu (2010) suggested a mainly Rachitova Formation (~900 m thick) is divided into two members, deep-water palaeoenvironment for this interval. the Lower Member and Upper Member. The former comprises The present study aims to contribute to the palynological data for 500e700 m of sandy turbidites (Melinte-Dobrinescu, 2010), rep- Upper Cretaceous terrestrial and marine deposits that crop out in the resented by calcareous sandstones, grey siltstones and claystone central and northwestern part of the Hat¸egBasin.Thedinoflagellate interlayers. In the studied outcrop along the Rachitova Valley cyst assemblage, identified in marine deposits of the region, is here (Fig. 1E), this member is characterized by the presence of a level described for the first time. The present work also aims to establish with poorly preserved fossil plant remains, considered as a litho- palaeoenvironmental conditions during deposition of this interval, as logical marker for its lower part by Melinte-Dobrinescu (2010). The based on palynofacies characteristics and the palynomorph taxa. Lower Member was dated as early Santonianeearly/late Campa- nian on the basis of calcareous nannofossil taxa indicative of zones 2. Geological setting CC16 up to CC20 (Melinte-Dobrinescu, 2010). The Upper Member is ~300 m thick at the Rachitova Valley site and The Hat¸ eg Basin, located in the western part of the Southern Car- consists of turbidites, represented by grey claystones with pathians in Romania (Fig.1A), includes a basement of crystalline rocks centimetre-thick calcarenite interlayers. A nannofossil event, i.e., first of the Getic Nappe, a tectonic unit that belongs to the Median Dacidic occurrence datums of Uniplanarius sissinghii and U. trifidus,indicatesa Nappe System (Sandulescu,1984 ), and a cover of sedimentary rocks of late Campanian age for this member (Grigorescu and Melinte, 2001; about 4 km in thickness. This basin is created in response to the Late Melinte-Dobrinescu, 2010). Strata assigned to this member are Cretaceous collision of at least three plates (Getic and Danubian units strongly folded (Fig. 1D) and crop out along the S¸ tei Valley (Fig. 1B). and an allochthonous continental block of the Moesian Platform; Fig. 1), upon closure of a narrow oceanic basin (Willingshofer et al., 3.2. Sînpetru Formation 2001). The oldest deposits that cover the Getic basement are Lower Jurassic terrestrial clastics. Starting in the Middle Jurassic, marine This formation is distributed across the central-eastern parts of sedimentation comprised limestones and marls (Stilla, 1985; Pop, the Hat¸ eg Basin (Fig. 1A), mainly along the Sibis¸ el and Barbat val- 1990). This type of deposition continued up to the Aptian, when leys. Although the entire stratigraphic interval of the formation is reef and fore-reef limestone were laid down. The Middle not exposed, Nopcsa (1905) estimated the Sînpetru Formation to JurassiceAptian marine sedimentation is followed by exhumation have been approximately 2,500 m thick, as based on the distribu- and erosion of the area, as indicated at the AptianeAlbian boundary tion of exposures within the basin. The commonest rocks comprise by bauxites accumulated within a palaeokarst (Nast aseanu, 1975). poorly sorted fluvial sandstones (or conglomerate) and floodplain At the start of the Late Cretaceous (early Cenomanian), the mudstones (Bojar et al., 2005; Therrien, 2006), yielding large Hat¸ eg region evolved towards a longitudinal basin (eastewest di- numbers of fossil vertebrate remains (Grigorescu, 2010). Along the rection), which allowed the accumulation of deep-marine hemi- Sibis¸ el Valley, the Sînpetru Formation includes two members. The pelagic deposits (Stei and Rachitova formations) in the northwest, lower member displays an admixture of grey-green mudstones and shallow-water ones in the southeast (Grigorescu and Melinte, with red mudstones and sandstones (Fig. 1C), while the upper 2001; Melinte-Dobrinescu, 2010). The marine sedimentation member is characterised by the presence of coarser channel de- ended towards the top of the Campanian throughout the
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