Planktonic Biota Constituents Responses to Global Sea-Level Changes Recorded in the Uppermost Albian to Middle Cenomanian Deep-Water Facies of the Outer Carpathians

: Interpretations of sea-level changes over geological time are mainly based on analyses of sediments deposited within stable platforms. One of the criteria for recognizing these changes is the composition of skeleton-bearing protists living in environments close to the shoreline and on the continental shelf. It can be assumed that the source of information about sea-level changes may also be found in assemblages of microfossils redeposited from the shelf to the marginal ocean basin. With such an assumption, this article presents an interpretation of changes in marine plankton communities (radiolarians and planktonic foraminifera), which during late Albian–middle Cenomanian were redeposited with carbonate mud by gravity currents from the peri-Tethyan shelf to the northern, marginal Silesian Basin of the Western Tethys. Planktonic biota identiﬁed in sediments deposited by gravity ﬂows and those found in hemipelagic shales separating them, indicate that their composition may be correlated with eustatic changes in the sea level from the late Albian (KAl8) to middle Cenomanian (KCe3). physico-geographical mesoregion of Poland, covering a fragment of the Beskidy foreland, located between the Wieprz ó wka and Raba valleys. The sediments


Introduction
The late Albian through middle Cenomanian period is characterized by a stepwise sea level rise that led to one of the highest sea levels recorded in the history of the Earth [1]. These long-term processes caused the development of wide epicontinental seas in the Northern hemisphere with variable pelagic carbonate lithofacies and biogenic siliceous sponge facies [2]. The short-term sea-level fluctuations are estimated at approximately 25-75 m (KAl8-Kce3; [1]), and resulted in stepwise environmental changes on shelves, both in the water column and on the seabed. They caused biotopes migration, and altered biogenic production, therefore shifting each facies areas coverage.
To interpret sea-level changes in the geologic past, planktonic foraminifera and polycystine radiolarians can be applied as palaeoenvironment indicators. Even as redeposited micro-constituents, these genera still display an obvious relationship to the specific water temperature, and thus indicate zones in the water column where they inhabited. Differences in the availability of food, nutrients supply and oxygenation may be additional factors influencing the water depth preferred by a group of organisms (e.g., [3][4][5]).
The usefulness of planktonic foraminifera in interpreting sea-level changes is based on a depth zonation model successfully applied to modern and fossil morphotypes (e.g., [6][7][8]), and it is widely used for palaeoenvironmental analyses applied to regions with carbonate sedimentation, in either the deep ocean or in epicontinental seas (e.g., [9][10][11]). Such interpretations are limited by the abundance of foraminiferal shells which dramatically  [27] in its Polish part. (B) Detailed geological map of the studied area (a part of the Outer Carpathians after [28]) with location of the study area (Barnasiówka-Jasienica quarry; B-J). (C) Albian-Cenomanian lithostratigraphic scheme of the Silesian Nappe in the Outer Carpathians (after [29][30][31][32]).

General Outline
The studied section of the upper Albian-middle Cenomanian is a mix of siliciclastic and calcareous deep sea deposits occurring in the Polish part of the Outer Western Carpathians ( Figure 1A,B), which comprises several units (nappes and thrust-sheets), regarded as remnants of oceanic basins. They were folded and thrust mainly in the middle and late Miocene (e.g., [33,34]) as a result of an oblique convergence between the Eurasian Plate and the Alcapa superterranes (e.g., [35]). The Silesian Nappe is now one of the core nappes of the Outer Carpathians which consists of a succession of the Upper Jurassic through Miocene sediments, mainly siliciclastic deposits of gravity flows (e.g., [36]).
During the Cretaceous to Paleogene interval, the deposits of the Silesian Nappe, predominately deep-water, siliciclastic turbidites (locally debris flow deposits-debrites) were laid down in the Silesian Basin which was a long and deep trough opened (as a result of rifting) along its southern margin (e.g., [36,37]). This basin was bordered on the northeast by the Subsilesian (submerged) Ridge and on the southwest-by the Silesian Ridge [34,36,38].
The late Albian and Cenomanian was a time interval when shallow, wide epicontinental seas located on the European peri-Tethyan shelves, north on the Silesian Basin were the places of carbonate sedimentation (e.g., [18,39]) overgrown by lush sponge  [27] in its Polish part. (B) Detailed geological map of the studied area (a part of the Outer Carpathians after [28]) with location of the study area (Barnasiówka-Jasienica quarry; B-J). (C) Albian-Cenomanian lithostratigraphic scheme of the Silesian Nappe in the Outer Carpathians (after [29][30][31][32]).

General Outline
The studied section of the upper Albian-middle Cenomanian is a mix of siliciclastic and calcareous deep sea deposits occurring in the Polish part of the Outer Western Carpathians ( Figure 1A,B), which comprises several units (nappes and thrust-sheets), regarded as remnants of oceanic basins. They were folded and thrust mainly in the middle and late Miocene (e.g., [33,34]) as a result of an oblique convergence between the Eurasian Plate and the Alcapa superterranes (e.g., [35]). The Silesian Nappe is now one of the core nappes of the Outer Carpathians which consists of a succession of the Upper Jurassic through Miocene sediments, mainly siliciclastic deposits of gravity flows (e.g., [36]).
During the Cretaceous to Paleogene interval, the deposits of the Silesian Nappe, predominately deep-water, siliciclastic turbidites (locally debris flow deposits-debrites) were laid down in the Silesian Basin which was a long and deep trough opened (as a result of rifting) along its southern margin (e.g., [36,37]). This basin was bordered on the northeast by the Subsilesian (submerged) Ridge and on the southwest-by the Silesian Ridge [34,36,38].
The late Albian and Cenomanian was a time interval when shallow, wide epicontinental seas located on the European peri-Tethyan shelves, north on the Silesian Basin were the places of carbonate sedimentation (e.g., [18,39]) overgrown by lush sponge communities (e.g., [40]). The material originated from the destruction of these sponge assemblages, predominately lithistids (e.g., [41,42]), and carbonate microconstituents were gradually washed away and redeposited into deep marginal basins of the Carpathians, forming wide turbidite bodies in the sea floor of the Subsilesian [24], Silesian [18,22,30] and Skole [43] basins. Currently, extensive spicule-rich turbiditic series containing mixed siliciclastic and calcareous deposits occur in the Outer Carpathian nappes in the Czech and Polish Carpathians and continue further east in the Silesian-Chornohora nappe of the Ukrainian Carpathians (e.g., [44][45][46]).

Lithostratigraphy, Biostratigraphy and Chemostratigraphy
These mixed siliciclastic and calcareous deposits belong to three lithostratigraphic units of the Silesian Nappe ( Figures 1C, 2  Previous lithostratigraphic, microfacial and palaeontological investigations showed the main features of these units and their stratigraphic position [21,22,31,32]. These are fine-grained turbidities consisting of detrital material mixed with biogenic particles, which are predominantly siliceous spicules of Demospongiae. This group is represented predominately by orders Lithistida, Hadromerida and Astrophorida [18]. Redeposited material is intercalated with hemipelagic non-calcareous shales (Figures 2 and 3) which include, among the microfossils, only radiolarians and deep-water agglutinated foraminifera (DWAF). The numerous redeposited biogenic grains start to appear in turbidites from the upper part of the MLB but the huge mass of spicule-rich particles and other bio-clasts are the main components of the overlying MCB [21,22,32].
Based on the radiolarian data, the succession studied is mostly correlated with the Holocryptocanium barbui radiolarian Zone (Figure 4), previously distinguished in the pelagic facies of the Pieniny Klippen Belt of the Carpathian domain [47]. The lower limit of this Zone is not specified in the studied deposits. The upper limit is marked by the first occurrence (FO) of Hemicryptocapsa prepolyhedra Dumitrică (the index species of the H. prepolyhedra radiolarian Zone [47], found 3.8 m above the upper boundary of the MCB ( Figure 4). Hemicryptocapsa prepolyhedra Dumitrică is a cosmopolitan species in the Western Tethys, thus, the base of this Zone is a correlation level recognized in various basins of the Carpathian realm [25,43] and corresponds to an interval between the Mid Cenomanian Event 1 and the Oceanic Anoxic Event 2 (discussion in [32,[48][49][50]).
The biotic marker pointing the lower part of the succession studied is the last occurrence (LO) of an DWAF species Plectorecurvoides alternans Noth noted 1.4 m above the lower boundary of the MCB (Figure 4). The total range of this species delimits the P. alternans Interval Zone [51] commonly used in the Western Tethyan deep-water successions (summary in [52]), which indicates that the MCB lower boundary may correspond to the uppermost Albian. The overlying sediments of the MCB and Barnasiówka Radiolarian Shale Formation belong entirely to the Bulbobaculites problematicus (Neagu) agglutinated foraminiferal Interval Zone ( Figure 4). The FO of this index species is close to the base of the MCB.
Combined biostratigraphic and chemostratigraphic (δ 13 C org ) studies allowed to date these mixed siliciclastic and calcareous deposits enriched in sponge spicules as the latest Albian through the middle Cenomanian, and distinguished the isotope excursions characteristic for this interval [32], as the Albian-Cenomanian Boundary Interval containing the OAE1d, and the Mid-Cenomanian Event containing the MCE Ia, MCE Ib and ?MCE II ( Figure 4). The base of the MCB corresponds to the top of OAE1d, whereas the top of this lithostratigraphic unit occurs between the MCE Ib and MCE II.    . Lithological log of the Barnasiówka-Jasienica section, Silesian Nappe, Outer Carpathians plotted against the main radiolarian and foraminiferal stratigraphic markers, and δ 13 Corg curve containing a range of the main carbon isotope events (after [32]). The position of the subsection studied is also presented. U. praejankoi-Uvigerinaminna praejankoi Agglutinated Foraminifera Zone; H. p.-Hemicryptocapsa polyhedra Radiolarian Zone, H. prepolyhedra-Hemicryptocapsa prepolyhedra Radiolarian Zone.

Sampling
The studied succession is outcropped in the central part of the Silesian Nappe of the Western Outer Carpathians ( Figure 1B,C), in the Barnasiówka Ridge, and is a part of the Wieliczka Foothills-a physico-geographical mesoregion of Poland, covering a fragment of the Beskidy foreland, located between the Wieprzówka and Raba valleys. The sedi- . Lithological log of the Barnasiówka-Jasienica section, Silesian Nappe, Outer Carpathians plotted against the main radiolarian and foraminiferal stratigraphic markers, and δ 13 C org curve containing a range of the main carbon isotope events (after [32]). The position of the subsection studied is also presented. U. praejankoi-Uvigerinaminna praejankoi Agglutinated Foraminifera Zone; H. p.-Hemicryptocapsa polyhedra Radiolarian Zone, H. prepolyhedra-Hemicryptocapsa prepolyhedra Radiolarian Zone.

Sampling
The studied succession is outcropped in the central part of the Silesian Nappe of the Western Outer Carpathians ( Figure 1B,C), in the Barnasiówka Ridge, and is a part of the Wieliczka Foothills-a physico-geographical mesoregion of Poland, covering a fragment of the Beskidy foreland, located between the Wieprzówka and Raba valleys. The sediments are exposed at the Barnasiówka-Jasienica quarry with conducted mining (N 49 •  A total of 300 rock samples has been taken for different studies. The digging and site access permits of these rock samples were not required. All processed rock material (as labeled residue) is stored in the Department of Geology of the Institute of Geography, Pedagogical University of Krakow, Poland.

Microfacies Analysis
Microfacies analysis of the deposits studied has been determined using 126 thin sections of the rocks taken along the whole 43-m thick section. High-resolution microfacies observations, were made lamina by lamina, for the Mikuszowice Chert Beds. The biogenicrich sediments contain numerous planktic biota. They have been made in 41 thin sections related to samples taken continuously along five subsections (A-E; Figure 2). Each of them comprises ca. 1.2-1.8 m thick succession of turbidite and hemipelagic deposits. Counting of the micro-constituent proportions was made according to the method described in [5]. Whole section views were subdivided arbitrary on micro-areas as subsequent fragments of sediment parallel to each other, which vary in thickness from 0.1 to 0.5 mm and were examined under a light microscope at magnification 50× ( Figure 5). Percentage abundance data of radiolarians and planktonic foraminifera were estimated over the total field of view and estimated using the diagrams of Baccelle and Bosellini [53]. Such counting was made in each of the successive 1750 micro-areas from subsections A-E. Microfacies and microconstituents have been photographed with a polarizing microscope (Nikon Eclipse 100 POL) in the Department of Geology of the Institute of Geography (Pedagogical University of Krakow).

Micropalaeontological Analysis
Radiolarians and planktonic foraminifera were taxonomically recognized and counted from the residues obtained after chemical rock sample disintegration. The occurrence of recognized assemblages in this study has been supplemented by data from previous research carried out in the Barnasiówka-Jasienica quarry before reactivation of its operation in 2015 [21,31,54,55].
Planktonic microfossils were extracted from 161 samples taken along the section. The samples of about 0.3-1 kg and of different lithologies as siliciclastics, carbonates, and cherts were used during this study. Each sample was first broken into pieces 1-2 cm across. The following procedures depended on the lithology of the sample. Mudstones and silty shales were soaked in hot solution of Glauber's salt (Na 2 SO 4 ) and heated, usually several dozen times. In case of marly shale and limestone, microfossils were freed by dissolving the rock matrix in hot acetic acid, by keeping the sample soaked with fully concentrated acid at a maximum temperature of 80 degrees Celsius for 4-6 h [56]. Chert and silicified limestone were treated with hydrochloric and hydrofluoric acids, respectively, according to the procedure described in [57]. After chemical preparation, the samples were washed over a 63-µm sieve and dried. The residue was completely picked for microfauna, which was present in residue of 125 samples (Table S1). For taxonomic studies we also used 41 thin sections taken from five subsections for microfacies analysis.  Selected specimens were photographed using a scanning microscope at the Institute of Geological Science, Jagiellonian University, Kraków. All micropalaeontological analyses have been made in the Geological Laboratory at the Department of Geology of the Institute of Geography (Pedagogical University of Krakow).

General Sedimentary Features of Turbidites
The Middle Lgota Beds (MLB) consist mostly of thin-and medium-bedded, siliceous, dark, fine-grained sandstones, intercalated with black, grey, green and spotty non-calcareous claystones ( Figure 3A-C). The analysis of carbon stable isotope data [32] showed that the uppermost part of these MLB sequence and the lowermost part of the MCB correspond to the oceanic anoxic event 1d (OAE1d) (Figure 4). The base of this succession with abundant biotic particles, redeposited from peri-Tethyan shelf occurs in the upper part of this carbonisotope unit. It is characterized by increasing admixture of loose sponge spicules which could be visible only in thin sections.
The Mikuszowice Chert Beds (MCB) are composed of mm to cm-thick siliciclastic to calcareous partly silicified, fine-grained flysch deposits, which represent predominantly T bde intervals of the Bouma sequence ( Figure 3D-G). The most striking feature of these deposits, visible only in thin sections, is the high content of siliceous sponge spicules. Other biogenic micro-constituents are planktonic and benthic calcareous foraminifera, inoceramid prisms and, sporadically, fragmented coralline algae and echinoid spines. Radiolarians are present in the MCB despite of the later diagenetic remobilization of biogenic silica and formation of bluish chert layers (summary in [18,22]). The carbon stable isotope analysis identified the upper part of the MCB corresponding to the Mid-Cenomanian event Ia and Ib ( Figure 4) [32,49]. The uppermost part of this unit passes gradually into the lower part of the BRSF which differs from MCB by the lack of chert layers. The lower part of the BRSF (9.7 m thick) consists of thin-to medium-bedded (up to 25 cm) calciturbidites and siliciclastic silty and fine-grained sandy turbidites with intercalations of non-calcareous green and black, partly hemipelagic siltstones.

Microfauna in Microfacies Record-Content and Preservation
Analysis of microfacies shows that these deposits are predominantly mud-supported and consist of microfaunal/microfloral allochems, quartz and lithic clasts, micrite, clay minerals and/or dispersed organic matter. Biogenic particles contain planktonic and benthic calcareous foraminifera, radiolarians, deep-water agglutinated foraminifera, and sporadically, fragmented coralline algae, echinoid spines and inoceramid prisms. Diversity of biotic and lithic clasts and their volume in relation to the matrix and cement type allowed to determine various microfacies in these deposits. Four microfacies types are distinguished in the centimeter scale ( Figure 6) containing: (1) sublitharenite, (2) spiculites containing predominately spicules of siliceous sponges, (3) biomicrite with predominately foraminifera and/or radiolarians, and (4) hemipelagic siltstones (Figures 6 and 7). foraminifera, and sporadically, fragmented coralline algae, echinoid spines and inoceramid prisms. Diversity of biotic and lithic clasts and their volume in relation to the matrix and cement type allowed to determine various microfacies in these deposits. Four microfacies types are distinguished in the centimeter scale ( Figure 6) containing: (1) sublitharenite, (2) spiculites containing predominately spicules of siliceous sponges, (3) biomicrite with predominately foraminifera and/or radiolarians, and (4) hemipelagic siltstones ( Figures 6 and 7).  This microfacies in thin section view ( Figure 6A,B) is composed predominately of quartz (up to 85%), usually angular in shape. Radiolarians and planktonic foraminifera content do not exceed 5% of this microfacies. They are also rarely present in the residuum

Sublitharenite
This microfacies in thin section view ( Figure 6A,B) is composed predominately of quartz (up to 85%), usually angular in shape. Radiolarians and planktonic foraminifera content do not exceed 5% of this microfacies. They are also rarely present in the residuum after chemical disintegration of this lithotype. The specimens of planktic biota present there are very poorly preserved and recrystallized. This rock includes also about 1% of benthic foraminifera occurring as moulds, usually infilled by calcite cement. Sizes of the tests and skeletons vary between 30 and 150 µm. Specimens in separated material are moderately to poorly preserved. Among radiolarians, specimens from the family Williriedellidae dominate there (Figure 8). Some species from genus Praeconocaryomma are also present. Among planktonic foraminifera, forms from the genera Hedbergella and Heterohelix were observed ( Figure 9).

Spiculite
Spiculite microfacies ( Figure 6C,D) contains up to 90% of spicules of siliceous sponges which are usually calcified. Other micro-constituents are foraminifera (planktonic and benthic), radiolarians, and rare detrital grains of quartz and glauconite. This type of sediment could be chaotically packed or micro-constituents might be arranged in parallel laminae on millimeter scale, separated by less than 1 mm thick seams. Those seams which are matrix-supported and more clayey consist up to 30% of radiolarians. Microfossil tests and skeletons within the seams are partly filled with spheroidal grains of opaque minerals, 3-10 μm in diameter being pyrite framboids. Better preserved

Spiculite
Spiculite microfacies ( Figure 6C,D) contains up to 90% of spicules of siliceous sponges which are usually calcified. Other micro-constituents are foraminifera (planktonic and benthic), radiolarians, and rare detrital grains of quartz and glauconite. This type of sediment could be chaotically packed or micro-constituents might be arranged in parallel laminae on millimeter scale, separated by less than 1 mm thick seams. Those seams which are matrix-supported and more clayey consist up to 30% of radiolarians. Microfossil tests and skeletons within the seams are partly filled with spheroidal grains of opaque minerals, 3-10 µm in diameter being pyrite framboids. Better preserved specimens of radiolarians belong to the family Williriedellidae (Figure 8), while the planktonic foraminifera belong to the genera Hedbergella and Heterohelix (Figure 9).

Foraminiferal and Radiolarian Biomicrite/Biosparite
Microfacies that contain predominately foraminiferal tests and/or radiolarian skeletons ( Figures 7A-C, 8 and 9) occur in the whole succession studied but become more frequent in the upper part of the MCB. Pure foraminiferal biomicrite/biosparite consists mostly of benthic and planktonic foraminifera, but the calcareous benthic foraminiferal tests prevail, reaching a maximum content of up to 30%. In some of the laminae planktonic species dominate; they belong mostly to hedbergellids. There is a very low radiolarian skeletons admixture in this type of microfacies (up to 1%), but radiolarians are commonly present in the radiolarian biomicrite/biosparite microfacies. A few such layers, up to 15 cm thick, occur also in the upper part of the MCB. Macroscopically, these layers consist of dark-grey allodapic limestone corresponding to T d intervals ( Figure 7C). The grain framework of this rock consists exclusively of biogenic components, which makes up 10 to 60% of the whole rock. Radiolarians are present in these rocks as voids after skeletons, secondarily filled by sparry calcite ( Figure 7C). Other biogenic components are tests of planktonic foraminifera which are in the minority. Radiolarians vary in size from 30 to 300 µm. Foraminifer tests are very small, usually less than 50 µm. Rare forms with single keel among the planktonic foraminifers (Thalmannamina/Rotalipora/Praeglobotruncana) were observed in some foraminiferal biomicrites.

Hemipelagic Siltstone to Claystone
Hemipelagic siltstone to claystone ( Figure 7D) contains radiolarians and deep water agglutinated foraminifera. Radiolarian skeletons are present in each type of clay layers. Their total abundance in green hemipelagites fluctuates from 0 to 40% while, in black and grey pelagites do not exceed 10%. Radiolarian skeletons are very small, with the widest dimension usually below 30 µm. Larger skeletons are rare. Radiolarians are moderately to poorly preserved. Most skeletons have been recrystallized and are now replaced by pyrite or Fe-oxides resulting in the obliteration of their external and internal wall structures. Only ca. 20% of skeletons are identifiable; Holocryptocanium, Cryptamphorella and Praeconocaryomma predominate among the recognizable individuals.

Analysis of Relative Abundance of Radiolarian Assemblage
For this analysis, samples taken along the entire section every few to several centimeters were used. Radiolarian assemblages are the most diversified among planktonic biota found in thin sections as well as in rock residue left after rock dissolution. In the section studied, the samples yielded in total a relatively well-preserved radiolarian assemblages consisting of 26 species and corresponding to 18 genera (Table S1; Figure 8). The most frequent species belong to the genera Holocryptocanium, Cryptamphorella and Hemicryptocapsa, among the nassellarids, and the genus Praeconocaryomma among the spumellarids. The order Entactinaria is represented by one genus (Quinquecapsullaria) which contains two species. The nassellarian species that belong to the family Williriedellidae are the main components of the radiolarian assemblages. Holocryptocanium barbui Dumitrică, Holocryptocanium tuberculatum Dumitrică and Praeconocaryomma lipmanae Pessagno are the most common species, comprising up to 90% of the total microfaunal assemblage. However, the majority of radiolarian species (23 taxa) in the whole assemblage belongs to rare species, which do not exceed 1% in relative abundance.
Identified radiolarians have been classified into radiolarian ecological groups defined for the Cenomanian Western Tethyan deposits [50] (Table S1). Thirteen species represent the B supergroup which were interpreted as deep dwelling taxa ( Figure 10) and which preferred nutrient-rich eutrophic conditions. Amongst the species of this group, Holocryptocanium barbui Dumitrică dominates quantitatively, comprising up to 85% of the total microfaunal assemblage. This species is commonly present in spiculites and hemipelagic and pelagic claystones. The frequency of H. barbui Dumitrică coincides with radiolarian dominance and culminates within the upper part of the MCB (32%) and in the lowermost part of the BRSF, with the maximum value of 75.5%. Identified genera that belong to radiolarian ecological groups [50] which could tolerate increased nutrient content are Squinabollum fossile (Squinabol) (group B2), Diacanthocapsa ovoidea Dumitrică (B2), Dictyomitra montisserei (Squinabol) (B2), Cryptamphorella conara (Foreman) (B2), Xitus mclaughlini (Pessagno) (B5), Thanarla veneta (Squinabol) (B5) and Holocryptocanium geysersensis Pessagno (B6). Ten species have been classified to the radiolarian ecological supergroup E. This group assembled species which lived predominately in surface waters and preferred oligotrophic conditions ( Figure 10). pelagic and pelagic claystones. The frequency of H. barbui Dumitrică coincides with radiolarian dominance and culminates within the upper part of the MCB (32%) and in the lowermost part of the BRSF, with the maximum value of 75.5%. Identified genera that belong to radiolarian ecological groups [50] which could tolerate increased nutrient content are Squinabollum fossile (Squinabol) (group B2), Diacanthocapsa ovoidea Dumitrică (B2), Dictyomitra montisserei (Squinabol) (B2), Cryptamphorella conara (Foreman) (B2), Xitus mclaughlini (Pessagno) (B5), Thanarla veneta (Squinabol) (B5) and Holocryptocanium geysersensis Pessagno (B6). Ten species have been classified to the radiolarian ecological supergroup E. This group assembled species which lived predominately in surface waters and preferred oligotrophic conditions ( Figure 10). Spumellaria is less frequent than Nassellaria in the studied assemblage. It composes 20 to 50% of the total number of radiolarian specimens. The species belong mainly to two families: Actinommidae and Hagiastridae. Hagiastrids were probably symbiont-bearing species living in oligotrophic conditions [5,15,50]. Representatives of the family Actinommidae, such as Praeconocaryomma lipmanae Pessagno are the most frequent, with the maximum value up to 60% of the total assemblage. This species (E3 ecological group) could tolerate increased nutrient input but preferred an open marine oligotrophic environment [50]. Species such as Gongylothorax siphonofer Dumitrică and Hemicryptocapsa tuberosa Dumitrică (NC group) are rare in the Tethys, but are known from the Carpathian basins [24]. Spumellaria is less frequent than Nassellaria in the studied assemblage. It composes 20 to 50% of the total number of radiolarian specimens. The species belong mainly to two families: Actinommidae and Hagiastridae. Hagiastrids were probably symbiont-bearing species living in oligotrophic conditions [5,15,50]. Representatives of the family Actinommidae, such as Praeconocaryomma lipmanae Pessagno are the most frequent, with the maximum value up to 60% of the total assemblage. This species (E3 ecological group) could tolerate increased nutrient input but preferred an open marine oligotrophic environment [50]. Species such as Gongylothorax siphonofer Dumitrică and Hemicryptocapsa tuberosa Dumitrică (NC group) are rare in the Tethys, but are known from the Carpathian basins [24].

Qualitative Analysis of Planktonic Foraminiferal Assemblages
Planktonic foraminiferal assemblages are poorly diversified among planktonic biota found in thin sections. The samples yielded in total relatively well-preserved tests consisting of 9 genera (Table S1) (Figure 9). Their species affiliation is difficult to determine due to the limited number of cross sections, especially for single forms visible in thin sections of the rock. Nevertheless, the most frequent are low trochospiral forms belonging to hedbergellids; mainly from species Muricohedbergella delrioensis (Carsey), subordinary-M. planispira (Tappan), and Clavihedbergella simplex (Morrow). They are associated by biserial forms belonging to heterohelicids from species Planoheterohelix moremani (Cushman). Other planktonic foraminifera have been determined as single specimens representing Guembelitria cenomana (Keller), Globigerinelloides ultramicrus (Subbotina), Whiteinella baltica Douglas and Rankin, Praeglobotruncana sp., and rotaliporids. The latter group contains taxa characteristic of the Cenomanian (?Thalmanninella apenninica (Renz), Th. greenhornensis (Morrow), Th. reicheli (Mornod), Rotalipora cushmani (Morrow)).
The largest content of planktonic foraminifera among bio-and lithogenic components in turbidites characterizes biomicrites that have a character of wakestones. They are accompanied by numerous benthic foraminifera, mainly of the genera Gavelinella, Lingulogavelinella, and Gyroidinoides, as well as individual calcareous algae and fragments of echinoderms. Single tests (larger in size) are also found in spiculites and sublitharenites. Single foraminifera were also found in claystones constituting the T e element of the Bouma sequence in turbidites.

Percentage Quantity of Planktonic Microfossils
The percentage quantity of radiolarians and planktonic foraminifera on a background of all microfacies constituents have been counted in all of the 1750 micro-areas from selected subsections (A-E) in the section studied ( Figure 11). The radiolarian never exceeds values of 3% in the subsections A-C. In the subsection D, their content increases up to 5% in samples corresponding to the MCE Ib deposits. Above this event, radiolarian quantity increases gradually, reaching a maximum value of 7.5% in the subsection E.
Planktonic foraminifera are a minor component of turbidites in the studied succession, and they are absent among hemipelagic deposits. The lowest values do not exceed 5% are noted in micro-laminae of subsections A and B. The higher values (up to 10%) are observed in the subsections D and E. The maximum quantity of 30% is noted in the middle part of the subsection C. The increased amount of planktonic foraminifera occurs also among the redeposited particles in the sediments corresponding to the OAE1d and to the younger part of the MCE Ib. Minerals 2022, 12, x FOR PEER REVIEW 18 of 27 Figure 11. Changes in planktonic microfossils and other components of sandstones presented in the studied segments of the lower-middle Cenomanian sediments of the Silesian Nappe, Outer Carpathians in relation to eurybathic/eustatic cycles sensu Haq [1]. Note that the correlation of the section studied with the sea-level curve is presented after [32].

Record of Sea Level Change
Our previous studies of the age of these sediments, based on analyses of carbon stable isotopes and micropalaeontological data, mostly related to abundance of sponge spicules [32] showed that the beginning of mixed siliciclastic and calcareous turbidites sedimentation, coinciding with the onset of increased supply of sponge spicules to the Silesian Basin, corresponds to the OAE1d. On this basis, we interpret that the sediments of the subsection A, partially corresponding to the youngest phase of the OAE1d, were accumulated at the beginning of a global regressive event KAl8 sensu Haq [1]. The proportion of microfacies, and above all the high content of biomicrites (on average 43.4%; Figure 11), indicate a relatively high sea level during the redeposition of calcareous micro-constituents from the shelf. This suggests that these sediments represent the early Figure 11. Changes in planktonic microfossils and other components of sandstones presented in the studied segments of the lower-middle Cenomanian sediments of the Silesian Nappe, Outer Carpathians in relation to eurybathic/eustatic cycles sensu Haq [1]. Note that the correlation of the section studied with the sea-level curve is presented after [32].

Record of Sea Level Change
Our previous studies of the age of these sediments, based on analyses of carbon stable isotopes and micropalaeontological data, mostly related to abundance of sponge spicules [32] showed that the beginning of mixed siliciclastic and calcareous turbidites sedimentation, coinciding with the onset of increased supply of sponge spicules to the Silesian Basin, corresponds to the OAE1d. On this basis, we interpret that the sediments of the subsection A, partially corresponding to the youngest phase of the OAE1d, were accumulated at the beginning of a global regressive event KAl8 sensu Haq [1]. The proportion of microfacies, and above all the high content of biomicrites (on average 43.4%; Figure 11), indicate a relatively high sea level during the redeposition of calcareous micro-constituents from the shelf. This suggests that these sediments represent the early lowstand systems tract. Consequently, the overlying sediments of the subsection B are interpreted as accumulated during the maximum of regression, related to the same KAl8 sea-level cycle. This is evidenced by the particularly high content of spiculites among microfacies in sandy-silty turbidites (~70%), the highest in the entire succession studied (Figure 11). Additionally, the time interval that covers the accumulation of sediments from subsections A and "B" could correspond to the worldwide first-order regression cycle (discussion in [32]).
In relation to the third-order sea-level cycles, sediments of the subsection C, which represent upper lower Cenomanian (discussion in [32]), are interpreted as accumulated during sea-level highstand coinciding with the well-developed calcareous production on the shelf.
The highest part of the succession studied which contains subsections D and E marks the termination of accumulation of mixed siliciclastic and calcareous deposits which took place between two oceanic events, the MCE Ib and MCE II [32]. The detailed correlation is indicated on the upper part of the Acanthoceras rothomagense ammonite Zone, in the upper part of the middle Cenomanian. Such stratigraphic position of both subsections suggests that they coincide with the KCe3 eustatic event. These intervals mark also the gradual transgression within the KCe3 eustatic event, which is part of the world's first-order transgression [1] (Figure 11).

Microplankton Content in Relation to Sea Level Changes
The study of radiolarian and planktonic foraminifera occurring in various microfacies within the sequences of turbidite layers or in hemipelagic sediments (the later only for radiolarian skeletons) shows changes in their volume and taxonomic composition in relation to identified episodes of sea-level stand. This is because each of these two groups may react on environmental factors by increasing the number of specimens or completely disappearing. Referring to contemporary plankton communities and those known from the Cretaceous strata, the radiolarian and planktonic foraminiferal fluctuations could correspond to the chemistry and physical properties of the water column and nutrient availability, partly associated with sea-level changes, especially in a marginal part of the basins (e.g., [4,58]).

Planktonic Foraminifera Environmental Signal
In modern environments that constitute the background for the interpretation of the studied fossil communities, some morphological features of planktonic foraminifera, such as test shape, occurrence of spines, wall structure including size and spatial density of pores, are partly related to adaptation (e.g., [59,60]). The distribution of this group of plankton is controlled mainly by temperature, salinity, trophic conditions, and additionally-by sunlight, and predation in the upper water column (e.g., [61][62][63]). They all have an influence on water depth preference for particular species, which shifts during ontogeny, and seasonal preference (e.g., [64][65][66]). The relationships described above were used in palaeoecological models for Cretaceous groups of planktonic foraminifera, taking into account their water depth habitat. Small, globular (Globigerina-like) forms have been included to the shallow-dwelling assemblage, whereas large, flattened taxa with developed ridge (Globorotalia-like) were attributed to environment with greater depths (e.g., [67][68][69]). This model had also biogeographic implication, that is, shallow-dwelling forms should dominate in the Cretaceous epicontinental seas, whereas more diversified assemblages containing the deep-dwelling taxa should represent pelagic setting (e.g., [70]). Nevertheless, further analysis of planktonic foraminiferal assemblages using oxygen isotope studies (summary in [71]) showed changes in depth preferences for many taxa during the late Albian and early Cenomanian. This concerns a rapid adaptation across the Albian-Cenomanian transition (ACT) of Rotalipora (Thalmanninella)-like taxa (Th. globotruncanoides (Sigal), Praeglobotruncana stephani (Gandolfi)) to living at a surface habitat [71] and the decline of surface-dwelling Paracostellagerina libyca (Barr). This vertical migration to greater depths occurred also in the early Cenomanian within the Hedbergella delrioensis (Carsey). The changes in adaptive strategy may, at least in part, be related to collapse of the upper water column stratification around the OAE1d, suggested in [72]; however, the reasons for this could be varied including warming of intermediate [73] or cooling of surface water during an interval that started at the ACT [71].
The suggestion about the depth-reorganization of planktonic foraminifera after the OAE1d has been proposed based on the data from pelagic environments, mostly from the oceanic settings.
When we compare the proportions in the abundance of different planktonic foraminiferarich rocks derived from the epicontinental environment of the seas associated with the Tethys, another change can be seen in the sediments of the early and middle Cenomanian. An example of this is the Annopol section, known as "lagerstatte", which since the late Albian was connected to the Carpathian part of the Tethys via the Lviv Gate [74]. In the glauconite marls of the lower Cenomanian, rich in foraminiferal plankton, the abundance of small, globular forms decreased compared to the upper Albian, with a very slight increase in the abundance of high trochospiral forms with keel and pseudo-keel [75]. This could indirectly be evidence of thermal changes in waters in the early Cenomanian, however, a reduction in the sea level should also be taken into account here. The latter is indicated by the reversal of the plankton-benthos ratio at the Albian-Cenomanian Boundary Interval. In the lower Cenomanian, the proportion of limestone foraminifera benthos is twice that of planktonic foraminifera. Such plankton-benthos ratios have been documented from many profiles from epicontinental seas where a drop in sea level took place (discussion in [7]).
The reference of the abovementioned bathymetric models to the observed changes in redeposited assemblages of planktonic foraminifera in the studied upper Albian-middle Cenomanian succession is extremely difficult due to the low number of tests. However, we are trying to identify these changes in relation to the taxonomic composition and trends visible in the composition of foraminiferal assemblages. The dominance of Hedbergella-like forms in the entire studied succession, accompanied by biserial Planoheterohelix moremani (Cushman) is a typical record for this time interval, known from both pelagic and neritic zones. The low content of P. moremani (Cushman), an oligotrophic form (e.g., [76]), the episodic occurrence of triserial Guembelitria cenomana (Keller) reflecting shallow marine stressful environment (e.g., [77,78]), the lack of planktonic foraminifera bearing elongated chambers which were found very close to the OAEs sediments (e.g., [79]), and the lack of significant differences in the size of the tests in all forms rather excludes the presence of extreme or variable surface water conditions in the shelf sea.
Only two parameters are worth discussing here, i.e., the charts showing the change in the abundance of planktonic foraminifera in turbidite sediments and diagrams of changes in the percentage content of biomicrites in these facies. We interpret both elements in the context of spatial and temporal range of pelagic/neritic zone, which are related to abundance of nutrients and dissolved oxygen, water temperature, salinity and, above all, the depth of the shelf bottom affecting life of planktonic biota.
Characteristic here are (Table S1): (1) a small content of planktonic foraminifera in the succession corresponding to the OAE1d (with one positive peak), (2) almost complete lack of it in the succession above the OAE1d and in the lower part of the Lower Cenomanian, (3) the increase in the content of this group in the lower part of subsection C, which also contains layers of allodapic limestones (uppermost part of Lower Cenomanian), as well as (4) their slight increase in turbidites above the MCE 1, where the proportion of biomicrites is also increasing.
The record of slightly enhanced content of small, globular (Hedbergella-like) forms in sediments corresponding to the OAE1d may be result of an increase in sea surface temperature (SST). Such increase of SST during the early and middle phases of the OAE1d was documented both based on planktonic foraminiferal δ 18 O data from the western subtropical North Atlantic (Blake Nose at ODP sites 1050 and 1052; [80]), and calcareous nannoplankton data (Rhagodiscus asper Stradner abundance, calibrated with TEX 86 SSTs) from the deep carbonate platform in the Western Tethys (Umbria-Marche; [81]). One more factor should be added here, which favored the growth of planktonic foraminifera on the peri-Tethyan shelf, even if by increasing its area, i.e., the maximum of transgression during third-order eustatic level corresponded to the KAl8 cycle of Haq [1].
The almost complete lack of redeposited planktonic foraminifera in turbidites with the lowest content of biomicrite microfacies in the subsections A and B which correspond to the Albian-Cenomanian transition and the lower Cenomanian (without its upper part) is interpreted as the record of regression cycles of KAl8. We used here as a rule of thumb that the plankton/benthos ratio is a proxy reflecting the depositional water depth or distance to the coast (or both; e.g., [82,83]). While the increase in the content of redeposited planktonic foraminifera occurring in the lower part of the subsection C, associated by layers of allodapic limestones is probably related to the transgression cycles during the early Cenomanian (KCe1). Alternatively, it represents eurybathic sea-level shift, as a product of both local vertical movements and eustasy.
The abundance of redeposited planktonic foraminifera across the MCE Ia and MCE Ib is low and begins to rise above these chemostratigraphic events. The same trend was described from pelagic sediments in the Western Tethys (Umbria-Marche Basin; [84]), where taxonomic changes containing increases in the proportion of opportunistic taxa and round chambered pustulose forms while a reduction of the the number of K-mode specialists occurred just above the MCE.

Environmental Signal from Radiolarian Distribution in Water Column
Differentiation of radiolarians in the Carpathian deposits are generally low. It is a clearly visible trend if we compare the differentiation in the studied deposits of the Silesian Basin (26 species) and the differentiation in sediments from this time period in other basins of the Outer Carpathians, such as the Subsilesian and Skole basins (for comparisonsee [24,43]). A similar trend is visible in the basins of the Inner Carpathians, such as the Zliechov Basin [25,26], and in the Branisko [85] or Niedzica [23] subbasins, which were part of the Pieniny Klippen Basin. In all these locations, the number of identified species of radiolarians does not exceed fifty. At the same time, in deposits from the same age range but from the Umbria-Marche area located closer to the equator, the number of species present in these deposits is almost 200 (e.g., [50]). Such a difference in the number of species in radiolarian communities could result from the geographic location of the Carpathian basins, located more to the north in relation to the Umbria-Marche Basin or from the circulation of ocean currents carrying cooler waters [50]. In the Carpathian basins, which are generally deep, the presence of radiolarians in the sediment was certainly related to physical features of the water column, but also to a large extent by taphonomic factors [86]. However, the fact that individual species belong to different ecological groups makes it possible to use this taphonomically depleted assembles for environmental interpretations.
Low radiolarian diversity coupled with a high frequency of single taxon occurrence, which is observed in the Carpathian basins, might point to a period of the high nutrient content in the water column. Such tendency might be analogous to the modern oceans, where radiolarians tend to be less diverse in highly productive than in oligotrophic regions, although radiolarians are abundant then (e.g., [87,88]). In the studied deposits from the Silesian Basin, the radiolarian content strongly increases in the uppermost part of the MCB and BRSF, which corresponds to a transgressive trend toward the KCe3 event. Amongst the identified taxa, species of the genus Holocryptocanium dominates quantitatively comprising up to 85% of the total microfaunal assemblage. It suggests that the rounded shape of skeleton of this species belonging to the family Williriedellidae and their thick wall of abdominal chamber [89] favored their preservation even within redeposited material, however, their quantity linked to production in the water masses must have played the main role in their abundance. Holocryptocanium barbui Dumitrică is the dominant species in the studied assemblage. This species represents the radiolarian ecological group B (see [50]) that assembled species recognized as deep-dwelling forms. It also belongs to the subgroup B3 sensu [50] which contains only two radiolarian species preferring nutrient-rich waters with possible phosphorus-rich conditions [50]. There is a clear tendency in the investigated sediments that the rocks containing a large abundance of H. barbui Dumitrică species are primarily pelagic or hemipelagic sedimentation, while in biomicrites and spiculites derived from the shelf, H. barbui Dumitrică species are extremely rare, occurring only in a single sample from the subsections D and E corresponding to the interval of sea-level rise. Such a distribution of H. barbui Dumitrică individuals in the studied deposits confirms that this species occurred in the Silesian Basin as deep-dwelling form that lived probably below the thermocline, where waters rich in nutrients (phosphorus) accumulated. The numerous occurrences of H. barbui Dumitrică in the lower to middle Cenomanian rocks testifies to the continuous occurrence of such conditions at that time. On the other hand, in the lowest part of the section studied including the sediments of the uppermost Albian and the lowest part of the lower Cenomanian, there is a group of radiolarians with a small content of species of H. barbui Dumitrică. This has appeared to be the result a lower saturation with nutrients in the deeper zone of this basin and no general conditions for the existence of radiolarian plankton.
Another trend in the occurrence of the ecological subgroup B3 is visible in the upper part of the MCB and the lower part of the BRSF (subsections D and E). The biomicrites and spiculites occurring here come from the redeposition of the material from outer shelf and upper slope of the Silesian Basin during the rising sea level in the middle Cenomanian. The increase of H. barbui Dumitrică content in these deposits could be related to an increase of the sea level which enabled upwelling circulation along the marginal Silesian Basin that could deliver high-nutrient input to the outer shelf environment. The increase in the content of H. barbui Dumitrică also coincides with the lower input of detrital material and the increased thickness of hemipelagic siltstone and claystone layers. This may additionally suggest deepening of the outer shelf due to global transgression.
After counting all radiolarians taxa found in the samples, divided into deep-dwelling and surface taxa (Figure 10), it can be seen that the greatest diversity and number of them occur in connection with the MCE Ia, MCE Ib and ?MCE II events. Particularly high content of radiolarians from both groups occurred during the event MCE Ib. Taking into account the food preferences of individual groups of radiolarians, it can be assumed that this increased content of deep-water taxa could be related to a high content of nutrients in the deeper part of the water column, which under upwelling conditions, could supply surface waters, where the surface radiolarian group could develop. It is presumed that the development of radiolarians in the Silesian Basin was primarily influenced by periodic changes in the sea level. During the sea level low-stand, the area of shallows was restricted. Thus, recycling of nutrients could be restricted then mostly above the slope favored deep-water assemblages. During sea level rise, the shallow area became expanded and plankton production was beginning to spread to the shelf area being aided by costal upwelling (e.g., [90]). This could be related to the growth of deep-dwelling and shallow-water radiolarian assemblages observed in the sediments, occurring during periods of sea-level rise. This phenomenon may have been caused by an increased supply and recycling of nutrients between the deeper water zone in the Silesian Basin and the surface waters, activated or act more strongly in the periods of rising global sea levels. The question here arises, whether climate warming may significantly affect plankton growth in this process, and whether this factor contributes more to plankton growth than sea-level rise triggering the process of costal upwelling over a large area. The answer to this doubt may be the example from a region of Northwestern Africa, where the heaviest increase of nutrient input recorded as δ 15 N values was recorded in sediments directly related to a deglaciation period (between 12,000 years BP and the climatic optimum at 6000 yrs BP) but not at the warmest stage [91].

General Trends in Plankton Distribution in Relation to Sea Level
The effect of the nutrient content in the water column in relation to sea-level stand and content and proportions of hard-shelled plankton can be seen in the studied sediments by comparison of subsection C and E. The subsection corresponds to record of sea level high-stand, where planktonic foraminifera reach up to 30%. In the subsection E, the content of planktonic foraminifera increases (does not exceed 10%), which we interpret as the result of a transgressive cycle. For comparison, the content of radiolarians in the subsection C is low, while in the subsection E, it increases significantly. This tendency indicates a higher content of nutrients during transgression in the KCe3 cycle (subsection E), which is a likely factor in a greater growth of radiolarians, and at the same time, limits the development of foraminiferal plankton. Such a tendency is a known phenomenon from modern marine environments (e.g., [92]).
The increased frequency of planktonic foraminifera coinciding with the increased content of carbonates on the shelf surrounded the Silesian Basin which coincides with the period of at least the beginning of the long-term transgressive cycle. This period coincided with increased proliferation of calcareous benthic foraminifera in the shelf environment, which lasted during a period of acceleration of transgression and sedimentation of siltstones and claystones in the uppermost part of the MCB and lower part of the BRSF [18].

Conclusions
Taxonomic composition and trends in abundance of the tests (skeletons) of planktonic foraminiferal and radiolarian assemblages in the redeposited material of the Mikuszowice Chert Beds (Silesian Nappe, Outer Carpathians), as well as changes in the percentage content of biomicrites in the turbidite facies allowed to identify the neritic environment of the peri-Tethyan shelf, in relation to redeposition of calcareous-siliciclastic mud, enriched in sponge spicules induced by sea level third-and first-order fluctuations.
Planktonic foraminifera, in the whole section studied, represent a typical record for the late Albian-middle Cenomanian assemblages known from both pelagic and neritic zones, which are dominated by Hedbergella-like forms, accompanied by biserial P. moremani. Episodic occurrence of taxa reflecting a shallow marine stressful environment, lack of forms living close to low oxygen zone exclude the presence of extreme water conditions on the continental shelf during that time. The radiolarian assemblage is dominated by H. barbui Dumitrică which are deep-dwelling forms and prefer nutrient-rich conditions.
Changes in the content of both groups of planktonic biota in material redeposited from shelf facies are here interpreted as fluctuations in their numbers in the neritic zone which were related to the depth of the shelf bottom and supply of nutrients. We recognized here a few trends in planktonic foraminifera which may be correlated with sea level changes of 3rd order including: (a) the record of enhanced content of small, globular planktonic foraminifera during the OAE1d corresponding to the maximum of transgression during the KAl8 cycle, (b) the lowest content of biomicrite microfacies along the Albian-Cenomanian transition and during the early Cenomanian (without its younger part) reflecting the regression cycles of KAl8, (c) the increase in the content of planktonic foraminifera between the layers of allodapic limestone in the upper lower Cenomanian corresponding to the next transgressive cycle (KCe1), (d) the rising abundance of planktonic foraminifera above the MCE Ia and MCE Ib related to transgressive KCe3 cycle.
The radiolarian sea level 3rd order signal is closely related to the distribution of nutrients in the water column. The greatest radiolarian abundance and diversity are related to the MCE Ia, MCE Ib and ?MCE II events. In sediments redeposited from the platform, radiolarians are present during the transgressive cycles, when sea level rise allows the upwelling of fertile waters towards the shelf and support sea-surface assemblies there. This is clearly visible during the transgressive KCe3 cycle which was especially strong due to the first order transgressive cycle at the same time. During regressive and lowstand cycles, radiolarian assemblages contain primarily taxa living in the deeper zones of the water column.