Crescentiella-microbial-cement microframeworks in the Upper Jurassic reefs of the Crimean Peninsula
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In the Upper Jurassic reef successions of the Crimean Peninsula (Sudak and Jalta areas), the microencruster Crescentiella morronensis (Crescenti), microbialites, and multiple generations of cements, form microframeworks. They were observed in two stages of the carbonate platform evolution, in the Middle–Upper Oxfordian, and in the Upper Kimmeridgian–Tithonian. Generally, in both stages, the features of the microframeworks are similar and consist of densely packed Crescentiella associated with microbialites and branched colonies of the sclerosponge Neuropora lusitanica Termier. The difference between the occurrences of the two stages is the variable amount of nubecularid foraminifera and enigmatic tube-shaped structures forming the central cavities of Crescentiella. The Crescentiella-microbial-cement microframeworks formed under phreatic conditions in the upper slope and seaward marginal depositional settings where intensive synsedimentary cementation took place. They formed in the initial stages of long cycles of restoration and blooming of the reefs. The late Jurassic examples resemble the Permian algae-microbial-cement reefs as well as the Triassic Tubiphytes and cement crust-dominated reefs. Concurrently, all these examples formed a transitional facies zone between typical slope facies to shallow subtidal platform margin facies characterized by high taxonomic diversity of calcified sponges, corals, and microencrusters forming the principal part of the reefs.
KeywordsMicroencrusters Crescentiella Microbialites Cement crusts Reefs Late Jurassic Crimea
In the Tethyan realm and its margins, the Late Jurassic was a time of intensive growth of reefs. The North Tethys/Atlantic reefs that developed on extensive ramp-type platforms can be assigned to three broad compositional types: (1) coral-dominated, (2) siliceous sponge-dominated, and (3) microbialite-dominated (e.g., Leinfelder et al. 2002). In contrast hereto, the isolated reefs growing at the margins of intra-Tethyan platforms were dominated mostly by mixed, corals-calcified sponges (including stromatoporoids and chaetetids) facies (e.g., Turnšek et al. 1981; Leinfelder et al. 2002, 2005; Vlahović et al. 2005; Ivanova et al. 2008; Rusciadelli et al. 2011; Della Porta et al. 2013; Hoffmann et al. 2017). Their characteristic lateral assemblages allow the zonation of these reef complexes, corresponding to fore-reef, reef crest, and flat to back-reef environments.
Unlike other Upper Jurassic reefs from both western and southern Europe, which have deserved a number of detailed studies, the reefs from the Crimea-Caucasus region have received less attention, as yet. Most of the studies were mainly descriptive, whereas detailed data were rarely published. For the Southern Crimea, Nikishin et al. (2015a, b) presented a ternary plot showing the Late Jurassic reef-building communities of Crimean reefs based upon data from, among others, the Ai-Petri Massif (Krajewski 2008, 2010). The main reef-builders were microbial mats/microencrusters, corals and sponges, which correspond to assemblages known from the Caucasus Mts. (e.g., Bendukidze 1982; Guo et al. 2011). In the Crimea Mts, the most spectacular Oxfordian coral reefs are reported from the Sudak area (e.g., Muratov 1973; Geister et al. 2007; Nikishin et al. 2015b) although detailed studies on their facies and microfacies have so far not been published. A few papers with details concerning Upper Jurassic reefs were published from the Demerdzhi Plateau (Piskunov et al. 2012; Rud’ko et al. 2014, 2017), the Mt. Pakhkal-Kaya (Baraboshkin and Piskunov 2010) as well as the Jalta and the Ai-Petri massifs (Krajewski and Olszewska 2006; Krajewski 2008, 2010; Bucur et al. 2014; Schlagintweit and Krajewski 2015). These publications describe several Upper Kimmeridgian–Berriasian Štramberk-type shallow-water facies and microfacies documenting the development of Crimean carbonate platform.
In recent papers dealing with both the Tethyan northern shelf and the intra-Tethyan platforms, still-growing attention is paid to the presence and the role of a wide spectrum of so-called “microencrusters” (e.g., Crescentiella, bacinellid fabrics, Thaumatoporella, Radiomura, Lithocodium, Iberopora, etc., e.g., Schmid 1996; Leinfelder et al. 1996; Ivanova et al. 2008; Pleş et al. 2013, 2017; Kaya and Altiner 2015; Hoffmann et al. 2017) in the formation of reef frameworks. Apart from microbial crusts, these microencrusters were important components of coral and sponge reefs as secondary reef-builders. Sometimes they form microbial-microencruster boundstones with a significant content of early cements. Late Jurassic to earliest Cretaceous microbial-microencruster-cement-boundstones (microframeworks) assigned to outer margin-upper slope depositional settings have been reported from various intra-Tethyan (mostly southern Tethyan) platform carbonates: Austria (Schlagintweit and Gawlick 2008, Plassen Limestone), Bulgaria, Czech Republic and Poland (Ivanova et al. 2008; Hoffmann et al. 2017, Štramberk-type Limestone), Romania (Pleş et al. 2013, 2017), Italy (Rusciadelli et al. 2011, e.g., Table 1, Ellipsactinia Limestone), Turkey (Kaya and Altiner 2015) and Japan (Shiraishi and Kano 2004; Ohga et al. 2013, Torinosu Limestone). For a paleogeographic sketch displaying these occurrences in the western part of the Tethys see Fig. 11 in Kaya and Altiner (2015). In terms of microfacies and micro-/macrobiota assemblages, they differ from time-equivalent ramp deposits of the European northern Tethyan margin (see Leinfelder et al. 1994, 2002).
A common and widespread taxon of microencruster inhabiting the Upper Jurassic–Lower Cretaceous platforms is Crescentiella (former Tubiphytes) morronensis (Crescenti 1969) (Senowbari-Daryan et al. 2008, for details). It represents an enigmatic microorganism of controversial systematic position (e.g., Flügel 1981; Schmid 1995; Senowbari-Daryan et al. 2008; Kaya and Altiner 2015; Pleş et al. 2017) interpreted as encrustation or symbiosis between nubecularid foraminifera or enigmatic, spar-filled, tube-shaped structures and cyanobacteria where foraminifera, tubes and/or other biogenic components provide a substrate for the growth of microbialites.
A significant share of Crescentiella in the formation of reefs, besides the typical reef-builders, was noticed by, e.g., Schlagintweit and Gawlick (2008) who proposed a new type of Upper Jurassic reefs (or part of the reefs) dominated by microencrusters-cement microframeworks, based upon data from the Northern Calcareous Alps of Austria. Less common is the pure dominance of Crescentiella, which is the case described and discussed in the present paper. It must be emphasized that a significant contribution of Crescentiella in microframework building was described also from the Tethyan northern shelf (Germany, southern Poland), where Oxfordian microbial-Crescentiella boundstone facies (Tubiphytes reefs) occurs (e.g., Pomoni-Papaioannou et al. 1989; Leinfelder et al. 1994; Matyszkiewicz 1997; Krajewski et al. 2016). For example, in southern Poland, such facies was found on the slopes of grabens active in Late Jurassic times, where the marine cements common in microbial-Crescentiella boundstones were accompanied by similarly abundant, stromatactis-like cavities (Matyszkiewicz 1997; Olchowy 2011; Matyszkiewicz et al. 2012; Krajewski et al. 2016).
In the Upper Jurassic reef successions of the Crimean Peninsula, reef facies were observed where Crescentiella, microbial crusts and cements were prevailing components thereby forming microframeworks. Such structures have so far not been described in detail from the Crimea-Caucasus region. Hence, the following paper aims to characterize such microframework based on data from two typical occurrences of Late Jurassic reefs in the Crimea. Furthermore, the position and the role of these Upper Jurassic microframeworks in the reef formation will be discussed.
Location and geological setting
The field studies were run in the two regions of Upper Jurassic reefs occurrences: in the vicinity of Sudak town where Upper Jurassic deposits belong to the Sudak Series and in the vicinity of Jalta town where the Ai-Petri Massif is built of sedimentary rocks of the Yaila Series (Fig. 1). According to Nikishin et al. (2015b), the reefs observed in the Sudak region represent a fragment of the Upper Oxfordian reef belt extending along the northern margin of the Shatsky Ridge carbonate platform. These reefs are regarded as close analogues to the Late Jurassic reefs found in the Shatsky Ridge (Afanasenkov et al. 2005; Guo et al. 2011). The Ai-Petri Massif is a spectacular example of the Late Kimmeridgian–Tithonian reef complex (Krajewski and Olszewska 2006, 2007) resembling the Štramberk-type reefs well known from the Pontides, Moesia, Southern Carpathian, Polish and Czech Outer Carpathian, Southern Crimea and the Northern Caucasus Mts (e.g., Matyszkiewicz and Słomka 2004; Bucur and Săsăran 2005; Ivanova et al. 2008; Guo et al. 2011; Piskunov et al. 2012; Pleş et al. 2013; Kaya and Altiner 2015; Kołodziej 2015; Strzeboński et al. 2017; Hoffmann et al. 2017; Vincent et al. 2018). The main part of the Late Jurassic successions from the Crimean Mts. was deposited onto the marginal part of the epicontinental basin, which rimmed the northern margin of the Tethys Ocean (Golonka 2004; Nikishin et al. 2015a).
Materials and methods
Characteristics of the Crescentiella-microbial-cement microframeworks in the Upper Jurassic reefs of the Crimean Peninsula. Reef classification after Riding (2002)
Upper Kimmeridgian–Lower Berriasian
Type of bioconstruction
Mainly: Coral biostrome, coral-microencruster cluster, segment and frame reef
Mainly: Calcified sponge-coral-microencruster segment and frame reef, coral biostrome
Locally: Skeleton-cement and microbial reef
Locally: Skeleton-cement and microbial reef
Position in the sequence
Lower part of the sequence; between platy
mainly microsolenid biostromes and coral microencruster
Mainly lower part of the sequence between
microbial reefs, microsolenid biostromes and
stromatoporoid-coral-microencruster reef and
Crescentiella, Neuropora, microbialites
cements, serpulids, foraminifers
Crescentiella, Neuropora, microbialites,
cements, serpulids, foraminifers
Central cavities: mainly enigmatic tube-shaped
structures, rarely nubecularid foraminifers;
Central cavities: mainly nubecularid
foraminifers, rarely enigmatic tube-shaped
structures; microbial envelopes
Moderate, locally high dominating
Isopachous, radiaxial-fibrous, dog tooth
dm-scale thickness m-scale or more extent
dm-scale thickness m-scale or more extent
Densely packed Crescentiella with stromatactis-like
Densely packed Crescentiella with stromatactis-like
Forereefal to upper slope
Upper slope to marginal setting
Field occurrence of the Crescentiella-microbial-cement (Cmc) microframeworks
Sudak area (Upper Oxfordian reefs)
In the Sudak area, investigations were carried out in the Koba-Kaya Mts., the Sokol Mts. and in the quarry close to Dachnoye village (Figs. 2a, 3). The sediments encountered there represent the Upper Oxfordian massive and bedded facies (e.g., Muratov 1973; Nikishin et al. 2015b; Figs. 2a, 3a). The bedded, partly marly facies is formed by coral floatstones with platy microsolenids whereas the massive facies is dominated by coral-microencruster boundstones (Fig. 3; Nikishin et al. 2015b). In the lower parts of the reefs and down the reef slope, both platy microsolenids and Actinaraea occurred (Fig. 3b). Both nodular and massive colonies coexisted with branching and dendroid corals (Fig. 3e–g). In a significant number of the reefs, branching scleractinians occur. Among the corals forms such as Calamophylliopsis, Stylosmilia, Thecosmilia, and Heliocoenia were identified. In the reef slope, coral-bioclastic grainstones–rudstones accumulated (Fig. 3c, d). In the massive facies, growth cavities with geopetal infillings were seen, indicating that the Koba-Kaya and the Sokol reefs have not been tectonically tilted. In the uppermost part of the reefs, synsedimentary breccias and microbial laminites have been observed (e.g., in the Koba-Kaya Mts.; Fig. 3h). Similar observations in the nearby Oxfordian reef (Sudak fortress mountain) were carried out by Geister et al. (2007). In a brief description, they distinguished a barrier reef system with lateral coral facies change from back-reef over the reef crest with dominating upright branching scleractinians to a steep reef slope with increasing presence of platy corals (Geister et al. 2007).
In the lower parts of the reef successions, bioclastic wackestones and coral floatstones are prevailing. Higher in the sequence, massive gray limestones appear classified as bioclastic grainstone-rudstones with Crescentiella as well as Crescentiella-microbial-cement (Cmc) boundstones (Fig. 5a, d). Both the lateral and vertical ranges of the Cmc boundstones are difficult to estimate due to the steepness of the terrain. In the best-accessible, lower part of the quarry near Dachnoye village (Fig. 5a), the Cmc lateral extension is up to several meters and the vertical one is about 1.5 m. Up the sequence, the facies with numerous Crescentiella grades into coral boundstones-floatstones (Fig. 5a, b). The contact between Crescentiella-microbial facies and coral facies is sharp.
Jalta area (Upper Kimmeridgian–Tithonian reef)
The Ai-Petri reef complex comprises strongly lithified, gray, massive Štramberk-type reef facies grading laterally into thick- and thin-bedded facies (Fig. 2b) with some intervals of mixed, siliciclastic–carbonate facies in both the lower and its central parts (Krajewski 2008, 2010). Based on biostratigraphic analyses the massive facies of the Ai-Petri reef is Upper Kimmeridgian–Tithonian in age whereas the bedded facies encountered in the uppermost part of the reef (Fig. 2b) is of Lower Berriasian age (Krajewski and Olszewska 2006, 2007). Generally, several main intervals are observed in which the slope and the fore-reef, marginal, back reef, and lagoonal facies are evident, all reflecting the reef evolution (Fig. 2b). Moreover, several smaller, repeating, low-rank sedimentary sequences can be observed (Krajewski 2008, 2010).
The lower part of reef complex in question comprises mainly bioclastic wackestones, platy corals floatstones with microsolenids and microbial boundstones, several tens of meters in thickness (Fig. 4a, b). Up the sequence, the fossil assemblage reveals a high diversity with dasycladalean and udoteacean algae (Fig. 4g), foraminifers, calcified demosponges (stromatoporoids and chaetetids, e.g., Chaetetopsis spengleri, Pseudoseptifer, Actinostromaria, Milleporidium, Sarmentofascis? digitatus, Cladocoropsis, Stromatopora, Milleporella; Fig. 4c, d), corals (e.g., Stylina, Thecosmilia, Heliocoenia, Latomeandra, Stylosmilia; Fig. 4e, f) and a wide spectrum of microencrusters including Crescentiella morronensis, Pseudolithocodium carpathicum, Koskinobullina socialis, Thaumatoporella parvovesiculifera, Lithocodium aggregatum. In the middle part of this sequence, bioclastic–ooidal marginal facies sometimes prevails over the reef facies (Fig. 4h). The boundstones and floatstones are built mainly by calcareous sponges and corals skeletons. Densely packed skeletons reveal growth with microencrusters and microbialites representing secondary reef-builders. Both the sponge and the sponge-coral facies are observed especially in the lower and the middle parts of the reef sequence whereas the coral-sponge facies is more common in its uppermost part.
The sedimentary sequence with the Cmc microframework was observed in the lower portions of the Ai-Petri reef succession (Figs. 2b, 5c) and, less commonly, in its middle portion (Krajewski 2010). In the upper reef succession, Crescentiella occurs dispersed in the peri-reefal bioclastic wackestones–floatstones or growing on skeletons of sponges and corals. The lower reef succession is dominated by bioclastic wackestones and coral floatstones followed upward by microbial, Crescentiella-microbial and calcified sponge-coral facies. The Cmc microframeworks of meter-scale lateral, and decimeter-scale vertical extensions were noticed although it is difficult to estimate their true lateral extent due to the steepness of the terrain.
Microfacies of the Crescentiella-microbial-cement (Cmc) microframework
Generally, in both the Upper Oxfordian and the Upper Kimmeridgian–Tithonian reefs from the Crimea area, the macroscopic features of the Cmc microframeworks are similar (Figs. 5, 6, 7, Table. 1): both are dark-grey (Sudak area) or light-grey (Jalta area), hard, lithified limestones (Fig. 5a–d). The sediment consists of densely packed Crescentiella, mostly in growth position (Figs. 5a, d, 6e, f). Common are caverns filled with various generations of cements, some of them representing stromatactis-like caverns with geopetal infillings (Fig. 6e). The microframeworks are dominated by Crescentiella accompanied by microbialites and specimens of the branching sclerosponge Neuropora lusitanica Termier (Fig. 6a, b). Some specimens of Crescentiella morronensis are up to 1.3 cm in height. Within the Crescentiella laminae, foraminifers and fine bioclasts are observed. Crescentiella is formed by encrustation or symbiosis between nubecularid foraminifers (Figs. 6e, f, 7a) or enigmatic, spar-filled, tube-shaped structures (Fig. 6a–d) and the microbial envelopes (Senowbari-Daryan et al. 2008; Schlagintweit and Gawlick 2009; Pleş et al. 2017). The basic difference between the Upper Oxfordian and the Upper Kimmeridgian–Tithonian specimens is the variable amount of nubecularid foraminifera and tube-shaped structures forming the central cavities of Crescentiella. In the Upper Oxfordian samples, higher amounts of tube-shaped, enigmatic structures are observed whereas in the Upper Kimmeridgian–Tithonian specimens, nubecularid foraminifers prevail.
In both areas, Crescentiella is commonly accompanied by the branching sclerosponge Neuropora, more common in the Oxfordian reefs from the Sudak area (Fig. 6a–d). Usually, specimens of Neuropora grow vertically as delicate, ramified colonies with branches ranging from 2 to 5 mm in diameter and showing dendroidal forms (Fig. 6a). In many cases, Crescentiella was growing on Neuropora specimens thereby connecting the branches (Fig. 6a, b). Similar to bryozoans and serpulids, Neuropora prefers cryptic habitats and is regarded as frame encruster (Fürsich and Werner 1991).
Further important components are microbialites, which form clotted fine, peloidal fabrics between the Crescentiella colonies (Fig. 6a–f). Sometimes, faint layered structures can be observed. In the voids, thin micrite films onto which thin, fibrous cement crusts grow can be observed (Fig. 7a).
Among the biogenic components, bryozoans and serpulids occur, developed mostly on sponges (Fig. 7a) and encrusting foraminifers (e.g., Nubeculariidae) together with numerous, enigmatic, irregular, polymorphous, spar-filled, tube-like microfossils resembling some taxa of mutualistic sponge-epibiont consortia (Schlagintweit and Gawlick 2009).
Numerous voids show the irregular shapes of inorganic origin (growth-framework porosity) or the oval shapes of possible organic provenance (biomoulds; Fig. 6a–f). In the caverns, faint relics of dissolved sclerosponges can be observed displaying poorly preserved internal structures (Fig. 6a, b). In the microframework, stromatactis-like cavities (sensu Matyszkiewicz 1997) are common (Figs. 5d, 6e). Cavities reach 3 cm in length and are up to 1.5 cm high. In their basal parts, the cavities contain internal sediments, followed by calcite cement. Internal sediment is represented by mudstone-thin bioclastic wackestone.
Although the Crimean Late Jurassic reefs are mostly organic reefs, it must be noticed that the Cmc microframeworks are also composed of various cements, which may constitute up to 30% of its components. The radiaxial fibrous cements represent the first generation of cements which developed as thin layers on the walls of voids (Fig. 7a–d), on Crescentiella specimens (Fig. 7a) as well as on thin, micrite films cutting through the voids (Fig. 7a). Important infillings of the voids are represented by massive, radiaxial fibrous and dog tooth cements (Fig. 7a). The central parts of the voids are filled with blocky cement type.
Micropaleontology of the Crescentiella-microbial-cement (Cmc) microframework
Genus Crescentiella Senowbari-Daryan et al. 2008.
Remarks: For a detailed description and interpretation see Senowbari-Daryan et al. (2008). We may note here that in the same year when Crescenti described Tubiphytes morronensis from the Late Jurassic of Italy, this microorganism was also described by Dragastan (1969) neutrally as “micro-oncolites” from the Late Jurassic of Romania, but without application of Linnean nomenclature. Subparallel growing, transversely sectioned specimens of C. morronensis might refer to a taxon described by Dragastan (2010), pl. 78A recently as Sarsteinia getica (interpreted as a sponge) from the late Tithonian of the Getic Carbonate Platform of Romania. In the material from the Crimea, the elongated specimens attain a length of up to 8 mm and a thickness of up to 1.5 mm (mostly 0.8–1.0 mm). The internal sparite-filled cavity (or core) maybe either a cylindrical tube of unknown systematic position or a foraminifera (Nodopththalmidium, Nubeculinella) with superimposed amphora-like chambers (Figs. 6, 7a). Most of the Crimean forms belong to the gregarious C. morronensis forma colligaris morphotype with laterally connected laminated crusts as described by Senowbari-Daryan et al. (2008). In some cases, depending on the plane of sectioning, the differentiation of the two morphotypes (forma morronensis and forma colligaris) may be difficult if not impossible. This peculiar morphotype was described by (Dragastan 1969, Fig. 1, right side) as “micro-oncolithe, sous-type amalgam”. Individual specimens are observed filling borings affecting the skeletons of Neuropora (Fig. 6c). As Crescentiella has never been reported exhibiting an euendolithic potential, these borings were drilled by other organisms of unknown taxonomic origin. These specimens nicely show the inner microbial crust layer of the cortex to be denser and therefore darker (Fig. 6a, c).
Remarks: Termier in Termier et al. (1985) distinguished two morphotypes of N. lusitanica (Oxfordian of Portugal), encrusting and ramose (tree-like branching). The Crimean specimens belong to the ramose morphotype forming delicate, branched colonies with branches ranging from 2 to 5 mm in diameter. As already mentioned, many skeletons display macroborings that are often completely filled with Crescentiella specimens (Fig. 6c). It is worth mentioning that long time considered a bryozoan, the sclerosponge nature of Neuropora Roemer was evidenced by Kaźmierczak and Hillmer (1974).
In the evolution of Jurassic platform of the Crimea Peninsula, the Cmc microframework was observed at two main stages of carbonate platform evolution, separated by erosional unconformity and stratigraphic gap (Nikishin et al. 2015b, cf. Baraboshkin and Piskunov 2010; Fig. 1, Table 1). Deposits of the first stage can be observed in the eastern part of Crimea Mts. (Sudak area) while the deposits of the second stage occur in the central and western parts (Jalta area). In the Middle–Late Oxfordian succession which represents the first stage of carbonate platform evolution, the Cmc microframeworks represent the initial evolution of the Sudak Series reefs. The Cmc microframework with stromatactis-like occur in the transitional phase, from relatively deep water bioclastic and platy coral facies (some tens of meters, e.g., Leinfelder et al. 1996; Insalaco et al. 1997; Lathuilière et al. 2005) to shallow subtidal coral-microencruster facies. The latter is dominated by massive and branching corals building the main parts of the reefs.
In the Late Kimmeridgian–Tithonian, which represents the second stage of carbonate platform evolution, represented in the Yaila Series (Fig. 1), the development of Cmc microframeworks was related to the consecutive stages of reef growth. The Upper Oxfordian–Early Kimmeridgian depositional break caused by tectonic movements was followed by the gradual restoration of reef communities. The bioclastic wackestones-floatstones and platy coral-microbial boundstones-floatstones located in the lower part of reef succession can be linked to the platform slope facies (Krajewski 2008, 2010). Up the sequence, the reefs structures evolved into meter-scale, low-relief microbial reefs with Cmc microframework, and stromatactis-like caverns. Higher up the reef succession is dominated by shallow subtidal massive sponge and coral boundstone or marginal oolitic facies (Krajewski 2008, 2010).
At both large-scale phases of reef development, the microbial and the Cmc boundstones contributed to the stabilization of loose substrate, which enabled the vigorous growth of calcified sponges and corals constituting the main parts of the reefs, together with common microencrusters such as Lithocodium, Thaumatoporella etc. Hence, the described Cmc microframeworks from the Sudak and the Jalta areas represent the initial stages of long cycles of restoration and blooming of the reefs in the Middle–Late Oxfordian and in the Late Kimmeridgian–Tithonian. The main phase of reef growth was characterized by vigorous expansion of a wide spectrum of massive and branching skeletal metazoans and microencrusters building the Frame Reef sensu Riding (2002).
Although the Cmc microframeworks were mostly observed in the lower parts of the reef successions, their infrequent presence must be mentioned also in the middle parts of the reef successions of the Ai-Petri massif where they were accompanied by minor metazoans. In the Ai-Petri reef, the repeating, vertical facies changes represent lower-rank cycles (Krajewski 2008, 2010). The appearance of microbial and Cmc microframeworks together with the deficit of main reef builders can be explained by a crisis in metazoans growth caused by paleoenvironmental stress then followed by the flourishing sponge-coral-microencruster communities. Similar to recent reefs, the Late Jurassic reefs were very sensitive to environmental changes (sea level fluctuations, tectonic events, climate, nutrient content, temperature, etc.). In the Ai-Petri reef, periods were documented during which carbonate production was disturbed by the influx of siliciclastic material and nutrients (Krajewski 2008, 2010; KB and KC sections). Such episodes, triggered by tectonic activity in the surrounding areas, resulted in periodical breaks in the reef growth. However, after the crisis, the restoration of reefs took place, as indicated by deposition of detrital bioclastic wackestones-floatstones followed by microbial and Cmc boundstones and, finally, succeeded by sponge-coral-microencruster framestones showing high biodiversity. In both the high and low sedimentary cycles of the Crimean reefs, the Cmc microframework also appears at the initial phase of reef growth after the breaks in metazoans development, during the restoration of the reef fauna assemblages.
The Cmc microframestone formed under phreatic conditions, in the upper slope, fore-reef and seaward marginal depositional settings where intensive synsedimentary cementation took place. Such environments are characterized by marginal topography and intensive fluid flow (e.g., Della Porta et al. 2003; Flügel 2004; Seeling et al. 2005; Marangon et al. 2011). Both Crescentiella and the microbialites were not only able to adapt to unstable environmental conditions but also stabilized the sediments, thus supporting the development of skeletal metazoans building the main parts of reef complexes. Significant contents of early cement crusts are typical of reefs showing low sedimentation rates and higher rates of water agitation, i.e., conditions preferred by low-growing microbialites and Crescentiella. These cements formed prior to burial, when the voids were open for the early cementation formed marine phreatic conditions. The synsedimentary origin of the fibrous cement is evidenced by microencrusters overgrowth (cf. Kendall and Tucker 1973; Koch and Schorr 1986; Flügel 2004; Schlagintweit and Gawlick 2008). The presence of thin micritic films in cavities intercalating various cement generations indicates that the early marine cementation took place when the voids were opened to marine water (e.g., Payne et al. 2006). In the massive reef sediments, the burial diagenesis is represented by blocky cement constituting the latest cement generation (e.g., Koch and Schorr 1986; Flügel 2004). In the Sudak reefs, large crystals of blocky cement partly replaced the earlier, fibrous cements as a result of burial/meteoric solution. In the Ai-Petri reef, the generations of cements are well preserved. The reefal limestones rich in microbialites and cements are typical of steep, high-energy upper slope depositional setting (e.g., Della Porta et al. 2003, 2013; Flügel 2004; Marangon et al. 2011). The lack of dasycladacean algae and typical shallow water microproblematica (e.g., Lithocodium, bacinellid fabrics, Thaumatoporella etc.) described from higher part of the Crimean reefs (Krajewski 2008; Baraboshkin and Piskunov 2010; Piskunov et al. 2012; Bucur et al. 2014) suggest that the Cmc microframework is rather deeper than several meters.
The examples of Cmc microframework encountered in the Crimea Mts., formed by small, low-growing Crescentiella and microbialites, and rich in early cement crusts resemble Permian algae-microbial-cement reefs (e.g., Edwards and Riding 1991; Flügel 1994; Saller et al. 1999; Wood 1999; Weidlich 2002; Schlagintweit and Gawlick 2008; Kosakowski and Krajewski 2014) as well as Triassic Tubiphytes and cement crust-dominated reefs (Senowbari-Daryan et al. 1993; Flügel 2002; Schlagintweit and Gawlick 2008; Marangon et al. 2011; Senowbari-Daryan 2013; Popa et al. 2014).
In the lower, rarely in the middle part of the Upper Jurassic reef successions of the Crimean Peninsula Crescentiella morronensis, microbialites and cements form cement-supported reefs. Although the Crimean Late Jurassic reefs are mostly organic reefs, it must be noticed that the Crescentiella-microbial-cement microframeworks are also composed of multiple generations of early and late cements, which may constitute up to 30% of its volume. Such structures have so far not been described in detail from the Crimea-Caucasus region.
In the evolution of Jurassic carbonate platforms of the Crimea Peninsula, the Crescentiella-microbial-cement microframeworks were observed in two main stages of carbonate platform evolution. Generally, in both the Middle–Upper Oxfordian and the Upper Kimmeridgian–Tithonian phases of Crimean reefs development, the features of the Crescentiella-microbial-cement microframeworks are similar. They consist of densely packed Crescentiella accompanied by microbialites and branched colonies of Neuropora lusitanica. The main difference between the Middle–Upper Oxfordian and the Upper Kimmeridgian–Tithonian specimens is the variable amount of nubecularid foraminifera and tube-shaped structures forming the central cavities of Crescentiella.
In the Middle–Late Oxfordian reef successions exemplified in the Sudak area, the metric-scale Crescentiella-microbial-cement microframeworks occur in the transitional realm from relatively deep water bioclastic and platy coral facies to shallow subtidal massive and branching corals facies. The Upper Oxfordian–Early Kimmeridgian depositional break was followed by the gradual restoration of reef communities. In the Late Kimmeridgian–Tithonian which represents the second stage of carbonate platform evolution, exemplified in the Jalta area, the development of Crescentiella-microbial-cement microframeworks was related to the consecutive stage of reef growth. The relatively deep water mainly microsolenid facies, up the sequence of the reefs structures evolved into meter-scale, low-relief cement-supported reefs with Crescentiella-microbial-cement microframework. Higher up, the reef succession is dominated by shallow subtidal Štramberk-type massive calcified sponge and coral boundstone and oolitic facies. Hence, the described Crescentiella-microbial-cement microframeworks from the Sudak and the Jalta areas can be observed in the initial stages of long cycles of restoration and blooming of the reefs in the Middle–Late Oxfordian and in the Late Kimmeridgian–Tithonian.
The Crescentiella-microbial-cement microframestone in the Crimean reefs formed under phreatic conditions, in the upper slope and seaward marginal depositional settings where intensive synsedimentary cementation took place. Both the Crescentiella and the microbialites were not only able to adapt to unstable environmental conditions but also stabilized the sediments, thus supporting the development of skeletal metazoans building the main parts of reef complexes. Significant contents of early cement crusts are typical of reefs showing low sedimentation rates and higher rates of water agitation, i.e., conditions preferred by low-growing microbialites and Crescentiella.
The authors are grateful to the two reviewers, G. Pleş and Anonymous, as well as the editor A. Munnecke for their constructive comments and suggestions that considerably improved this paper. MK would like to thank L. Guo and S.J. Vincent for useful discussions. The research was financed from the AGH-UST Grant Nos. 184.108.40.2066.
- Afanasenkov AP, Nikishin AM, Obukhov AN (2005) The system of Late Jurassic carbonate buildups in the northern Shatsky swell (Black Sea). Dokl Earth Sci 403:696–699Google Scholar
- Bendukidze NS (1982) Late Jurassic corals from deposits of reefal origin from the Caucasus and Crimea. Geological Institute A.I. Dzhanelidze, Academy of Sciences of Georgian SSR, Trudy (n.s.) 74:3–166 (in Russian)Google Scholar
- Bucur II, Săsăran E (2005) Micropaleontological assemblages from the Upper Jurassic–Lower Cretaceous deposits of Trascău Mountains and their biostratigraphic significance. Acta Paleont Rom 5:27–38Google Scholar
- Bucur II, Granier B, Krajewski M (2014) Calcareous algae, microbial structures and microproblematica from Upper Jurassic–lowermost Cretaceous limestones of southern Crimea. Acta Palaeont Rom 10:61–86Google Scholar
- Crescenti U (1969) Biostratigrafia delle facies Mesozoiche dell´Appennino Centrale: correlazioni. Geol Romana 8:15–40Google Scholar
- Della Porta G, Kenter JAM, Bahamonde JR, Immenhauser A, Villa E (2003) Microbial boundstone dominated carbonate slope (Upper Carboniferous, N Spain): microfacies, lithofacies distribution and stratal geometry. Facies 49:175–208Google Scholar
- Della Porta G, Merino-Tomé O, Kenter JAM, Verwer K (2013) Lower Jurassic microbial and skeletal carbonate factories and platform geometry (Djebel Bou Dahar, High Atlas, Morocco). Publication, SEPM Special, p 105Google Scholar
- Dragastan O (2010) Getic Carbonate Platform—Jurassic and Lower Cretaceous stratigraphy, reconstructions, paleogeography, provinces and biodiversity. Ed Univ Bucureşti, 621 pp (in Romanian with English abstract)Google Scholar
- Edwards DE, Riding R (1991) Mid-Phanerozoic microskeletal-microbial reef frameworks. In: 5th International symposium on fossil algae, Capri, 7–12 April 1991, abstracts volume, pp 20–21Google Scholar
- Flügel E (1981) “Tubiphyten” aus dem fränkischen Malm. Geol Bl Nordost-Bayern angr Gebiete 31:126–142Google Scholar
- Flügel E (2002) Triassic reef patterns. In: Kiessling W, Flügel E, Golonka J (eds) Phanerozoic reef patterns. SEPM Special Publication, Tulsa, pp 735–744Google Scholar
- Geister J, Lathuilière B, Yudin S (2007) Late Jurassic coral reefs and their paleo-relief at Sudak (South coast of Cromea Peninsula, Ukraine). In: Kossovaya O, Somerville I, Evdokimova I (eds) X International Congress on Fossil Cnidaria and Porifera, August 12–16, 2007, St. Petersburg, Russia-Abstracts: 38. St. PetersburgGoogle Scholar
- Guo L, Vincent SJ, Lavrishchev V (2011) Upper Jurassic reefs from the Russian western Caucasus: implications for the eastern Black Sea. Turk J Earth Sci 20:629–653Google Scholar
- Hoffmann M, Kołodziej B, Skupien P (2017) Microencruster-microbial framework and synsedimentary cements in the Štramberk Limestone (Carpathians, Czech Republic): insights into reef zonation. Ann Soc Geol Polon 87:325–347Google Scholar
- Ivanova D, Kołodziej B, Koleva-Rekalova E, Roniewicz E (2008) Oxfordian to Valanginian palaeoenvironmental evolution on the western Moesian carbonate platform: a case study from SW Bulgaria. Ann Soc Geol Polon 78:65–90Google Scholar
- Kaźmierczak J, Hillmer G (1974) Sclerosponge nature of the Lower Hauterivian “Bryozoan” Neuropora pustulosa (Roemer, 1839) from Western Germany. Acta Palaeont Polon 19(4):443–453Google Scholar
- Krajewski M (2008) Lithology of the Upper Jurassic–Lower Cretaceous (Tithonian–Lower Berriasian) Ay-Petri reef complex (southern Ukraine, the Crimea Mountains). N Jb Geol Paläont Abh 5:298–312Google Scholar
- Krajewski M (2010) Facies, microfacies and development of the Upper Jurassic–Lower Cretaceous of the Crimean carbonate platform from the Yalta and Ay-Petri massifs (Crimea Mountain, southern Ukraine). Dissertation Monographs 217 Wydawnictwa AGH, Kraków 253 ppGoogle Scholar
- Krajewski M, Olszewska B (2006) New data about microfacies and stratigraphy of the Late Jurassic Ay-Petri carbonate buildup (south-western Crimea Mountains, South Ukraine). N Jb Geol Paläont Abh, Mh 5:298–312Google Scholar
- Krajewski M, Olszewska B (2007) Foraminifera from the Late Jurassic and Early Cretaceous carbonate platform facies of the southern part of the Crimea Mountains, Southern Ukraine. Ann Soc Geol Polon 77:291–311Google Scholar
- Leinfelder RR, Krautter M, Laternser R, Nose M, Schmid DU, Schweigert G, Werner W, Keupp H, Brugger H, Herrmann R, Rehfeld-Kiefer U, Schroeder JH, Reinhold C, Koch R, Zeiss A, Schweizer V, Christmann H, Menges G, Luterbacher H (1994) The origin of Jurassic reefs: current research developments and results. Facies 31:1–56CrossRefGoogle Scholar
- Leinfelder RR, Werner W, Nose M, Schmid DU, Krautter M, Laternser R, Takacs M, Hartmann D (1996) Paleoecology, growth parameters and dynamics of coral, sponge and microbialite reefs from the Late Jurassic. Göttinger Arb Geol Paläont Sb 2:227–248Google Scholar
- Matyszkiewicz J (1997) Microfacies, sedimentation and some aspects of diagenesis of Upper Jurassic sediments from the elevated part of the Northern peri-Tethyan Shelf: a comparative study on the Lochen area (Schwäbische Alb) and the Cracow area (Cracow–Wielun Upland, Poland). Berliner Geo Abh E 21:1–111Google Scholar
- Matyszkiewicz J, Słomka T (2004) Reef-microencrusters association Lithocodium aggregatum – Bacinella irregularis from the Cieszyn limestones (Tithonian–Berriasian) of the Outer Western Carpathians (Poland). Geol Carpath 55:449–456Google Scholar
- Mileev VS, Baraboshkin EYu, Rozanov SB, Rogov MA (2006) Kimmerian and Alpine tectonics of Mountain Crimea. (English summary). Bull Moscow Soc Natur Geol Ser 8:22–33Google Scholar
- Muratov M.V. 1973. Geology of the Crimea Peninsula. (in Russian), vol. 2, Moskva 191 ppGoogle Scholar
- Nikishin AM, Wannier M, Alekseev AS, Almendinger OA, Fokin PA, Gabdullin RR, Khudoley AK, Kopaevich LF, Mityukov AV, Petrov EI, Rubtsova EV (2015b) Mesozoic to recent geological history of southern Crimea and the Eastern Black Sea region. In: Sosson M, Stephenson RA, Adamia SA (eds) Tectonic Evolution of the Eastern Black Sea and Caucasus. Geological Society, Spec Pub 428, London, pp 241–264Google Scholar
- Oszczypko N, Ślączka A, Bubniak I, Olszewska B, Garecka M (2017) The position and age of flysch deposits in the Crimean Mountains (Southern Ukraine). Geol Quart 61:697–722Google Scholar
- Popa L, Panaiotu CE, Grădinaru E (2014) An early Middle Anisian (Middle Triassic) Tubiphytes and cement crusts-dominated reef from North Dobrogea (Romania): facies, depositional environment and diagenesis. Acta Geol Polon 64:189–206Google Scholar
- Schmid DU (1995) “Tubiphytes” morronensis—eine fakultativ inkrustierende Foraminifere mit endosymbiontischen Algen. Profil 8:305–317Google Scholar
- Schmid DU (1996) Marine Mikrobolithe und Mikroinkrustierer aus dem Oberjura. Profil 9:101–251Google Scholar
- Senowbari-Daryan B, Bucur II, Schlagintweit F, Săsarăn E, Matyszkiewicz J (2008) Crescentiella, a new name for “Tubiphytes” morronensis Crescenti, 1969: an enigmatic Jurassic–Cretaceous microfossil. Geol Croatica 61(1–2):185–214Google Scholar
- Strzeboński P, Kowal-Kasprzyk J, Olszewska B (2017) Exotic clasts, debris flow deposits and their significance for reconstruction of the Istebna Formation (Late Cretaceous–Paleocene, Silesian Basin, Outer Carpathians). Geol Carpath 68:562–582Google Scholar
- Termier G, Termier H, Ramalho M (1985) Spongiofaunes du Jurassique Supérieur du Portugal. Com Serv Geol Portugal 71(2):197–222Google Scholar
- Wood R (1999) Reef evolution. Oxford University Press, Oxford, p 354Google Scholar
- Yudin VV, Arkadiev VV, Yurovsky YuG (2015) “Revolution” in geology of Crimea (in Russian with English summary). Viestnik SPGU 7:25–37Google Scholar
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