02_Schlagintweit za web.indd 29 Schlagintweit et al.: Onset of an Aptian carbonate platform overlying a Middle-Late Jurassic radiolaritic-ophiolithic mélange in the Mirdita Zone of Albania � AB STRA CT Late Jurassic and Early Cretaceous carbonate sediments of different age and facies form the post-emplacement set- tings on top of the Mirdita Ophiolite Zone in northern Albania. They seal the early Late Jurassic emplacement of the ophiolite nappes, and are the only datable relics overlying the ophiolites. They aid evaluating the different tectonic movements associated with uplift and erosion as well as sea-level fl uctuations during that time span. These carbon- ates overlie ophiolite-derived clastics very often as shallowing-upward sequences. One of the largest shallow-water platforms is the Mali I Shenjtit platform, previously assigned to the Barremian-Aptian. A well-preserved section at the base of the platform can be ascribed to the Early-Late Aptian based on orbitolinid foraminifera together with dasycladalean algae. This carbonate platform is the youngest preserved Early Cretaceous platform in Albania, but was largely eroded away. Late Cretaceous shallow-water rudist limestones are widespread and preserved in the Di- naride-Albanide-Hellenide realm directly above an eroded older basement. Therefore, this Aptian platform is very important for the reconstruction of the Early Cretaceous palaeogeography in the northwestern Neotethyan realm. In addition, the stratigraphic ranges of characteristic Aptian orbitolinid foraminifera, Rectodictyoconus giganteus SCHROEDER and Mesorbitolina texana (ROEMER), are discussed on the basis of these results. Keywords: Mirdita Ophiolite Zone, Platform Carbonates, Early Cretaceous, Neotethys Realm Onset of an Aptian carbonate platform overlying a Middle-Late Jurassic radiolaritic-ophiolithic mélange in the Mirdita Zone of Albania � Felix Schlagintweit1, Hans-Jürgen Gawlick2, Richard Lein3, Sigrid Missoni2 and Lirim Hoxha4 1 Lerchenauerstr. 167, D-80935 Munich, Germany; (ef.schlagintweit@t-online.de) 2 Department of Applied Geosciences and Geophysics, Chair of Prospection and Applied Sedimentology, University of Leoben, Peter-Tunner-Strasse 5, A-8700 Leoben, Austria; (gawlick@unileoben.ac.at; s.missoni@ daad-alumni.de) 3 University Vienna, Center for Earth Sciences, Althanstr. 14, A-1090 Vienna, Austria; (richard.lein@univie.ac.at) 4 Empire Mining Albania (Empire Mining Corporation) Rruga Perlat Rexhepi, Pallati Unikon, Kati i VI-te Ap. 28, Tirana, Albania; (l.hoxha@yahoo.com) doi: 104154/gc.2012.02 Geologia Croatica 65/1 29–40 8 Figs. Zagreb 2012 Geologia CroaticaGeologia Croatica 1. INTRODUCTION AND GEOLOGICAL SETTING The onset of carbonate platforms in tectonically active moun- tain ranges like the Albanides (Fig. 1) plays an important role in the reconstruction of the evolution of orogenic belts. The Mirdita zone in Albania consists of obducted Triassic-Jurassic ophiolites, which derived, according to the Triassic shelf ar- rangement, from the Neotethys Ocean further to the east (GAWLICK et al., 2008), comparable with the ophiolites in the Dinarides (SCHMID et al., 2008; GAWLICK et al., 2009). For a different palaeogeographic interpretation see e.g.: ROB- ERTSON & SHALLO (2000), DILEK et al. (2005); ROB- ERTSON et al. (2011). These ophiolites and the accompany- ing ophiolitic mélanges (radiolaritic-ophiolitic (wild-)fl ysch in the sense of GAWLICK et al., 2008), were overlain by sev- eral carbonate platforms of different ages, that sealed the em- placement of the ophiolite nappe stack and their obduction onto the Apulian lower plate in Oxfordian times. These plat- forms allow to reconstruct the post-emplacement history of the ophiolite nappes (e.g., ongoing tectonic movements, sea- level changes). The oldest proven platform is represented by the Kimmeridgian-Tithonian Kurbnesh carbonate platform Geologia Croatica 30 Geologia Croatica 65/1 Munella carbonate platform was established (PEZA & MAR KU, 2002; GAWLICK et al., 2008) in a tectonically ac- tive regime (SCHLAGINTWEIT et al., 2008; ROBERTSON et al., 2011). The Munella platform (e.g., in the regions of Mali I Munelles, Mali I Shenjtit – Fig. 2) in addition to the younger Mali I Shenjtit platform, represents the only autochthonous Early Cretaceous shallow-water carbonate platform in the area of the Mirdita Zone, covering large areas in central Albania. Both platforms were originally seen as one platform and were dated by PEZA & MARKU (2002) and PEZA & ZITT (2002) as Barremian to Aptian in age. GAWLICK et al. (2008) sub- divided this platform into representing two stages of shallow- water carbonate deposition, the older Munella carbonate plat- form (?Late Berriasian to Valanginian) and the younger Mali I Shenjtit platform (?Late Barremian to Aptian). Like the Late Jurassic Kurbnesh platform, the Munella carbonate platform was eroded in most areas. The next carbonate platform was established after this deep erosion in ?Barremian or Aptian times (GAWLICK et al., 2008). Nevertheless, the exact age of the onset of the Mali I Shenjtit platform has remained enig- matic, but is very important for the manifestation/correlation of tectonic events or sea-level fl uctuations in the whole Di- naridic-Albanide-Hellenide realm. West of Bulshari (Fig. 2), the Bathonian to Oxfordian radiolaritic-ophiolitic (wild)fl ysch (mélange) (Perlat Forma- tion: GAWLICK et al., 2008) and the overlying ?Early Cre- taceous conglomerates are followed by the onset of the Mali I Shenjtit carbonate platform (Fig. 3). At the base of the in- vestigated section (Fig. 4), directly on top of the mélange, a sequence of ophiolite-derived clastics (some tens of metres thick) is preserved (e.g., north of Konaj: Fig. 2). This suc- cession is overlain by a marine carbonate succession with a preserved shallowing-upward sequence. This paper describes the early evolution of the youngest Early Cretaceous platform in Albania together with new bio- stratigraphic and microfacies data. The results are important for the exact timing of ongoing tectonic movements in the Dinaride-Albanide mountain chain and to close a gap in knowledge of the age of the onset of different shallow-water carbonates above the Mirdita Ophiolite Zone. 2. SEDIMENTOLOGY, STRATIGRAPHY, AND MICROPALAEONTOLOGY 2.1. Microfacies and micropalaeontology of the resediments The microfacies of the mass-fl ows are represented by differ- ent types of packstones with bio- and lithoclasts of varying size and degrees of sorting. Some clasts are close-packed with stylolitized contacts. This fi tted fabric corresponds to the stylobreccia fabric of LOGAN & SEMENIUK (1976) (Fig. 5a). Sorting of the subangular clasts in these breccias is poor. The stylobreccia may directly overlie wackestones with dispersed larger litho- and bioclasts, mainly skeletons of stro- matoporoids and small globigerinid and globigerinelloid fora- minifera (Fig. 5a–b, f). The stromatoporoids belong to two taxa, Tubuliella fl uegeli TURNŠEK (Figs. 6i) and Tubuliella (SCHLAGINTWEIT et al., 2008), which was eroded in Early Cretaceous (Berriasian – Valanginian) times. After erosion of the Kurbnesh platform, the ?Late Berriasian-Valanginian Figure 1: A simplifi ed tectonic map of Albania (after NOWACK, 1928; XHO- MO et al., geological map of Albania 2002) and the study area. Geologia Croatica 31 Schlagintweit et al.: Onset of an Aptian carbonate platform overlying a Middle-Late Jurassic radiolaritic-ophiolithic mélange in the Mirdita Zone of Albania Figure 2: The Mali i Shenjtit carbonate platform and the Munella carbonate platform (Mali I Munelles) in the northern/central Mirdita zone. Simplifi ed geological map on the basis of the Harta Gjeologjike e Shqiperise 1 : 200.000 (XHOMO et al., 2002), redrawn with the integration of the present results (after GAWLICK et al., 2008; SCHLAGINTWEIT et al., 2008). The studied section is located west of the village of Bulshari. Geologia Croatica 32 Geologia Croatica 65/1 rotunda TURNŠEK (Fig. 6j), so far only known from the Late Jurassic of Slovenia (TURNŠEK, 1966), Croatia (MILAN, 1969) and Albania (SCHLAGINTWEIT et al., 2008). Tubu- liella is a typical representative of the so-called actinostro- mariid zone, characterizing the outer zone of Late Jurassic barrier-type reef complexes along shelf margins (TURNŠEK, 1969; TURNŠEK et al., 1981), thus explaining their resedi- mentation along a presumably rather steep slope, and their occurrence in the investigated mass-fl ows. The new Aptian fi ndings also provide clear evidence that the two taxa have broad stratigraphic ranges. Typical microencrusters such as Radiomura cautica SENOWBARI-DARYAN & SCHÄFER (Figs. 5c, 6b) and Crescentiella morronensis (CRESCENTI) (Fig. 6a) also occur in accordance with the inferred original platform margin setting of the resedimented limestones. Beside this, the packstones contain Dasycladalean algae: Triploporella sp., Acroporella radoicicae PRATURLON (Fig. 6d), Linoporella/Steinmanniporella sp. (Fig. 6g) and Stein- manniporella? parsica TAHERPOUR KHALIL ABAD et al. (Fig. 6e, h). This taxon was described recently from the Ap- tian of Iran (TAHERPOUR KHALIL ABAD et al. 2010). Higher up in the section, grain- to rudstones occur with dasycladalean algae and orbitolinid foraminifera. The two taxa characterizing this interval are Rectodictyoconus giganteus SCHROEDER (Fig. 7a–c) and Mesorbitolina texana (ROE- MER) (Fig. 7d–f) being of importance for the biostratigraphic dating of the section (Fig. 8). Figure 3: A) Field view of the Mali I Shenjtit carbonate platform overlying the Jurassic radiolaritic-ophiolitic mélange, in the upper part with ?Early Cretaceous deep-water conglomerates. B) Studied section north of Moun- tain Guri Cicit showing a shallowing-upward sequence, which refl ects a prograding platform. 2.2. Biostratigraphy Discussion of the biostratigraphy of Aptian strata, requires recognition that some authors use a bipartite division (Bedou- lian = Early, Gargasian + Clansayesian = Late Aptian) (e.g., SCHROEDER et al., 2010) while others prefer a tripartite di- vision (Bedoulian = Early, Gargasian = Middle, Clansayesian = Late Aptian) of the stage (e.g., CASTRO et al., 2002; GRADSTEIN et al., 2004). MASSE (2003) additionally dis- tinguished a Lower ?Early Bedoulian (Deshayesites tuarkyri- cus + D. weissi ammonite zones) and an Upper ?Late Bedou- lian (D. deshayesi + Dufrenoya furcata ammonite zones). The stratigraphy of the studied section is based on orbito- linid foraminifera (e.g., SCHROEDER, 1964, 1985; CHER- CHI & SCHROEDER, 1999; SCHROEDER et al., 2002) (Fig. 7a–f). Supporting data are available from dasyclada- lean algae (e.g., GRANIER & DELOFFRE, 1993; BUCUR, 1999) and other benthic foraminifera. The two biostrati- graphically most important taxa are Rectodictyoconus gigan- teus SCHROEDER (Fig. 7a–c) and Mesorbitolina texana (ROEMER) (Fig. 7d–f). R. giganteus was described by SCHROEDER (1964) from the Urgonian of Spain. Zone II with R. giganteus was considered to belong to the Barremian. Following Zone I with Palorbitolina lenticularis, (also char- acterizing Zone IV of SCHROEDER 1964), a Late Barremian age was originally assumed. In subsequent works, this age was corrected, with R. giganteus having its fi rst appearance (FAD) in the earliest Aptian (e.g., CHERCHI & SCHROEDER, 1999; SCHROEDER et al., 2002, fi g. 1; SCHROEDER et al. 2010, fi g. 3). The total taxon range should be restricted to the lowermost part of the Early Aptian (Bedoulian) (e.g., SCHRO- EDER, 1964, fi g. 1; SCHROEDER et al., 2010, fi g. 3). Re- viewing the literature, MASSE (2003), concluded that R. giganteus is a Bedoulian marker and that data from Spain sug- gests its essentially lower ?early Bedoulian range. The taxon range zone of Mesorbitolina texana is often indicated as Late Aptian (= Clansayesian) to Middle Albian (SCHROEDER, 1975, 1985; VELIĆ, 2007). A thorough analysis of different sections in Spain with orbitolinids, planktonic foraminifera and ammonites (CASTRO et al., 2002, fi g. 3) has shown, that M. texana reaches down to the upper part of the Gargasian within the Globigerinelloides algerianus planktonic fora- minifera zone (= upper part of the Parahoplites melchioris ammonite zone, compare Fig. 6 in ROPOLO et al., 2008). In a new biostratigraphic scheme of Barremian-Albian orbitoli- nids, the fi rst occurrence of Mesorbitolina texana is indicated as the middle part of the Gargasian (base of the P. melchioris ammonite zone) (SCHROEDER et al., 2010). Our results are partly in contradiction to the generally accepted stratigraphic considerations according to SCHROE- DER (1964), that R. giganteus and M. texana or also M. parva (Gargasian-Lowermost Clansayesian acc. to SCHRO- EDER et al., 2010), should not display overlapping ranges. In the studied section, the basal part, up to sample AL 972 only contains R. giganteus, followed by an interval (~ 17 m) where R. giganteus co-occurs with M. texana in the same thin-sections (AL 972 to AL 980) (see Fig. 4). As the two species occur as both isolated bioclasts, and within lithoclasts that have been contemporaneously resedimented, reworking Geologia Croatica 33 Schlagintweit et al.: Onset of an Aptian carbonate platform overlying a Middle-Late Jurassic radiolaritic-ophiolithic mélange in the Mirdita Zone of Albania Figure 4: Detailed section, biostratigraphy and micro- fauna and -fl ora content. Geologia Croatica 34 Geologia Croatica 65/1 Figure 5: Microfacies of the Aptian resediments. a – Wackestone with some litho- and bio-clasts (here: stromatoporoid skeleton), overlain by a close- packed mass-fl ow of stylo-breccia or diagenetic packstone habitus (sensu LOGAN & SEMENIUK 1976). Note the dark layer of styloreactate at the bound- ary. Sample A 3744. b – Wacke- to packstone containing globigerinid planktonic foraminifera (p) overlain by a grain- to rud-stone with bioclasts of cal- careous algae and metazoan skeletons. Sample A 3755-2. c – Packstone with incertae sedis Radiomura cautica SENOWBARI-DARYAN & SCHÄFER (Ra), Crescentiella morronensis (CRESECENTI), diverse bioclasts and tests of Rectodicytoconus giganteus SCHROEDER (Re). Sample A 3741. d – Mass-fl ow consist- ing of close-packed clasts containing dasycladalean algae and tests of Rectodictyoconus giganteus SCHROEDER (Re). Sample Al 976. e – Well washed-out packstone with dasycladalean algae, (D), Mesorbitolina texana (ROEMER) (M) and Rectodictyoconus giganteus SCHROEDER (Re). Sample A 3746-1. f – Mass- fl ow deposit with skeleton of the stromatoporoid Tubuliella rotunda TURNŠEK. Sample Al 990. For a scale bar is 5.0 mm; for b–f scale bar is 2.0 mm. Geologia Croatica 35 Schlagintweit et al.: Onset of an Aptian carbonate platform overlying a Middle-Late Jurassic radiolaritic-ophiolithic mélange in the Mirdita Zone of Albania Figure 6: Microproblematica (a–c), dasycladalean algae (d–h) and stromatoporoids (i–j) from the studied section. a) Crescentiella morronensis (CRESCEN- TI). Sample A 3741. b) Radiomura cautica SENOWBARI-DARYAN & SCHÄFER. Sample A 3741. c) Koskinobullina socialis CHERCHI & SCHROEDER. Sample A 3743. d) Acroporella radoicicae PRATURLON. Sample A 3741. f) Salpingoporella pygmaea (GÜMBEL). Sample A 3745. g) Linoporella sp. Sample A 3745. e, h) Steinmanniporella? parsica TAHERPOUR KHALIL ABAD et al. Sample A 3753. i Tubuliella rotunda TURNŠEK. Sample A 3744. j) Tubuliella fl uegeli TURNŠEK. Sample A 3748. For a, c–h scale bar is 0.5 mm; for b, i–j scale bar is 1.0 mm. Geologia Croatica 36 Geologia Croatica 65/1 Figure 7: Middle-Late Aptian Foraminifera from the studied section. a–c) Rectodictyoconus giganteus SCHROEDER. Note the centric embryonic appara- tus in c; subaxial section of Lenticulina sp. on the right. Samples A 3748, AL 976, A 3476. d–f) Mesorbitolina texana (ROEMER). Samples A 3753, AL 976, g–h) Planispial Globigerinelloides sp., comparable to section of G. algerianus in SLITER (1989, pl. 1/13). Samples A 3753, A 3752. i) Trochospiral globiger- inid foraminifer. Sample A 3753. j) Globigernid planktonic foraminifer (pf) and Sabaudia minuta (HOFKER) (S). Sample A 3753. For a–b, f scale bar is 1mm; for c–e, g–j scale bar is 0.5 mm. Geologia Croatica 37 Schlagintweit et al.: Onset of an Aptian carbonate platform overlying a Middle-Late Jurassic radiolaritic-ophiolithic mélange in the Mirdita Zone of Albania SON et al. (2011, fi g. 6/11), however, does not allow a con- clusion to be drawn in this respect. Therefore, this section could also belong to R. giganteus in accordance with our re- sults from northern Albania. According to HENSON (1948), the dimensions of Dictyoconus (= Montseciella) arabicus are: test diameter 2.4 to 3.2 mm and height 1.7 to 2.0 mm. For Rectodictyoconus giganteus SCHROEDER (1964) in- dicated a test diameter from 4-5 mm and height of 3-4 mm. Juvenile specimen of R. giganteus, clearly evidenced by the central embryo in our material (Fig. 7c, compare also Fig. 4a-4 in SCHROEDER et al., 2010), however falls into the dimensional range of M. arabica, so that the pure dimen- sional discrimination of both taxa remains ambiguous. The situation becomes more complicated as microspheric speci- mens of M. arabica may reach test diameters of up to 6 mm (Fig. 4b-7 in SCHROEDER et al., 2010). Another point to mention is the fact that no holotype has been indicated for R. giganteus in the original description. Another example refers to the paper of MARRONI et al. (2009), which deals with Early Cretaceous fl yschoid de- posits in northern Albania. These authors report the occur- rence of Paleodictyoconus arabicus (= Montseciella ara- bica) in turbidite deposits, assigning these, also based on calcareous nannoplankton data, to the Barremian. The fi g- ured oblique section of Paleodictyoconus arabicus in MAR- RONI et al. (2009, fi g. 6e) however, does not belong to this taxon. The typical vermicular structural elements in the cen- tral zone are absent, and this orbitolinid could be a fl at dis- coidal specimen of Mesorbitolina or Palorbitolina without allowing a species attribution, as the embryonic apparatus is not shown. In any case, a Barremian age based on this orbi- tolinid section alone is not possible; but we cannot comment on the nannofossil determination. A third example comes from the Vardar zone of Serbia, where “Paleodictyoconus arabicus” was reported by ZELIC et al. (2010, fi g. 5c). Fur- thermore, this oblique section of an orbitolinid foraminifer belongs to Palorbitolina or Mesorbitolina. Last but not least, an undetermined orbitolinid that we refer to as an oblique section of either M. arabica (HENSON) or R. giganteus SCHROEDER was fi gured by CARRAS et al. (2004: Pl. 1, Fig. F) from the Pelagonian Unit of Greece. It occurs in re- sedimented carbonates assigned to the Cenomanian, assuming of older material/clasts seems unlikely. The middle-upper part of the studied section contains only M. texana. Given these results (CASTRO et al., 2002; SCHROEDER et al., 2010), the stratigraphic range of R. giganteus must be en- larged, comprising at least the late Gargasian. An extension into the earliest Clansayesian seems possible. A possible rea- son that both taxa are clearly separated at the type-locality of R. giganteus might be related to a facies control, as its lat- est occurrence shows a distinct contemporaneous lithologi- cal change from limestones to marls/marly limestones (see fi g. 1 in SCHROEDER, 1964). In contrast to Mesorbitolina texana with its numerous records in the literature, Rectodic- tyonus giganteus represents a rather poorly known taxon, which may account for the limited knowledge of its strati- graphic distribution (see MASSE, 2003). Although determination of Globigerinelloides in thin- section is problematic (e.g., WEIDICH, 1990), we have to state that our specimens within an interval from sample A-3752 to A-3753 (Fig. 7g-h) are comparable to a section of G. algerianus illustrated by SLITER (1989, pl. 1/13). This species characterizes the G. algerianus zone (MOULLADE, 1966; SLITER, 1989; CASTRO et al., 2002). In summary, the studied section is of Aptian age, assumed to comprise parts of the Bedoulian (Early Aptian) and ranging into the Clansayesian (Late Aptian) (Fig. 8). Whether the top part stretches into the Early Albian is unknown. As only an 18 m thick sequence below the fi rst occurrence of Mesorbitolina texana exists, extension of the section into the Late Bar- remian is not very likely. The associated dasycladalean algae are also compatible with an Aptian age (e.g., BUCUR, 1999; TAHERPOUR KHALIL ABAD et al., 2010). It is worth mentioning that for the carbonate platforms overlying the ophiolites and cropping out in northern Alba- nia, an overall Late Barremian-Early Aptian age has been deduced from micropalaeontological investigations, namely the occurrence of Montseciella arabica (HENSON) (ROB- ERTSON et al., 2011, tab. 1). As stated by CHERCHI & SCHROEDER (1999, p. 13), Montseciella arabica “grades into Rectodictyoconus giganteus” during the basal Aptian. R. giganteus differs from M. arabica by “the centric position of the embryo and its generally larger test” (op. cit., p. 13). The oblique section of “M. arabica” shown by ROBERT- Figure 8: Stratigraphic framework of the studi- ed section (modifi ed after CASTRO et al., 2002). The fi rst appearance of Mesorbitolina texana (ROEMER) at the base of the melchioris ammo- nite zone refers to SCHROEDER et al. (2010). Geologia Croatica 38 Geologia Croatica 65/1 “an hiatus including the whole Early Cretaceous” (op. cit., p. 353). This situation generally mirrors the situation in Al- bania, where fi rstly a Late Jurassic carbonate platform over- lies the ophiolites, later followed by several emersion phases and at least a Late Cretaceous series. Whether the Early Cre- taceous orbitolinid in the Greek case study was reworked from older sediments or whether the age of the “Late Creta- ceous” series must be re-assessed is unknown. In conclusion, stratigraphic data obtained from orbitoli- nid foraminifera from sediments associated with Dinaric ophiolites reported in the literature, (with or without fi gura- tion), must be considered with caution, especially when these determinations are coupled with dating of tectonic or sedi- mentary events. 3. DISCUSSION AND CONCLUSIONS After the obduction of the Mirdita ophiolites onto the Apu- lian margin in early Late Jurassic times, subsequent shallow- water carbonates were formed overlying the ophiolite nap pes. The fi rst platform, of Kimmeridgian-Tithonian age (Kurb- nesh Platform), was eroded before the onset of the second platform in ?Late Berriasian times. The Late Jurassic plat- form can only be recognized by preserved Late Jurassic ba- sinal deposits (slope sediments) and their erosional products in earliest Cretaceous foreland basin fi lls (SCHLAGINT- WEIT et al., 2008). In-situ platform areas of Late Jurassic age overlying the ophiolites, are not preserved on top of the Mirdita ophiolites. In contrast, the second platform of ?Late Berriasian to Valanginian age (Munella Platform) is partly preserved in central Albania. However the type-locality, the Mali I Munelles, is highly sheared and the platform carbon- ates are imbricated (SCHLAGINTWEIT et al., 2006). Con- temporaneous coarse-grained foreland basin fi lls, contain clasts of the Munella Platform (SCHLAGINTWEIT et al., 2008). Both platforms were therefore formed under a tec- tonically active regime after ophiolite emplacement. After a period of erosion/omission until the Late Bar- remian, a new cycle of carbonate deposition began in the early Aptian, at the top of the deeply eroded Mirdita nappe pile and its overlying Late Jurassic and Early Cretaceous carbonate platforms. The formation of the Aptian Mali I Shenjtit carbonate platform most probably began in the Early Aptian and not in the Barremian as formerly estimated. In contrast to the older platforms, the sedimentary succession of this platform is not sheared and its layering is fl at. After formation of this platform, tectonic movement, most prob- ably the formation of a horst-and-graben structure, must have been established before deposition of the Late Cretaceous (rudist) limestones. The onset of the Mali I Shenjtit platform and the total thickness of the fl at lying shallow-water carbonates up-sec- tion, clearly demonstrate a fl ooding event, triggered more probably by eustatic sea-level changes rather than important tectonic movements. An important sea-level rise is known near the base of the Aptian (e.g., GRADSTEIN et al., 2004), followed by a regression near the end of the Aptian. This fi ts well with the age range of the Mali I Shenjtit platform, which does not extend beyond the Aptian. On basis of the analysis of the foreland basin fi lls and their generally recognizable fi ning-upward trend (e.g., BOR- TOLOTTI et al., 1996: “Firza Flysch”), as well as complete erosion of the oldest and the imbrication of the second plat- form, GAWLICK et al. (2008) considered a decrease in tec- tonic activity from the Late Jurassic to the Early Cretaceous. The fl at lying Aptian shallow-water carbonates fi t into the trend, that platform formation in Late Jurassic to Early Cre- taceous times become more and more controlled by sea-level fl uctuation rather than tectonic motion. This was recently confi rmed in general by ROBERTSON et al. (2011). The onset and demise of the Late Jurassic carbonate platforms after the emplacement of the ophiolite nappe stack in the Oxfordian refl ect a decrease in tectonic activity from the Kimmeridgian to the Aptian. Whereas the fi rst platform (Kimmeridian – Tithonian) was rapidly eroded after its for- mation, most probably as the result of the ongoing tectonic shortening, (compare SCHMID et al., 2008), and also docu- mented by thick foreland basin deposits, the second platform (?Late Berriasian-Valanginian) was formed in a tectonically active regime, but one of decreasing intensity. The younger sedimentary evolution refl ects deposition in a regime, which was more imprinted by eustatic sea-level fl uctuations than tectonics. The Aptian carbonate platform was formed in a phase of relative tectonic quiescence before a new tectonic cycle (?late Albian/Cenomanian) began. Only these younger tectonic motions – faulting and thrusting -, e.g. in meso-Cre- taceous, Palaeogene and/or Neogene times, affected this plat- form together with its underlying rocks. As a result of the pre-Late Cretaceous faulting, the Mali I Shenjtit platform become eroded over large areas and the ophiolites, particu- larly the ophiolite mélanges were overlain by early Late Cre- taceous rudist Limestones. ACKNOWLEDGEMENT The joint projects ‘‘Tectonothermal Evolution of the Al- banides 2003–2005’’ and “emplacement of the copper ore deposits 2006-2007” received fi nancial support from: Alba- nian Government (Geological Survey of Albania); Univer- sity of Leoben, University of Vienna, Austrian Academic Exchange Service, all Austria; University of Tübingen, Ger- many. The careful reviews of Ioan BUCUR (Cluj-Napoca) and Anonymus are gratefully acknowledged. The assistance with the English of Julie ROBSON is kindly acknowledged. REFERENCES BORTOLOTTI, V., KODRA, A., MARRONI, M., MUSTAFA, F., POLFI, L., PRINCIPI, G. & SACCANI, E. (1996): Geology and Petrology of ophiolite sequences in the Mirdita region (Northern Albania).– Ofi oliti, 21/1, 3–20. BUCUR, I.I. (1999): Stratigraphic signifi cance of some skeletal algae (Dasycladales, Caulerpales) of the Phanerozoic.– In: FARINACCI, A. & LORD, A.R. (eds.): Depositional Episodes and Bioevents. Palaeopelagos Spec. Pub., 2, 53–104. CARRAS, N., FAZZUOLI, M. & PHOTIADES, A. (2004): Transition from carbonate platform to pelagic deposition (Mid Jurassic-Late Cretaceous), Vourinos Massif, Northern Greece.– Riv. Ital. Paleont. Strat., 110/1, 345–355. Geologia Croatica 39 Schlagintweit et al.: Onset of an Aptian carbonate platform overlying a Middle-Late Jurassic radiolaritic-ophiolithic mélange in the Mirdita Zone of Albania CASTRO, J.M., COMPANY, M., DE GEA, G.A. & AGUADO, R. (2001): Biostratigraphy of the Aptian-Middle Cenomanian platform to ba- sin domain in the Prebetic Zone of Alicante, SE Spain: calibration between shallow water benthonic and pelagic scales.– Cret. Res., 22, 145–156. doi: 10.1006/cres.2000.0249. CHERCHI, A. & SCHROEDER, R. (1999): Montseciella, a new orbito- linid genus (Foraminiferida) from the uppermost Hauterivian – Ear- ly Barremian.– Treb. Mus. Geol. Barcelona, 8, 5–23. DILEK, Y., SHALLO, M. & FURNES, H. (2005): Rift-Drift, Seafl oor Spreading, and Subduction Tectonics of Albanian Ophiolites.– In- ternational Geology Review, 47, 147–176. doi: 10.2747/0020-6814. 47.2.147 GAWLICK, H.J., FRISCH, W., HOXHA, L., DUMITRICA, P., KRY- STYN, L., LEIN, R., MISSONI, S. & SCHLAGINTWEIT, F. (2008): Mirdita Zone ophiolites and associated sediments in Albania reveal Neotethys Ocean origin.– Int. J. Earth Sci., 97, 865–881. doi: 10.1007/ s00531-007-0193-z GAWLICK, H.-J., MISSONI, S., SCHLAGINTWEIT, F., SUZUKI, H., FRISCH, W., KRYSTYN, L., BLAU, J. & LEIN, R. (2009): Jurassic Tectonostratigraphy of the Austroalpine domain.– Journal of Alpine Geology, 50, 1–152. GRANIER, B. & DELOFFRE, R. (1993): Inventaire critique des algues dasycladales fossiles II Partie – les algues dasycladales du Jurassic- ssique et du Crétacé.– Rev. Paléobiol., 12, 19–65. LOGAN, B.W. & SEMENIUK, V. (1976): Dynamic metamorphism; processes and products in Devonian carbonate rocks, Canning Ba- sin, Western Australia.– Geol. Soc. Australia Spec. Pub., 16, 1–138. MARRONI, M., PANDOLFI, L., ONUZI, K., PALANDRI, S. & XHO- MO, A. (2009): Ophiolite-bearing Vermoshi fl ysch (Albanian Alps, Northern Albania): elements for its correlation in the frame of Di- naric-Hellenic belt.– Ofi oliti, 34/2, 95–108. MASSE, J.-P. (2003): Integrated stratigraphy of the Lower Aptian and applications to carbonate platforms: a state of the art.– In: GILI, H.N. & SKELTON, P.W. (eds.): North African Cretaceous carbon- ate platform systems, NATO Science Series, IV. Earth and Environ- mental Sciences, 28, 215–227, Kluwer Academic Publishers. MILAN, A. (1969): Faziesverhältnisse und Hydrozoenfauna des Malms im Küstenland des nördlichen Velebit und Velika Kapela.– Geol. vjesnik, 22 (1968), 201–219. MOULLADE, M. (1966): Étude stratigraphique et micropaléontologique du Crétacé inférieur de la « fosse Vocontienne ».– Doc. Lab. Géol. Fac. Sci. Lyon, 15, 1–369. NOWACK, E. (1928): Geologische Karte von Albanien 1:200.000.– Ver- lag Kartographisches Institut Wien. GRADSTEIN, F., OGG, J. & SMITH, A. (2004): A Geological Time Scale.– Cambridge University Press, Cambridge, 1–589. PEZA, L.H. & MARKU, D. (2002): Lower Cretaceous in the Munella Mountains (Mirdita Zone, northeastern Albania).– In: WAG- REICH, M. (ed.): Aspects of Cretaceous Stratigraphy and Palaeo- biogeography. Österr. Akad. Wiss., Schriftenr. Erdwiss. Komm., 15, 365–372. PEZA, L.H. & ZITT, J. (2002): Urgonian (Early Cretaceous) echinoids of the Mirdita Zone (Southeast Albania).– Geol. Carpath., 53/5, 327–332. ROBERTSON, A. & SHALLO, M. (2000): Mesozoic-Tertiary tectonic evolution of Albania in its regional Eastern Mediterranean context.– Tectonophysics, 316, 197–254. doi: http://dx.doi.org/10.1016/S0040- 1951(99)00262-0 ROBERTSON, A.H.F., IONESCU, C., HOECK, V., KOLLER, F., ONU- ZI, K., BUCUR, I.I. & GHEGA, D. (2011): Emplacement of the Jurassic Mirdita ophiolites (southern Albania): evidence from as- sociated clastic and carbonate sediments.– Int. J. Earth Sci. doi 10.1007/s00531-010-0603-5 ROPOLO, P., CONTE, G., MOULLADE, M., TRONCHETTI, G. & GONNET, R. (2008): The Douvilleiceratidae (Ammonoidea) of the Lower Aptian historical stratotype area at Cassis-Le Bédoule (SE France).– Carnets de Géologie Mem. 3 (CG2008_M03) SCHLAGINTWEIT, F., GAWLICK, H.J., MISSONI, S., LEIN, R. & HOXHA, L. (2006): Late Jurassic to Early Cretaceous dasycladales and benthonic foraminifera from the Munella carbonate platform s. l. of the Mirdita Zone (Albania).– In: SUDAR, M., ERCEGOVAC, M. & GRUBIC, A. (eds.): Proceedings XVIIIth Congress of Car- pathian-Balkan Geological Association), 527–530, (National com- mittee of the Carpathian - Balkan Geological Association; Serbian Geological Society) Belgrade. SCHLAGINTWEIT, F., GAWLICK, H.J., MISSONI, S., HOXHA, L., LEIN, R. & FRISCH, W. (2008): The eroded Late Jurassic Kurb- nesh carbonate platform in the Mirdita Ophiolite Zone of Albania and its bearing on the Jurassic orogeny of the Neotethys realm.– Swiss J. Geosci., 101, 125–138. doi: 10.1007/s00015-008-1254-4 SCHMID, S.M., BERNOULLI, D., FÜGENSCHUH, B., MATENCO, L., SCHEFER, S., SCHUSTER, R., TISCHLER, M. & USTASZEWS- KI, K. (2008): The Alpine-Carpathian-Dinaride-orogenic system: correlation and evolution of tectonic units.– Swiss J. Geosci. (Eclogae Geol. Helv.), 101, 139–183. doi: 10.1007/s00015-008-1247-3 SCHROEDER, R. (1964): Orbitoliniden-Biostratigraphie des Urgons nordöstlich von Teruel (Spanien).– N. Jb. Geol. Paläont. Mh., 1964, 462–472. SCHROEDER, R. (1975): General evolutionary trends in Orbitolinas.– Rev. esp. Micropaleont., num. spec., 117–128. SCHROEDER, R. (1985): Orbitolina (M.) texana (ROEMER, 1849).– In: SCHROEDER, R. & NEUMANN, M. (eds.): Les grands Fo- raminifères du Crétacé Moyen de la région Méditerranénne. Géo- bios Mém. Spéc., 7, 77–80. SCHROEDER, R., CLAVEL, B., CHERCHI, A., BUSNARDO, R., CHA- ROLLAIS, J. & DECROUEZ, D. (2002): Lignées phylétiques d´Orbitolinidés de l´intervalle Hauterivien supérieur – Aptien inférieur; leur importance stratigraphique.– Rev. Paléobiol., 21, 853–863. SCHROEDER, R., VAN BUCHEM, F.S.P., CHERCHI, A., BAGHBANI, D., VINCENT, B., IMMENHAUSER, A. & GRANIER, B. (2010): Revised orbitolinid biostratigraphic zonation for the Barremian – Aptian of the eastern Arabian Plate and implications for regional stratigraphic correlations.– GeoArabia Spec. Pub., 4, 49–96. SLITER, W.V. (1989): Biostratigraphic zonation for Cretaceous plank- tonic foraminifers examined in thin section.– J. Foramin. Res., 19, 1–19. doi: 10.2113/gsjfr.19.1.1 TAHERPOUR KHALIL ABAD, M., CONRAD, M.A., ARYAEI, A.A. & ASHOURI, A.R. (2010): Barremian-Aptian Dasycladalean algae, new and revisited, from the Tigran Formation in the Kopet Dagh, NE Iran.– Carnets de Géologie – Notebooks on Geology, Article 2010/05 (CG2010_A05) TURNŠEK, D. (1966): Upper Jurassic hydrozoan fauna from southern Slovenia.– Razprave Razr. SAZU, 9, 335–428. TURNŠEK, D. (1969): A contribution to the palaeoecology of Jurassic Hydrozoa from Slovenia.– Razprave Razr. SAZU, 12, 209–237. TURNŠEK, D., BUSER, S. & OGORELEC, B. (1981): An Upper Jurassic reef complex from Slovenia, Yugoslavia.– SEPM Spec. Pub., 30, 361–169. VELIĆ, I. (2007): Stratigraphy and palaeobiogeography of Mesozoic benthic foraminifera of the Karst Dinarides (SE Europe).– Geol. Croat., 60, 1–113. WEIDICH, K.F. (1990): Die kalkalpine Unterkreide und ihre Foramini- ferenfauna.– Zitteliana, 17, 1–312. XHOMO, A., KODRA, A., DIMO, Ll., XHAFA, Z., NAZAJ, SH., NA- KUÇI, V., YZEIRAJ, D., LULA, F., SADUSHI, P., SHALLO, M., Geologia Croatica 40 Geologia Croatica 65/1 VRANAJ, A. & MELO, V. (2002): Harta gjeologjike e Shqiperise, Geological map of Albania, scale 1:200,000, published by the Min- istry of Industry and Energy, Republic of Albania. ZELIC, M., MARRONI, M., PANDOLFI, L. & TRIVIĆ, B. (2010): Tec- tonic setting of the Vardar suture zone (Dinaric-Hellenic belt): the example of the Kopaonik area (southern Serbia).– Ofi oliti, 35/1, 49–69. Manuscript received May 04, 2011 Revised manuscript accepted November 15, 2011 Available online February 25, 2012