Annales Societatis Geologorum Poloniae (2016), vol. 86: 165–183. doi: http://dx.doi.org/10.14241/asgp.2016.005

DEPOSITIONAL ENVIRONMENTS, FACIES AND DIAGENESIS OF THE UPPER –LOWER CARBONATE DEPOSITS OF THE BUILA-VÂNTURARIÞA MASSIF, SOUTHERN CARPATHIANS (ROMANIA)

George PLEª, Ioan I. BUCUR & Emanoil SÃSÃRAN

Department of Geology, Babeº-Bolyai University, M. Kogãlniceanu 1, 400084 Cluj-Napoca, Romania; e-mails: [email protected]; [email protected]; [email protected]

Pleº, G., Bucur, I. I. & Sãsãran, E., 2016. Depositional environments, facies and diagenesis of the Upper Jurassic–Lower Cretaceous carbonate deposits of the Buila-Vânturariþa Massif, Southern Carpathians (Romania). Annales Societatis Geologorum Poloniae, 86: 165–183.

Abstract: The Buila-Vânturariþa Massif consists of massive Upper Jurassic reef limestones (Kimmeridgian– Tithonian) and Lower Cretaceous (Berriasian–Valanginian, and Barremian–?Lower Aptian) deposits. Besides corals and stromatoporoids, a wide range of micro-encrusters and microbialites has contributed to their deve- lopment. In this study, the authors describe briefly and interpret the main facies associations and present the microfossil assemblages that are important for age determination. The distribution of facies associations, corro- borated with the micropalaeontological content and early diagenetic features, indicate different depositional environments. The carbonate successions show the evolution of the Late Jurassic–Early Cretaceous depositional environments from slope and reef-front to internal-platform sedimentary settings, including peritidal environ- ments in the lowermost Cretaceous. Early diagenesis, represented by synsedimentary cementation in the form of micritization (including cement crusts in the reef microframework), followed by dissolution, cementation and dolomitization in a meteoric regime, and void-filling late cementation during the burial stage.

Key words: Carbonate platforms, reefs, microfacies, micro-encrusters, carbonate diagenesis, Upper Jurassic, lowermost Cretaceous, Southern Carpathians, Romania.

Manuscript received 9 February 2015, accepted 14 April 2016

INTRODUCTION

The Buila-Vânturariþa Massif, located in the central- ªerban et al., 2004; Bucur and Sãsãran, 2005; Sãsãran, northern part of Vâlcea County, Romania, is part of the 2006; Ivanova et al., 2008; Pleº et al., 2013; Sãsãran et al., Cãpãþânii Mountains, central Southern Carpathians (Fig. 1). 2014; Ko³odziej, 2015a, b and literature therein), and as Its lithology, geological history and geomorphology are “Plassen”-type limestones in the Alps (e.g., Schlagintweit unique by comparison with the features of the main moun- and Gawlick, 2008; Schlagintweit et al., 2005). The term tain chain in the Capãþânii Mountains. The Buila-Vântura- “Štramberk”-type limestones was even recently applied to riþa Massif consists of a 12-km-long and 0.5- to 2-km-wide, limestones in Turkey (Masse et al., 2015). In many occur- linear, calcareous crest, mainly built of Jurassic limestones. rences, as is also the case with the Buila-Vânturariþa Massif, It is a fragment of the carbonate sedimentary system, known the reef limestones are conformably overlain by lowermost as the Getic Carbonate Platform (Sãndulescu, 1984), which Cretaceous (Berriasian–Valanginian) stratified limestones, covered the Getic-Supragetic domain during the Late Juras- followed by transgressive Urgonian limestones, Barre- sic–Early Cretaceous. The outline and NNE–SSW orienta- mian–Lower Aptian in age (Dragastan, 2010; Pleº et al., tion of the morphology of the main Buila-Vânturariþa crest 2013; Mircescu et al., 2014; Pleº and Schlagintweit, 2014). are similar to those of the Piatra Craiului Massif, another The aim of this paper is the identification and interpretation part of the Getic Carbonate Platform, located more to the of the main microfacies types, micropalaeontological as- east. The studied massif is dominated by Kimmeridgian– semblages and diagenetic processes that affected these Tithonian reef limestones. Synchronous limestones of other limestones, in order to reconstruct their depositional envi- areas in the Tethys realm are known as “Štramberk”-type ronments. limestones in the Carpathians (see Uþã and Bucur, 2003; 166 G. PLEª ET AL. , 1978). et al. Geological map of the Buila-Vânturariþa Massif (modified after Lupu Fig. 1. UPPER JURASSIC–LOWER CRETACEOUS CARBONATE DEPOSITS, ROMANIA 167

GEOLOGICAL SETTING

The Buila-Vânturariþa Massif is part of the former Getic Nappe, a structural unit within the Median Dacides, in the Southern Carpathians (Sãndulescu, 1984). In this massif, post- sedimentary deposits are mainly represented by –Oxfordian detrital and siliciclastic rocks, overlain by Kimmeridgian–lowermost Cretaceous reef lime- stones (Fig. 1). Boldur et al. (1968) identified de- posits in the south-eastern area. The Bajocian age is sup- ported by the assemblages of ostreids, Phylloceratidae ammonites, and bivalve species of Entolium Meek, 1865 and Camptochlamys Arkell, 1930 (Dragastan, 2010). Bathonian deposits are present in smaller areas in the Buila-Vânturariþa Massif and are often associated with Lower Callovian ones. Boldur et al. (1968) identified specimens of Oecotraustes sp. in a horizon of calcareous sandstones in the Bistriþa Val- ley, indicating the presence of Bathonian–Callovian rocks within the succession. Boldur et al. (1968, 1970) identified Callovian deposits in the central-western part of the massif, in the Bistriþa and Costeºti valleys, as well as south of Stogu Peak. These authors have described the following lithologi- cal succession for the Bathonian–Callovian: micaceous cal- careous sandstones with Oecotraustes (Upper Bathonian– Lower Callovian); reddish and yellowish micaceous calcar- eous sandstones with Grossouvria curvicosta (Oppel, 1857) and G. subtilis (Neumayr, 1871), and sandy limestones with Fig. 2. Location of the sections studied. Bositra buchi (Roemer, 1836) and Phylloceras sp. (Middle– Upper Callovian). Sediments assigned to the Oxfordian oc- cur across relatively larger areas compared to the Middle Ju- intra-Tethys domain. In this region, lowermost Cretaceous rassic equivalents. They were grouped into the Buila and (Berriasian–Valanginian) sediments cover small areas; they Bistriþa members (Dragastan, 2010), two lithological units are overlain transgressively by Urgonian limestones (Dra- that are difficult to discriminate in outcrop. From the first gastan, 1980; Uþã and Bucur, 2003). Dragastan (1980, studies concerning the Jurassic deposits in this massif, it 2010) identified the following micro-organisms as charac- was assumed that Oxfordian deposits were present at the terizing the Berriasian–Valanginian interval: foraminifera base of the reef limestones, as limestones with siliceous [Mohlerina basiliensis (Mohler, 1938), Andersenolina nodules. Boldur et al. (1968) assigned the succession of red, elongata (Leupold, 1935), A. alpina (Leupold, 1935),A. marly limestones and pink limestones with layers of reddish delphinensis (Arnaud-Vanneau, Boisseau et Darsac, 1988), jasper to the Oxfordian. Nevertheless, the associations de- Mayncina bulgarica ng1033 Laug, Peybernes et Rey, 1980, scribed in these deposits by Dragastan (2010) show a wider and Kaminskia acuta Neagu, 1999], calcareous algae [Sal- stratigraphic distribution, including the Kimmeridgian– pingoporella annulata Carozzi, 1953, Rajkaella iailensis Tithonian interval. As a consequence, the presence of the (Maslov, 1965), Macroporella praturloni Dragastan, 1978, Oxfordian in the white limestones succession is still uncon- Actinoporella podolica (Alth, 1878), Felixporidium atana- firmed. The Kimmeridgian–Tithonian deposits, consisting siui Dragastan, 1999, Fagetiella angulata Dragastan, 1988] of massive reef limestones with thicknesses sometimes ex- and micro-encrusting organisms. Dragastan (2010) consid- ceeding 300 m, dominate the calcareous succession of the ered that Hauterivian deposits also should be present within Buila-Vânturariþa Massif, making up the main crest. They the Lower Cretaceous deposits of the Buila-Vânturariþa contain a rich micropalaeontological fossil suite. Pleº et al. Massif. In the opinion of the present authors, the foramini- (2013) identified the following main species of micro-or- feral assemblage including Haplophragmoides joukowskyi ganisms in microbial crusts and encrusting microbial organ- Charollais, Bronnimann et Zaninetti, 1966, Neotrocholina isms: Crescentiella morronensis Crescenti, 1969, Radio- sp., Patellina turriculata Dieni et Massari, 1966, Ander- mura cautica Senowbari-Daryan et Schäfer, 1979, Koskino- senolina histeri Neagu, 1994 and Kaminskia exigua Neagu, bullina socialis Cherchi et Schroeder, 1979, Iberopora 1999 cannot be considered to be typical for the Hauterivian bodeuri Granier et Berthou, 2002, Bacinella-type structures thus, its presence in the succession leaves questions about and/or Lithocodium aggregatum Elliott, 1956. The micro- the correctness of the stratigraphy. Uþã and Bucur (2003) bial structures and the encrusting organisms were essential confirmed the presence of Barremian–?Lower Aptian in the for the development of these bioconstructions. Pleº et al. area, based on the occurrence of the species Vercorsella (2013) defined the latter as “coral-microbial-microencruster hensoni (Dalbiez, 1958), Vercorsella camposaurii (Sartoni boundstones”. They are similar to the Upper Jurassic–low- et Crescenti, 1962), Charentia sp., Everticycla- mmina sp. ermost Cretaceous carbonate deposits of other regions in the and Falsolikanella danilovae Radoièiæ, 1969. In the north- 168 G. PLEª ET AL.

eastern part of the massif, Upper Cretaceous deposits lie Bucur et al. (1995), Bulot et al. (1997), Ko³odziej and De- transgressively and unconformably on top of the Upper Ju- crouez (1997); Ivanova (1999), Moshammer and Schlag- rassic–Lower Cretaceous limestones (Todiriþã- Mihãilescu, intweit (1999), Schlagintweit and Ebli (1999), Schroeder et 1973). Within these deposits, Boldur et al. (1970) recog- al. (2000), Pop and Bucur (2001), Radoièiæ (2005), Draga- nized three individual sedimentary complexes: Vraconian– stan (2010), Bucur et al. (2014a, b, c) and Mircescu et al. Cenomanian–Turonian, Coniacian–Santonian, and Campa- (2014). nian–Maastrichtian. Mesozoic deposits are covered by trans- In some areas within the Buila-Vânturariþa Massif (Ar- gressive Eocene sedimentary rocks (Popescu, 1954). nota Mountain, Costesti Gorges, Cacova Mountain, Albu Mountain, ªtevioara sector and Curmãtura Oale) the au- thors identified limestones that transgressively overlie the MATERIAL AND METHODS Upper Jurassic–lowermost Cretaceous. In such deposits the authors have identified specimens of Paracoskinolina? The authors collected 1,250 samples from profiles in jourdanensis Foury et Moullade, 1966 and Vercorsella eight different areas in the Buila-Vânturariþa Massif: P1 – camposaurii. Dragastan (1980), and Uþã and Bucur (2003) Bistriþa Gorges; P2 – Arnota Mountain; P3 – Costeºti Gor- also found Vercorsella hensoni, Paracoskinolina sp., Ever- ges; P4 – Cacova sector; P5 – Albu Mountain; P6 – ªtevio- ticyclammina sp., Salpingoporella muehlbergii (Lorenz, ara sector; P7 – Curmãtura Oale, and P8 – Cheii Gorges 1902), Falsolikanella danilovae, as well as rudist frag- (Fig. 2). The sampling procedure was established on the ba- ments. On the basis of this association, the deposits on top sis of local features in each of the profiles/transects. In most of the Upper Jurassic–lowermost Cretaceous succession cases, the profiles run along valley bottoms, where the car- were assigned by Dragastan (1980), and Uþã and Bucur bonate deposits are well-exposed. From these samples, the (2003) to the Barremian–?Lower Aptian interval. Similar authors prepared 1,270 thin sections for petrographic analy- associations were described elsewhere (Bucur et al., 1993; sis and the study of microfacies and diagenetic processes. Bodrogi et al., 1994; Turi et al., 2011; Lazãr et al., 2012; Michetiuc et al., 2012; or Bruchental et al., 2014).

AGE CONSTRAINTS FACIES AND MICROFACIES ANALYSIS Reef-type deposits were found in all eight profiles, making up the most significant calcareous succession in the The authors identified five major microfacies associa- Buila-Vânturariþa Massif. The most important microfossils tions (MFA), three in the Upper Jurassic (MFA1, MFA2, for biostratigraphy (Table 1) led the authors to assign a MFA3) and two in the Lower Cretaceous (MFA4 and Kimmeridgian–Tithonian age to the sequence, on the basis MFA5) deposits, respectively (Figs 3, 4). of the association of foraminifera and calcareous algae [Sal- pingoporella pygmaea (Gümbel, 1891), Clypeina sulcata MFA1 – Fine bioclastic grainstone/packstone (Alth, 1881), Nipponophycus ramosus Yabe et Toyama, 1928, Coscinoconus alpinus Leupold, 1935, Mohlerina ba- This facies was identified on Albu Mountain (P5), in siliensis] that are typical for Upper Jurassic carbonate-plat- the ªtevioara sector (P6) and in the Curmãtura Oale profile form facies in many European regions (Dragastan, 1975; (P7). In the Albu Mountain area (P5), MFA1 is represented Bucur, 1978; Ko³odziej and Decrouez, 1997; Carras and mostly by fine bioclastic grainstones and packstones with Georgala, 1998; Krajewski, 2000; Uþã and Bucur, 2003; small fragments of echinoids, calcified sponges, foramini- Olivier et al., 2004; Bucur and Sãsãran, 2005; Sãsãran, fera and Crescentiella morronensis. In the ªtevioara sector 2006; Catincuþ et al., 2010; Ivanova and Ko³odziej, 2010; (P6), such deposits dominate the lower half of the carbonate Rusciadelli et al., 2011; Turi et al., 2011; Pleº et al., 2013; succession and they are represented by fine-grained, bio- Pleº and Schlagintweit, 2014). clastic limestones with peloids, foraminifera and Cresce- The carbonate deposits overlying the reef limestones ntiella morronensis. In the well-sorted deposits, the authors include a micropalaeontological association composed of identified the following microfacies types: fine, bioclastic- Coscinoconus delphinensis (Arnaud-Vanneau, Boisseau et peloidal grainstone; bioclastic packstone/grainstone with thin Darsac, 1988), Montsalevia salevensis (Charrolais, Brönni- microbial crusts; and bioclastic packstone with small frag- mann et Zaninetti, 1987), Protopeneroplis ultragranulata ments of bioconstructing organisms (sclerosponges or en- (Gorbatchik, 1971), Charentia evoluta (Gorbatchik, 1968) crusting micro-organisms). The abundance of microbial lam- and Bacinella-type structures. To these, Dragastan (1980) inated crusts in these limestones is noteworthy. In the Curma- added Salpingoporella annulata, Rajkaella iailensis, Ma- tura Oale profile (P7), the fine-grained microfacies types croporella praturloni, and Actinoporella podolica. The en- (MFA1) also occurs in the lower part of the succession, as tire micropalaeontological association is typical for lower- interlayers within coarser deposits. These limestones have si- most Cretaceous (Berriasian–Valanginian) rocks, as it also milar characteristics to the ones previously described: well sor- has been recognised in other areas within the facies types ted, microbial content, fragments of corals and encrusting mi- assigned to this stratigraphic interval, for example, in the cro-organisms. The main MFA1 microfacies types in this pro- Romanian Carpathians, the Haþeg-Pui and Braºov-Dâm- file are represented by fine, bioclastic grainstone with forami- bovicioara-Piatra Craiului areas, and in other areas of the nifera, peloids or Crescentiella-type structures and bioclastic Tethyan domain by Bucur (1993), Chiocchini et al. (1994), packstone with fragments of sclerosponges and echinoids. UPPER JURASSIC–LOWER CRETACEOUS CARBONATE DEPOSITS, ROMANIA 169 . General succession of the limestone deposits of the Buila-Vânturariþa Massif (sections P1 to P4). Fig. 3 170 G. PLEª ET AL. e Buila-Vânturariþa Massif (sections P5 to P8). General succession of the limestone deposits of th Fig. 4. UPPER JURASSIC–LOWER CRETACEOUS CARBONATE DEPOSITS, ROMANIA 171 Table 1 Main Upper Jurassic–Lower Cretaceous microfossils of the Buila-Vânturariþa Massif and their stratigraphic range 172 G. PLEª ET AL. UPPER JURASSIC–LOWER CRETACEOUS CARBONATE DEPOSITS, ROMANIA 173

Interpretation fied the following microfacies types: intra-bioclastic float- Most probably, the fine-grained facies types (MFA1), stone, bio-intraclastic rudstone, and less frequently, bio- identified in the three sections, are the results of moderate clastic grainstone. In the Costeºti Gorges (P3), rudstone lev- and concentrated density flows (turbiditic deposits). The els (MFA2) are very thick; they were mainly observed in the clasts originated in the reef area and were probably depos- lower and middle part of the profile. Facies assigned to the ited in the lower part of the reef slope. In some cases, they MFA2 type dominate the upper half of the Cacova sector are associated with deposits showing MFA2 and MFA3 fa- succession (P4) and Albu Mountain (P5), consisting of cies types. On the basis of their association with reef-slope coarse grainstone and bioclastic rudstone with fragments of rudstones (MFA2), these deposits can be assigned to the reef macro-organisms. In the ªtevioara (P6) and Curmãtura “slope carbonate apron” model defined by Mullins and Oale (P7) sectors, the coarse deposits (MFA2) are found in Cook (1986). Comparable microfacies types were docu- the middle part of the succession. The main biota present in mented by Bucur et al. (2010a) in the Upper Jurassic car- these microfacies types consist of organisms related to the bonate deposits of the Mateiaº area, indicating similar depo- reef, represented by fragments of corals and sclerosponges, sitional environments. microproblematic organisms (Crescentiella morronensis, Lithocodium aggregatum or Bacinella-type micro-organ- isms), benthic foraminifera, as well as some molluscs (gas- MFA2 – Coarse bioclastic-intraclastic tropods or fragments of bivalves). In the lower and middle grainstone/rudstone part of the Cheia Valley succession (P8), coarse deposits of This microfacies type is commonly recognized throu- MFA2 dominate. ghout the entire carbonate succession in the Buila-Vântu- rariþa Massif, in all eight sections studied. In the Bistriþa Interpretation Gorges (P1) it consists mainly of reef debris levels ubiqui- The MFA2-type deposits are significantly thick and tous throughout the entire succession, showing tabular and they consist of poorly-sorted angular clasts represented by layer-like geometries (Pleº et al., 2013). The microfacies intraclasts and bioclastic fragments. Constant wave action are intra-bioclastic rudstone and coarse, intra-bioclastic and currents caused erosion during reef growth, so many grainstone. These limestones are mainly composed of coral fragments were redeposited and incorporated within these fragments, sclerosponges and large intraclasts of coral-mi- rudstones (Turnšek et al., 1981). Resedimentation of the crobial boundstone, stromatolitic-thrombolitic microbial reef clasts can be linked to small debris flows in an upper crusts and bioclastic packstone with Crescentiella morro- slope environment (Morsilli and Bosellini, 1997). The en- nensis. Clasts are angular to subangular and variable in size crusting nature of many of the micro-organisms, associated (up to 1.5 cm in diameter). The deposits are poorly sorted, with syndepositional cement crusts, have stabilized and re- with a chaotic orientation of clasts. These limestones con- inforced these slope carbonates. The reef debris deposits tain a micropalaeontological association of foraminifera (MFA2) in association with coral-stromatoporoid-micro- [Charentia evoluta, Lituola? baculiformis Schlagintweit et encruster boundstones (MFA3) are interpreted as an equiva- Gawlick, 2009, Mohlerina basiliensis (Fig. 5B), Coscinoco- lent of the fore-reef/upper-slope “Plassen”-type limestones, nus alpinus, C. delphinensis (Fig. 5A), Troglotella incru- described by Schlagintweit and Gawlick (2008) from the stans Wernli et Fookes, 1992, Bullopora laevis Sollas, Northern Calcareous Alps. They also resemble the plat- 1877, Lenticulina sp. (Fig. 5C), Coscinophragmaain sp. form-margin Ellipsactinia facies of the Central Apennines (Fig. 5D), Ammobaculites sp.)], calcareous algae [Clypeina (Rusciadelli et al., 2011), characterized by similar sedimen- sulcata (Fig. 5J), Salpingoporella pygmaea (Fig. 5H), tary settings. Other close facies associations have been de- Thaumatoporella parvovesiculifera (Ranieri, 1927), Nippo- scribed from several areas of the Romanian Carpathians nophycus ramosus (Fig. 5I), “Solenopora” sp.), sclero- (Bucur, 1978; Bucur and Sãsãran, 2005; Bucur et al., sponges (Perturbatacrusta leini Schlagintweit et Gawlick, 2010a, b; Bucur and Sãsãran, 2012). 2011, Murania reitneri Schlagintweit, 2004, Neuropora lusitanica Termier et Termier, 1985, Thalamopora lusita- MFA3 – Coral-stromatoporoid-microencruster nica Termier et Termier, 1985 (Fig. 5K), Calcistella jachen- boundstone hausenensis Reitner, 1992), gastropods, bivalves and worm tubes (Mercierella dacica Dragastan, 1967 and Terebella In the Bistriþa Gorges profile (P1), boundstone levels sp.). In the Arnota Mountain profile (P2), the authors identi- (MFA3) occur as interlayers in the lower and upper part of

Fig. 5. Main Upper Jurassic–Lower Cretaceous microfossils of the Buila-Vânturariþa Massif. A. Coscinoconus delphinensis (sample 794 – Valea Cheii Gorges – P8). B. Mohlerina basiliensis (sample 1053 – ªtevioara sector – P6). C. Lenticulina sp. (sample 38 – Bistriþei Gorges – P1). D. Coscinophragma sp. (sample 1040 – ªtevioara sector – P6). E. Protopeneroplis ultragranulata (sample 879 – Curmãtura Oale – P7). F. Vercorsella camposaurii (sample 890 – Curmãtura Oale – P7). G. Paracoskinolina? jourdanensis (sample 457 – Costeºti Gorges – P3). H. Salpingoporella pygmaea (sample 1054 – Valea Cheii Gorges – P8). I. Nipponophycus ramosus (sample 472 – Costeºti Gorges – P3). J. Clypeina sulcata (sample 1054 – ªtevioara sector – P6). K. Thalamopora lusitanica (sample 19b – Bistriþei Gorges – P1). L. Ellipsactinia sp. (sample 114 – Bistriþei Gorges – P1). 174 G. PLEª ET AL.

the succession, on top of the intraclastic-bioclastic rudstone/ sented by leiolitic microstructures, as well as fine-laminated grainstone facies types (MFA2). The corals and sponges are mesostructures. intensely encrusted by problematic micro-organisms (Cres- centiella morronensis, Radiomura cautica, Koskinobullina Interpretation socialis, Lithocodium aggregatum, Iberopora bodeuri,or The bioconstruction levels (MFA3) from the Buila- Bacinella-type structures). Additionally, the authors identi- Vânturariþa Massif are generally characterized by crustose fied stromatolitic- and thrombolitic-type structures. Peloids, and encrusting fabrics, associated with widely developed bioclasts and silt-sized carbonate intraclasts embedded in cement crusts. The intrareef sediment of MFA3-type depos- stromatolitic crusts were recognized. Other organisms are its is mud-dominated, represented by bioclastic wackestone represented by stromatoporoids (Ellipsactinia sp., Calci- with various reef organisms, such as fragments of corals and stella jachenhausenensis), ?udoteacean algae (Nipponophy- sclerosponges, foraminifera, calcareous algae (Salpingopo- cus ramosus), dasycladales (Salpingoporella pygmaea), rella pygmaea and/or Nipponophycus ramosus), as well as benthic foraminifera (Lituola? baculiformis, Mohlerina encrusting micro-organisms or clotted microbial structures. basiliensis, Coscinoconus alpinus, Troglotella incrustans, The micro- and macropalaeontological assemblages from Lenticulina sp., Coscinophragma sp.), molluscs, echinoid the MFA3 deposits, represent a typical frontal reef or reef- fragments and spines, or worm tubes (including Terebella crest association, as previously documented by Morsilli and sp.). An important feature of the bioconstructed limestones Bosellini (1997), Schlagintweit and Gawlick (2008) or Pleº from Bistriþa Gorges is represented by the presence of Epi- et al. (2013). The abundance of calcareous sponges [Per- phyton-type micro-organisms. These were recently identi- turbatacrusta leini, Ellipsactinia sp. (Fig. 5L), Neuropora fied for the first time in the Upper Jurassic limestones (Kim- lusitanica, Thalamopora lusitanica or Cylicopsis verticalis meridgian–Tithonian) in Romania (Sãsãran et al., 2014). In Turnšek, 1968], makes possible the correlation of the ana- the Arnota Mountain profile (P2) MFA3 is less frequent. lysed boundstones (MFA3) with bioconstructions of the The main micro-encrusters involved in the development and stromatoporoid zones from many Late Jurassic barrier-reef consolidation of this deposit are Lithocodium aggregatum models of the intra-Tethys domain. Thus, the MFA3 micro- and Crescentiella morronensis. MFA3-type boundstones facies association may correspond to the “Stromatopores were mainly observed in the lower half of the Costeºti Unit” of Rusciadelli et al., (2011) from the external zone Gorges section (P3), interlayered with MFA2-type deposits. (upper slope-reef crest transition) of the Marsica area reef They consist of coral-microencruster boundstones with in- (Central Apennines), characterized by abundant stromato- ternal wackestone/packstone sediment and boundstones poroids (Ellipsactinia Limestones). MFA3-type deposits with stromatoporoids and encrusting organisms. In the Ca- also resemble facies associations 4 and 5 (boundstones and cova sector (P4) the boundstone levels (MFA3) are thin and coarse grainstones with Ellipsactinia or Sphaeractinia)of were observed only at the base and the top of the succes- Morsilli and Bosellini (1997), and with the Actinostromaria sion. The most representative facies types consist of coral- Zone described by Turnšek et al. (1981) from Slovenia. microbial boundstones with thrombolitic crusts and stroma- toporoids and brecciated boundstones with problematic MFA4 – Peritidal bioclastic-oncoidal-peloidal micro-organisms (Crescentiella morronensis). In the ªtevio- wackestone ara profile (P6), a horizon of coral-microbial boundstone with stromatoporoids (MFA3) conformably overlies the fine- This microfacies association was assigned to the lower- grained deposits (MFA1). Here, the following microfacies most Cretaceous. They have been identified only in the pro- types occur: coral-microbial boundstone and boundstone files in the Arnota Mountain (P2), Cacova (P4), ªtevioara with stromatoporoids (Ellipsactinia sp., Calcistella jachen- (P6), Curmãtura Oale (P7) sectors, and Cheia Valley (P8), hausenensis, Neuropora lusitanica or Actinostromaria sp.) where they are developed conformably on top of the Juras- and micro-encrusters. MFA3 is present along the entire suc- sic reef limestones. For example, in the profile at Arnota cession in the Curmãtura Oale profile (P7), as interlayers Mountain (P2), the peloidal-bioclastic wackestones and the within bio-intraclastic rudstones (MFA2) and micritic fenestral-microbial bindstones represent the main microfa- fenestral deposits (belonging to MFA4). Boundstones dom- cies (MFA4) the top of the profile. In the Cacova (P4) and inate the lower part of the profile as banks of various thick- ªtevioara (P6) sectors, MFA4 includes the following micro- nesses. The dominant microfacies type is coral-microbial facies: peloidal wackestones with fenestrae, bioclastic-pe- framestone and boundstone with stromatoporoids and mi- loidal wackestones with micritized rivulariacean-type cya- crobial crusts. Only sporadically, leiolitic or stromatolitic nobacteria (?Cayeuxia sp.), peloidal-intraclastic wackesto- structures were noticed. In the Cheii Valley profile (P8), the nes, fenestral wackestones, and bioclastic-peloidal pack- deposits that the authors assigned to MFA3 occur solely at stones. Foraminifera [Protopeneroplis ultragranulata (Fig. the end of the lower part of the profile. They are represented 5E) or Montsalevia salevensis], cyanobacteria, crustacean by coral-microbial and pure, microbial boundstone. Micro- coprolites (Favreina sp.) and Bacinella-type structures rep- scopically, as opposed to most of the MFA2- and MFA3-type resent the main biotic components. In the upper part of the limestone samples investigated in the region, thin sections Curmãtura Oale profile (P7) the authors identified microbial from Cheii Valley (P8) show lesser amounts of microbial limestones with fenestrae, which we also assigned to the crusts. Crustiform fabrics associated with various encrust- MFA4. These are associated with (or, towards the top gradu- ing micro-organisms are rare, while boundstones with stro- ally pass into) bioclastic fenestral wackestone, peloidal bio- matoporoids are absent. The microbial structures are repre- clastic wackestone/packstone and non-fossiliferous mud- UPPER JURASSIC–LOWER CRETACEOUS CARBONATE DEPOSITS, ROMANIA 175 C. Bioclastic E. Bioclastic float- D. Crescentiella morronensis (sample 657 – Albu Mountain – P5). le 548 – Costeºti Gorges – P3). Fine bioclastic-peloidal grainstone with A. es and echinoid fragments (MFA2) -type structures (MFA3) (sample 489 – Costeºti Gorges – P3). Crescentiella and tinct micritic envelopes surrounding the cyanobacteria fragments (samp Perturbatacrusta leini , e carbonate succession of the Buila-Vânturariþa Massif. Coarse intraclastic-bioclastic rudstone with microbial structur Neuropora lusitanica B. Distribution of the main facies associations within th packstone with foraminifera (MFA5) (sample 889 – Curmãtura Oale – P7). (MFA1) (sample 778 – Albu Mountain – P5). Stromatoporoid-microencruster boundstone with stone with rivulariacean-type cyanobacteria oncoids (MFA4); note the dis Fig. 6. 176 G. PLEª ET AL. UPPER JURASSIC–LOWER CRETACEOUS CARBONATE DEPOSITS, ROMANIA 177

stone. In the carbonate succession from Cheii Valley, the fol- deposits assigned to MFA5 crop out in small areas on top of lowing microfacies occur: peloidal-bioclastic wackestone with the successions in Albu Mountain (P5), ªtevioara (P6) and cyanobacteria and micritic envelopes; bioclastic wackestone Curmãtura Oale (P7) sectors. Here, fossils are relatively with fractures and cement-filled cavities; fractured mudstone, scarce, the main bioclasts being represented by benthic fora- and brecciated peloidal-intraclastic wackestone. Here, the bio- minifera. Microfacies types are: bioclastic peloidal wacke- tic component is represented by foraminifera, microbialites, as stone with foraminifera, bioclastic microbial wackestone well as species of green algae (Clypeina sulcata). and fractured bioclastic packstone.

Interpretation Interpretation The facies types assigned to MFA4 are present in the The carbonate deposits assigned to MFA5 formed in upper part of the profiles studied, being deposited in peri- a shallow, subtidal environment of the platform shelf. Taxo- tidal environments with reduced hydrodynamics (Shinn, nomic diversity of microfossils is significantly reduced as 1983; Hardie and Shinn, 1986). These limestones are fre- compared to the previously described deposits (MFA1 to quently associated with the facies of intertidal ponds and in MFA4). Micrite-dominated facies types, characterized by places with supratidal deposits. Overall, they most probably micritization processes, were noticed towards the top of this characterize lagoonal sedimentary settings (Morsilli and microfacies association type. Bosellini, 1997). The abundant rivularia-type cyanobacteria (often with clear envelopes or fine micritic cortexes), micro- bial oncoids and fenestral structures indicate a transition with more protected depositional environments of these FACIES DISTRIBUTION, SEDIMENTARY micrite-dominated limestones (Flügel, 2004). SETTINGS AND EVOLUTION OF STUDIED CARBONATE PLATFORM

MFA5 – Bioclastic packstone/wackestone Starting with the lower part of the carbonate succession of the Buila-Vânturariþa Massif, finer deposits of granular This microfacies type is found in six out of the eight pro- flows with turbiditic character (MFA1) occur. They were files studied. They transgressively overlie Upper Juras- recognized in three of the sections analysed (Fig. 6). This sic–lowermost Cretaceous deposits (MFA1, MFA2, MFA3). feature points to an environment with relatively high en- In the Arnota Mountain (P2) and the Costeºti Gorges (P3), ergy, most probably located towards the base of the reef the Lower Cretaceous deposits (MFA5) are similar to those slope (Mullins and Cook, 1986; Bucur et al., 2010a). On top of MFA4-type, at the tops of the successions. Microfacies of these deposits, thick levels of reef rudstones (MFA2), types are represented by bioclastic-peloidal wackestone with intelayered with coral-microencruster boundstones with foraminifera [Paracoskinolina? jourdanensis (Fig. 5G) and stromatoporoids (MFA3), are present. Bioconstructions Vercorsella camposaurii (Fig. 5F)], fractured, intraclastic (MFA3) occur on top of MFA2-type facies that evidence wackestone, bioclastic-oncoidal wackestone with rivularia- the instability of the reefal slope. The associated distribution cean-type cyanobacteria and peloidal-fenestral wackestone. of reef facies types (MFA2 and MFA3), the thickness of the In the Cacova sector (P4), the authors have identified bio- rudstone levels and the presence of typical microfossil asso- clastic-peloidal wackestone/packstone with foraminifera ciations are all arguments for a patch-reef development of (Paracoskinolina? jourdanensis) and rudist fragments, pe- most of the bioconstructions in Buila-Vânturariþa Massif. loidal fenestral wackestone and fractured wackestone. The The genesis of these bioconstructions was strictly controlled

Fig. 7. Diagenetic features. A. Large cement crust formed as a result of radiaxial-fibrous cement recrystalization (RFC) in a reef-slope rudstone; note fine laminated peloidal sediment in the cavity formed by cement growth indicating synsedimentary cementation (sample 21 - Bistriþei Gorges – P1). B. Neomorphic features inside a coral fragment; after dissolution of the septa the interseptal spaces were subse- quently filled with granular cement (arrow) (sample 1050 – ªtevioara sector – P6). C. Synsedimentary radiaxial-fibrous cement (RFC) succeeded by a recrystalization phase; notice the relic features of the primary radiaxial-fibrous cementation (arrows) followed by a granu- lar spar cement coarsening towards the centre of the crust; CM – Crescentiella morronensis encrusting synsedimentary cement (sample 14b – Bistriþei Gorges – P1). D. Multiple cement generations in a reef-slope facies; the first generation of cement is represented by a fine rim of isopachous-fibrous cement (IFC) surrounding the oncoids, followed by a brownish microcrystaline cement (MC); the third genera- tion of cement is composed of bladed isopachous spar crystals (BS) succeeded by a final stage of clear blocky calcite cementation (BC) (sample 696 – Albu Mountain – P5). E. Meteoric dissolution resulted in cavities (DC) bordered by rims of non-isopachous dog-tooth ce- ment (NIDC), locally associated linewith syntaxial cement overgrowing echinoid fragments (SOC); the internal filling of the cavities is made up of fine, marl-silty sediment, probably of vadose origin (sample 151 – Bistriþei Gorges – P1). F. Mixed meteoric and shallow burial features in a coral-microbial boundstone; the meteoric diagenesis is represented by several dissolution cavities (DC); the corals were partially fractured during initial burial, followed by a last stage of cementation inside the fissures, represented by clear blocky crys- tals (sample 13a – Bistriþei Gorges – P1). G. Peritidal oncoidal wackestone with gravitational cements (GC) that hang from the bottoms of the grains; the remaining pores were filled with granular spar (sample 332 – Arnota Mountain – P2). H. Early dolomitization; some of the rhomboedrical dolomite crystals are partially filled with vadose calcite (dedolomitization), probably triggered by the change of meteoric regime into a normal-marine one (sample 943 – Curmãtura Oale – P7). 178 G. PLEª ET AL. UPPER JURASSIC–LOWER CRETACEOUS CARBONATE DEPOSITS, ROMANIA 179

by stabilization of the reef debris. Thus, the encrusting char- remian) transgressively overlie the Jurassic–lowermost Cre- acter or the sediment-binding function that most biocons- taceous succession (Fig. 6). Towards the top of the Creta- tructing organisms play. The relatively reduced thickness of ceous succession the authors observed a more internal evo- these bioconstructed levels (MFA3) may be also connected lutionary trend of the depositional environment, as indica- to the nature of the reef framework-forming organisms. In ted by fracture fillings, bioclast micritization and oncoids. contrast to the Upper Jurassic microbialite-dominated reefs The general distribution and features of the main facies of the northern Tethyan realm (Leinfelder et al., 1993), the associations, together with the associated biota, indicate a cement-supported microencruster frameworks, which char- barrier-type development of the Buila-Vânturariþa carbon- acterize the MFA2 and MFA3 facies associations, show ate platform (Turnšek et al., 1981; Schlagintweit and Gaw- many similarities with the Late Jurassic “Plassen”-type mi- lick, 2008; Rusciadelli et al., 2011). Furthermore, the Buila- croencruster boundstones of the Northern Calcareous Alps Vânturariþa platform slope shows the classical geometry of (Schlagintweit and Gawlick, 2008; Pleº et al., 2013). There- many intra-Tethyan platform margins (Morsilli and Bose- fore, laminated microbial structures are subordinate to en- llini, 1997; Pleº et al., 2013). The gradual transition from crusting micro-organisms associated with synsedimentary deeper to shallower sedimentary settings can be strongly cement crusts in the development and consolidation of these correlated with the prograding character of the carbonate deposits. On the basis of the composition and textural-stru- platform during the Upper Jurassic. ctural features, the described facies associations (MFA2 and MFA3) were assigned to fore-reef slope environments, close to the proximal areas of the reef crest (Turnšek et al., 1981; Schlagintweit and Gawlick, 2008; Rusciadelli et al., DIAGENETIC HISTORY 2011; Pleº et al., 2013). The presence of stromatoporoids in Early marine diagenesis in subtidal environments these facies was supported by their location in shallow, high-energy environments. This also explains the resistance The features identified in the eight profiles studied that of most of these taxa to remobilization or fragmentation, are related to early marine diagenesis consist of: (i) succes- which are typical phenomena in platform-marginal environ- sive generations of cements with fibrous fabrics, (ii) recrys- ments (Leinfelder et al., 2005). In the upper part of the Up- tallization, and (iii) micritization. Fibrous-radiaxial, micro- per Jurassic–lowermost Cretaceous succession, all the typi- crystalline and scalenohedral cements were frequently no- cal terms of peritidal environments (subtidal, intertidal and ticed in reef deposits (MFA2 and MFA3). Fibrous radiaxial supratidal – MFA4) were recorded. The subtidal, marine en- cements may form crusts inside interparticle spaces or vugs, vironment is indicated by the type of carbonate components in most cases being associated with biogenic encrustations. (bioclasts, peloids, oncoids), embedded in a micritic matrix Sometimes these cements can be seen as replacements for associated sometimes with bioturbation structures. The fast, early cementation products. This mechanism is sup- intertidal environment includes beach deposits, formed in ported by the presence of relic, prismatic crystals (possibly areas with high energy (peloidal packstones with “keystone of aragonitic nature) within the crusts (Fig. 7A, C; Reitner, vugs”) and fine, laminated fenestral deposits, typical for a 1986). Morphological traits of the relic crystals are pre- low-energy environment. The supratidal environment con- served (Kendall and Tucker, 1973; Henrich and Zankl, tains non-fossiliferous and fenestral, micritic limestones 1986; Koch and Schorr, 1986), or alternatively the replace- that might have been affected by dolomitization. These de- ment process may be traced by the presence of obvious dis- posits are comparable to the peritidal cycles of the lagoonal continuities within the cements crusts formed in the cavities facies association (F1A, F1D and F1E), documented by of the reef deposits (MFA2 and MFA3). The synsedimen- Morsilli and Bosellini (1997) in Upper Jurassic–Lower Cre- tary nature of these cement crusts is reflected in the encru- taceous platform-margin limestones in Southern Italy. Peri- station by micro-encrusters (Fig. 8A; Schlagintweit and tidal limestones of the Buila-Vânturariþa Massif show a de- Gawlick, 2008; Ko³odziej, 2015b). The scalenohedral ce- crease of accommodation space in the carbonate platform. ments are mainly composed of denticulated, prismatic ce- The Lower Cretaceous deposits assigned to the MFA5 (Bar- ments, developed as infilling crusts within intra-reef cavi-

Fig. 8. Microfacies and diagenetic features. A. Crusts of radiaxial-fibrous cement (RFC) strengthening a stromatoporid-microencruster framework with Cylicopsis verticalis (C), Tubuliella fluegeli Turnšek (T) and Perturbatacrusta leini (P) (sample 737 – Albu Mountain – P5). B. Scalenohedral cement (SC) formed in a reef cavity; note the presence of a boring structure (BS) inside the zoantharian fragment (sample 1109 – Arnota Mountain – P2). C. Stromatolitic-clotted meso-structure supporting the stromatoporid boundstone (sample 554 – Costeºti Gorges – P3). D. Dissolution cavity (DC) filled with fine silty or marly sediment; the external margins are bordered by a clear layer of non-isopachous dog-tooth crystals (NIDC) associated with syntaxial-overgrowth cement (SOC) (sample 1118 – Arnota Mountain – P2). E. Successive microcrystalline crusts probably induced by cyanobacterial growth; note the radial displacement of crystals associ- ated with fine, micritic lens; in the upper pat of the picture, there is a small cavity filled with geopetal sediment (arrow); in the lower part of the cavity a second generation of non-isopachous dog-tooth cement developed on a early generation of isopachous marine cement (sample 1130 – Arnota Mountain – P2). ain F. Multiple generations of cements in a closed pore; the chronological order of cementation is evi- denced by cathodoluminescence; the first cementation stage is represented by non-luminescent, zoned crystal rims, followed by dull-lumi- nescent much larger crystals; the final filling of the pore is marked by bright orange, blocky cementation probably formed during shallow burial (sample 5 – Bistriþei Gorges – P1). 180 G. PLEª ET AL.

ties (Fig. 8B). In the peritidal facies types (MFA4), some of the mixing zone towards the basin, in connection with crusts of microcrystalline cements are represented by very falls in sea level (Frykman, 1986). fine, micritic laminae intercalated with radial, microsparitic cements (Fig. 8E). The relatively small size of crystals in the Shallow burial diagenesis microcrystalline filaments indicates relatively rapid cemen- tation processes, probably induced by changes in the chem- In their material, the authors noticed a low compaction istry of the environments, where cyanobacteria were pres- of sediments, given the fact that early cementation took ent. Heinrich and Zankl (1986) have described association place during marine diagenesis. The fragmentation of some of cyanobacteria with sparitic, microcrystalline cements as macrofossils (corals, bivalves or gastropods), and the pres- organic-diagenetic-type cements. Microbial micritization ence of fissures and cavities filled with sparitic calcite are occurs in sponge-coral bioconstructions (MFA3) and partic- the most typical features of burial diagenesis in the lime- ularly in peritidal facies (MFA4). This characteristic may be stones of the Buila-Vânturariþa Massif. In the reef deposits used as a proxy for incipient diagenetic processes (Qureshi (MFA1, MFA2 and MFA3), the burial diagenesis-related et al., 2008; Lazãr et al., 2013). These processes consist of cements show typical morphological features for burial en- the formation of micritic microcrystalline cortices around vironments. The crystals are mainly equigranular (mosaic), some bioclasts (partial micritization); in extremis, the bio- but in some places there is an increase in size towards the clasts can be completely replaced by micrite (complete mi- centre of the pores (druse-type cement) (Fig. 8F). Such late critization; Flügel, 2004). In the Jurassic reef deposits stud- stages may be followed by a final, blocky-type cementation. ied (MFA2 and MFA3), the authors have identified neo- In the peritidal facies (MFA4), the final cavity-filling prod- morphic processes represented by selective (partial or total) ucts are represented by mosaic-type granular cements. dissolution of the coral structure, or of some stromatoporoid skeletons. This was followed by low-Mg calcite recrystalli- Porosity zation (precipitation) within the newly-created inter-skele- tal space (Fig. 7B). The intense microbial activity and the encrusting char- acter of most of the biota identified in the reef limestones of the Buila-Vânturariþa Massif (MFA3) resulted in a signifi- Diagenesis in meteoric environments cant decrease of primary porosity and in the development of Selective dissolution, gravitational isopachous and syn- morphologies, typical for bioconstructions. In the reef-slope taxial cements and microkarst associated with marly-fine deposits (MFA1 and MFA2) showing coarser fabric as a re- siliciclastic fillings, are all proof of meteoric diagenesis in sult of reef detrital flows, the primary porosity is relatively the limestones in the Buila-Vânturariþa Massif. In the reef higher. Secondary porosity was clearly noticed in some environments (MFA2 and MFA3), as well as in the inter- samples, in spite of the fact that most of the cavities had tidal facies (MFA4), gravitational cementation is repre- been rapidly filled with early marine cements. The authors sented by microstalactitic cements, formed on bioclasts or assume that, following the early burial, selective dissolution intraclasts (Fig. 7G; Scholle and Ulmer-Scholle, 2003). The by meteoric waters led to increased porosity in the form of most common cements that the authors have associated with fissures and cavities (Heinrich and Zankl, 1986). These processes in the phreatic zone are the bladed and dog-tooth voids were subsequently filled in part by sparitic microcrys- types. They consist of crystalline bands, bordering cavities talline crusts or bands of inequigranular crystals (Fig. 7E). in reef deposits (Figs 7E, 8B). The crystals are oriented Kerans et al. (1986) stated that porosity shows particular sub-perpendicular to their substrate. Another meteoric dia- features on the basis of the depositional environments. The genesis-related product is the overgrowth of syntaxial ce- highest values are registered in areas with constant synsedi- ment formed on the echinoderm radioles and/or plates (Figs mentary activity, such as reef-slope deposits (MFA1 and 7E, 8D), identified in reef detrital deposits (Pomoni-Papaio- MFA2), or peritidal facies (MFA4) at the top of the carbon- annou et al., 1989; Flügel and Koch, 1995; Qureshi et al., ate succession. 2008). In the case of the samples in the present study, the syntaxial cements are often associated with the bladed or dog-tooth cements along the borders of cavities formed as a CONCLUSIONS result of meteoric dissolution. Koch and Schorr (1986) con- sidered the association of these cements as possible evi- 1. Carbonate deposits of the Buila-Vânturariþa Massif, dence for subaerial episodes. According to Buddemeier and studied here in eight profiles, mainly consist of massive, Oberdorfer (1986), dolomitization is favoured by a certain white carbonates, assigned to the Upper Jurassic–Lower degree of mixing between marine and meteoric fluids. The Cretaceous interval. The lower and middle part of the suc- present authors consider that this may explain the fact that cession is characterized by thick levels of reef debris inter- dolomitization was observed in their samples only in the layered with coral-microbial bioconstructions with encrust- peritidal facies (MFA4), on the top of the Jurassic succes- ing micro-organisms and stromatoporoids. Towards the top sion. The results are rhombohedral crystals dispersed in the of the succession, peritidal limestones are assigned to the microcrystalline matrix, associated with late-generation ce- lowermost Cretaceous. The Barremian–?Lower Aptian de- ments (Fig. 7H). In the same peritidal facies the authors also posits, which cover relatively small areas, spread over the have observed partial dissolution of dolomite crystals (de- massif, transgressively overlie the white limestones of Kim- dolomitization). De-dolomitization may point to a migration meridgian-Valanginian age. UPPER JURASSIC–LOWER CRETACEOUS CARBONATE DEPOSITS, ROMANIA 181

2. The assemblages of calcareous algae and benthic Stephen Kershaw for correcting the English of the manuscript. foraminifera allowed the authors to specify the age of the Last but not least, the first author gratefully acknowledge the sug- deposits studied. Reef limestones were assigned to the Kim- gestions of Micha³ Gradziñski (Kraków). meridgian–Tithonian; peritidal facies to the Berriasian–Va- langinian (Montsalevia salevensis and Protopeneroplis ul- tragranulata being the main supporting evidence), while REFERENCES limestones at the top of the succession, which transgressi- vely overlie the Upper Jurassic–lowermost Cretaceous de- Bodrogi, I., Bona J. & Lobitzer, H., 1994. Vergleichende Untersu- chung der Foraminiferen- und Kalkalgen-Assoziationen der posits, are referable to the Barremian–?Lower Aptian (with Urgon-Entwiklung des Schrattenkalks in Voralberg (Öster- Paracoskinolina? jourdanensis). reich) und der Nagyharsány Kalkstein Formation des Villány- 3. 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Microfaciesurile calcarelor albe din partea nor- sic–Lower Cretaceous limestones in the Getic domain (e.g., dica a masivului Piatra Craiului. Consideratii biostratigrafice. Piatra Craiului-Dâmbovicioara area). Dãri de seamã ale Instutului Geologic al României, 64: 89– 5. Investigation of diagenetic features of the Buila- 105. [In Romanian.] Vânturariþa Massif reveals three stages. The first stage is Bucur, I. I., 1993. Les représentants du genre Protopeneroplis Weynschenk dans les dépôts du Crétacé inférieur de la zone represented by syndepositional, marine cementation that de Reºiþa-Moldova Nouã (Carpathes Méridionales, Rouma- strongly influenced the features of the reef deposits, either nie). Revue de Micropaléontologie, 36: 213–223. during their formation or during early burial. Successive Bucur, I. I., Beles, D., Sãsãran, E. & Balica, C., 2010a. New data laminae of radiaxial and microcrystalline fibrous cements on facies development and micropaleontology of the eastern have consolidated the reef framework and have strength- margin of the Getic Carbonate Platform (South Carpathians, ened the reef-slope and peritidal deposits. The second dia- Romania): case study of Mateiaº Limestone, Studia Univer- genetic stage is represented by dissolution, recrystallization sitatis Babeº-Bolyai Geologia, 55: 33–41. and precipitation of specific cement types, as a result of the Bucur, I. I., Cociuba, I. & Cociuba, M., 1993. Microfacies and infiltration of meteoric waters. Processes of dolomitization microfossils in the Upper Jurassic-Lower Cretaceous lime- and de-dolomitization took place sporadically, triggered by stone in the southern part of the Pãdurea Craiului Mountains. the mixing of marine and meteoric waters, probably con- Romanian Journal of Stratigraphy, 75: 33–40. nected with transgression episodes. Given the frequent ma- Bucur, I. I., Conrad, M. A. & Radoièiæ, R., 1995. Foraminifers and calcareous algae from the Valanginian limestones in the Jer- rine and meteoric cementation stages, the deposits are ma River Canyon, Eastern Serbia. Revue de Paléobiologie, poorly compacted. The third stage was the formation of 14: 349–377. fractures and late-generation cements, which took place in Bucur, I. I., Gradinaru, E., Lazar, I. & Gradinaru, M., 2014b. Early the burial environments. Cretaceous micropaleontological assemblages from a con- densed section of the Codlea Area (Southern Carpathians, Romania). Acta Palaeontologica Romaniae, 9: 65–82. Acknowledgements Bucur, I. I., Granier, B. & Krajewski, M., 2014a. Calcareous algae, This work was made possible by the financial support of the microbial structures and microproblematica from Upper Ju- Sectoral Operational Programme for Human Resources Develop- rassic-Lowermost Cretaceous limestones of southern Crimea. ment 2007-2013, co-financed by the European Social Fund, under Acta Palaeontologica Romaniae, 10: 61–86. project number POSDRU/159/1.5/ S/132400 with the title “Suc- Bucur, I. I., Pãcurariu, A., Sãsãran, E., Filipescu, S. & Filipescu, cessful young researchers – Professional development in interdis- R., 2014c. First record of lowermost Cretaceous shallow-wa- ciplinary and international context”. We would like to thank Cris- ter limestones in the basement of the Transylvanian Depe- tian Victor Mircescu for assistance in the field. We also thank the ssion (Romania). Carnets de Géologie, 14: 199–210. two reviewers, Felix Schlagintweit and Bogus³aw Ko³odziej for Bucur, I. I. & Sãsãran, E., 2005. Micropaleontological assem- their remarks, which helped to improve the paper. Iuliana Lazãr blages from the Upper Jurassic-Lower Cretaceous deposits of and Mihaela Grãdinaru (University of Bucharest) are thanked for Trascãu Mountains and their biostratigraphic significance. their support with cathodoluminescence analysis. We also thank Acta Palaeontologica Romaniae, 5: 27–38. 182 G. PLEª ET AL.

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