Palaeoenvironmental Interpretation of Pleistocene Deposits from Magoula (Northwestern Peloponnesus, Greece)

University of Patras September 2019

Department of Geology

Geosciences and the Environment

Laboratory of Palaeontology - Stratigraphy

Palaeoenvironmental interpretation of Pleistocene deposits from Magoula (northwestern Peloponnesus, Greece)

Konstantina Karanika (R.N: 1029636)

Members of the committee:

George Iliopoulos (supervisor)

Ioannis Koukouvelas

Elsa Gliozzi

Contents

ACKNOWLEDGEMENTS ...... 3 ABSTRACT ...... 5 1. INTRODUCTION ...... 7 2. GEOLOGICAL SETTING ...... 8 2.1 Geotectonic evolution of the Corinth-Patras basin ...... 10 2.2 Pliocene – Quaternary formations of the Corinth-Patras graben ...... 11 2.3 Rio-Antirrio sub-basin ...... 13 2.3.1 LITHOSTRATIGRAPHY OF RIO-ANTIRRIO SUB-BASIN ...... 13 2.3.2 TECTONIC, STRATIGRAPHIC AND PALEOGEOGRAPHIC EVOLUTION OF THE RIO-ANTIRRIO SUB- BASIN ...... 15 3. PALAEONTOLOGY ...... 19 3.1 Ostracods ...... 19 3.2 Foraminifera ...... 20 4. MATERIAL & METHODS ...... 22 5.1 Section M ...... 27 5.2 Section K ...... 28 6. TAXONOMY ...... 32 7. RESULTS OF MICROPALAEONTOLOGICAL ANALYSES ...... 40 7.1 Section M ...... 40 7.1.1 RELATIVE ABUNDANCE DIAGRAMS ...... 40 7.1.2 STATISTICAL ANALYSIS ...... 41 7.2 Section K ...... 44 7.2.1 RELATIVE ABUNDANCE DIAGRAMS ...... 44 7.2.2 STATISTICAL ANALYSIS ...... 45 8. DISCUSSION ...... 50 8.1 Section M ...... 50 8.2 Section K ...... 54 8.3 Age of the sections ...... 60 8.4 Correlation between the sections ...... 62 8.5 Correlation with previous studies ...... 64 9. CONCLUSIONS ...... 66 REFERENCES ...... 67 Annex I...... 78 Annex II ...... 82 1

ACKNOWLEDGEMENTS

I would first like to thank my thesis advisor Prof. George Iliopoulos. The door to his office was always open whenever I ran into a trouble spot or had a question about my research or writing. He consistently allowed this paper to be my own work but steered me in the right the direction whenever he thought I needed it.

I would also like to thank the experts who were involved in the validation survey for this research project: Prof. Ioannis Koukouvelas and Prof. Elsa Gliozzi. Without their passionate participation and input, the validation survey could not have been successfully conducted!

Moreover, i would like to thank Prof. Nikolaos Kontopoulos for all the knowledge that he gave me during field work and Prof. Avraam Zelilidis for his assistance in understanding the evolution of the basin.

Special thanks to my best partners Penelope Papadopoulou and Maria Tsoni for their advices, the conversations we had and Maria Kolendrianou, Eleni Liapi, Irene Pappa and everyone else that helped me during the field work and the sampling and all the great working times in the lab! I will miss you all!

Finally, I must express my very profound gratitude to my parents, Andriana & Efthimios, my sister Despoina and to my mate, Eleftherio Georgoula for providing me with unfailing support and continuous encouragement throughout my years of study and through the process of researching and writing this thesis. This accomplishment would not have been possible without them. Thank you.

Konstantina Karanika

September 2019

ABSTRACT

This work involves the palaeoecological study of Pleistocene deposits from Magoula (northwestern Peloponnesus, Greece), based on the analysis of microfaunal elements. The study area has been chosen not only as a site of significant palaeontological interest where plant fossils, mammal bones and a wide range of different kinds of invertebrate and microfossils occur, but also for its tectonic position at the Rio –Antirio basin. The former basin bridges the Patraikos and Corinth Grabens.

Microfaunal analyses were carried out on 267 samples collected every 20-40cm from two natural sections in the area of Magoula. From the first section (section M), which has a total thickness of 31.30 meters, 133 samples were processed, whereas from the second section (section K) with a total thickness of 27.20 meters, 134 samples. Sediment samples were wet sieved with tap water through 500 and 63 μm mesh sieves. Microfossils were sorted from the dried residues and subsequently were studied under the stereoscope.

Species were determined based on previous studies of Mediterranean benthic taxa. The collected data were analyzed, relative abundance diagrams were prepared for each species using the software C2. Furthermore, taphonomic indices (Right/Left valve ratio, Sex ratio, Adult/Juvenile ratio and Carapace/Disarticulated Valves ratio) were calculated for most of the abundant species of ostracods. Also, stratigraphic columns were plotted according to collected section log data. Considering both the stratigraphic and the micropalaeontological analysis results, a detailed palaeoenvironmental reconstruction took place.

In section M, according to microfaunal analysis, 4 ostracod taxa (Cyprideis torosa (both un-noded and noded morphotypes), Candona neglecta, Ilyocypris gibba, Aurila convexa) were recorded in the studied samples. The most abundant were C. torosa and C. neglecta. Two benthic foraminifera taxa (Ammonia tepida and Haynesina depressula), as well as some charophyte gyrogonites, freshwater gastropod opercula and fragments (Bithynia sp. and Valavata cristata) were identified as well. These data suggest that an initially lagoon system, turned gradually into a lagoonal river mouth environment (barren layers) due to sea level drop, and finally when sea level rose, it became again a lagoonal environment influenced by a river system with strong freshwater influxes. Moreover, the relative abundance diagrams and the taphonomic indices in combination

with the stratigraphic column characterize a possible flood event at 24.10-24.30 meters. Thus paleoenvironmental changes occurred due to eustatism.

In section K, according to the microfaunal analysis, 6 ostracod taxa (C. torosa (un-noded morphotypes), C. neglecta, Loxoconcha elliptica, Cytheridea neapolitana, Leptocythere rara and A. convexa were recorded in the studied samples, 6 benthic foraminifera taxa (A. beccarii, Ammonia tepida, H. depressula, Elphidium advenum, Elphidium crispum and Quinqueloculina seminula), as well as some brackish gastropods (Hydrobia acuta) brackish bivalves and fragments (Cerastoderma glaucum and Mytilidae) were identified as well. Palaeonvironmental changes occurred due to eustatism. Initially a lagoon system, turned gradually into an open lagoon environment due to sea level rise, and finally when sea level dropped became again a lagoonal environment influenced by a river system with freshwater influxes.

The distance between section M and section K is only 138 meters, however, there is no connection between the two referred palaeoenvironments. The small distance between the two sections and the difference of the determined palaeoenvironments indicate the effect of a fault, with a total throw of at least 58.5 metres.

1. INTRODUCTION This work involves the palaeoecological study of Pleistocene deposits from Magoula (northwestern Peloponnesus, Greece, Fig. 1), based on the analysis of microfaunal elements. The study area (2.5 km SE of the University of Patras) has been chosen not only as a site of significant palaeontological interest where plant fossils, mammal bones and a wide range of different kinds of invertebrate and microfossils occur, but mainly because it belongs to the tectonically interesting Rio –Antirrio Βasin, which is part of the Corinth rift. Rio–Antirrio basin is an asymmetric graben with a NΕ-SW trend, located between the mainland of Greece and NW Peloponnesus (Kontopoulos & Zelilidis 1997). The basin formed during the Upper Pliocene to Lower Pleistocene, due to WNW normal faults and NNE transfer faults (Doutsos et al. 1988).

Fig. 1 . Map illustrating the position of the studied area

2. GEOLOGICAL SETTING The Corinth-Patras rift system constitutes a back arc basin formed due to extensional tectonism and its borders are generally defined by WNW trending normal faults (Doutsos et al., 1988). The rift system consists of the Corinth, Rio-Antirrio and Patras (CRP) grabens (Zelilidis, 2003) (Fig. 3). Its length is 180 km, while its maximum width is 40 km and separates Peloponnese from the Continental Greece. Τhe rifting process is considered that started during the Early Pliocene with intense tectonic activity (Rohais and Moretti, 2017), by which Peloponnese was separated from Central Greece. Along the Corinth - Patras rift system, the Cenozoic sediments have been deposited on the Pre-neogene substrate of the Peloponnese (Poulimenos, 1993). This consists of rocks belonging to the following geological units: the Ionian unit, Gavrovo - Tripoli unit, Olonos – Pindos nappe, Parnassos unit and the Sub-Pelagonian unit (Fig. 2).

Fig. 2 Geological map of the Hellenic units illustrating the Gulf of Corinth, which consists of the Corinth, Rio-Antirrio (the study area) and Patras sub-grabens. The Gulf of Corinth consists of the geological units: the Ionian unit (blue), Gavrovo - Tripoli unit (red), Olonos – Pindos unit (green), Parnassos unit (yellow) and the Sub-Pelagonian unit (purple). (modified after Vakalas and Zelilidis, 2014)

Fig. 3 Simplified geological map of the Gulf of Corinth, illustrating the three sub-basins of the Corinth, Rio-Antirrio (study area(red)) and Patras. (Zelilidis, 2003)

Ever since the end of Eocene, the wider area of the Peloponnese is characterized by the eastern modern subduction of the ocean of Pindus. During this convergence, the microplates of the Apulian and Pelagonian were included in a tectonic convergence environment (Fig. 4) (Xypolias and Doutsos, 2000). Simultaneously with this convergence, the rocks of Pindos nappe were ovethrusted westwards onto the Tripolis limestones. These movements resulted in the thickening of the Apulian Plate and the simultaneous elevation and subdivision of contemporaneous flysch’s basins into piggy-back basins (Xypolias and Doutsos, 2000).

Fig. 4 Synthetic east–west cross-section throughout southwestern Hellenides, showing that the microplates of the Apulian and Pelagonian zones were included in a tectonic convergence environment (Xypolias and Doutsos, 2000)

2.1 Geotectonic evolution of the Corinth-Patras basin

Since the last stage of the Alpine orogenesis (Up. Eocene - M. Miocene) compressional tectonics prevailed in western Greece and from the upper Pliocene until today the region was characterized by neo-tectonic evolution. This evolution was characterized by extension due to the constant migration of the extension of the Aegean arc to the west. The sub-grabens of Patras, Rio-Antiriro and Corinth were formed during this extension (Doutsos et al., 1987, 1988). The sub graben of Rio- Antirrio, with ENE direction, was formed after the extension and the post-orogenetic elevation, during the upper Pliocene to Lower Pleistocene. The extension and the westward movement caused the extension of the Corinth rift to the southwest. Moreover, the movement was transferred to the south and the connection of the sub-graben of Corinth and the sub-graben of Rio –Antirio created the sub-graben of Patras (Fig. 5).

Fig. 5 Schematic block diagrams showing Α: the formation of the sub graben of Rio- Antirrio with ENE direction, after the extension due to the constant migration of the extension of the Aegean arc to the west and the post-orogenetic elevation, during the upper Pliocene to Lower Pleistocene. B: the formation of the sub graben of Patras due to the transfer of the movement to the south and the connection of the sub-graben of Corinth and the sub-graben of Rio –Antirrio. (Doutsos et al. 1988)

The number of terraces observed along the borders of the sub-grabens certify an uplift of the area. Kalletat et al. (1976), surveying the entire Peloponnese by studying the vertical movements in the area, argued that the area is turning around an axis with NNW direction. According to Zelilidis (2003), during the Holocene, a subsidence (up to 10 mm/year) of the southwestern part of Patras Bay over the Neogene-Pleistocene substrate and a deposition of 40m-thick sediments has 10

been observed. Deltaic and alluvial fan sediments were deposited along faults of listric geometry, during the Holocene until today, on the margins of the Patras and Corinth basins. According to Zelilidis (2003), the rate of uplifting of the Quaternary terraces is 0.8 mm/year in the sub-basin of Patras and 1mm/year near the city of Patras. Also, the highest elevation rate has been observed in the sub-basin of Rio (4,5 mm/year) by Kontopoulos & Zelilidis (1997) while the uplift rate decreases to the east in the Corinth basin from 2,2 mm/year near Aigio, to 1.5 mm/year in the central region of the basin and only 0.3-0.4 mm/year near the city of Corinth.

2.2 Pliocene – Quaternary formations of the Corinth-Patras graben The most widespread formations around the graben of Corinth - Patras are those of Pliocene and Pleistocene age, which were built up to 1800m (Xirokambos hill in the southern margins of the basin, in the area of mountain Helmos). Their thickness is estimated to exceed 1000m. For this reason, their geological evolution follows. During the Lower Pliocene, Corinth basin was characterized by lagoon deposits. Up to the Upper Pliocene, the Corinth rift was a uniform basin in width and depth, in which lagoon sedimentation environments developed. This basin was controlled by WNW trending faults and by NNE trending transfer faults (Doutsos et al., 1988).

The geometry of the basin changes in the Lower Pleistocene. Several researchers have proposed different ages and palaeoenvironmental interpretations for the sediments of Northern Peloponnese. In 1892, Phillipson, without specifying age, divided the neogene sediments into the lower level, consisting of sands, marls, clays and calcareous sandstone, and the upper level, consisting of conglomerates. According to Deperet (1913), the Neogene formations in the Northern Peloponnese are of Upper Pliocene age. On the contrary, Mitzopoulos (1940) and Psarianos (1943) consider the age of these deposits as Lower Pliocene. Charalambakis (1951), also, believes the age of the neogene formations of the Peloponnese is Lower Pliocene. In 1955, Psarianos argued that lacustrine outcrops in Northern Peloponnese lie over the marine outcrops and continue from the Isthmus to ancient Ilida. Both the lacustrine and the marine formations are of Pliocene age.

According to Decourt (1964), the conglomerates between mountains Erymanthos and Panachaiko are of continental origin and of Pliocene age. In 1976, Kelletat et. al. argued that marls of Neogene age have brackish to lacustrine origins, over which conglomerates overlap unconformably. Serbier (1977) also agreed with this view. In 1985, Doutsos and Kontopoulos divided the area of Antirio 11

into five main lithofacies of middle-upper Pliocene age, of which the two upper ones are of terrestrial origin, the two intermediates of lacustrine and lagoon origin, while the deepest one is of marine origin. In the same year, Mariolakos et al. noticed the absence of Miocene deposits in northern Peloponnese. In 1987, Frydas demonstrated that the oldest sediments of Achaia were deposited in the Upper Pliocene, and Doutsos et. al. (1987), defined the origin of the terrestrial conglomerates as upper and lower braided river deposits. In 1988, Doutsos et. al, distinguished two sedimentary facies for the sediments of the western Corinth sub-graben. One facies consist of alternations of sandy clays and clays of Upper Pliocene age and the other consists of conglomerates covering unconformably the underlying horizons.

In the same year, Zelilidis et. al. separated the sediments of the Patraikos basin into the following lithofacies: A) marine deposits, B) lacustrine deposits, C) terrestrial fluvial deposits, D) sediments of alluvial origin, E) terrestrial and river deposits. Frydas in 1989 proposed a Lower Pleistocene age for fine-grained sediments in the Kastritsi region. Rozos (1989) and Koukis and Rozos (1990, 1993) divided the Pliocene and Pleistocene deposits of the prefecture of Achaia into the sub-basin of Patraikos, the sub-basin of the Corinth gulf and the sub-basin of Leontio. According to Kontopoulos and Zelilidis (1992), the sub-graben of Rio consists of sediments of lacustrine origin, covering marine sediments, which date back to the Upper Pliocene. These lacustrine sediments are placed unconformably on silts of marine origin, and which are covered by braided river deposits and alluvial fan deposits of Lower Pleistocene age. Danatsas and Strauch (1994) studied the ostracod fauna and found that the post-Miocene sediments of the area were deposited between the Upper Pliocene and the Lower Pleistocene in a series of transgression and regression events at different coastal sites and environments. The brackish and lacustrine facies occupy the upper segments and are of Pliocene and Pleistocene age. Danatsas (1994) defined the age of the lagoon sediments of Northwest Peloponnese as Pleistocene.

Stamatopoulos et al. (1994) determined the age of the sediments of the Western Peloponnese (samples from Lapa and Eleotopos) as middle Pleistocene or younger, applying the Th230/U238 dating method to corals. In 1997, Kontopoulos and Zelilidis, determined the sediments of Argyra, Kastritsi and Romanos as: Plio-Pleistocene the marine/lagoonal deposits, Lower Pleistocene the proximal braided river deposits, Middle to Upper Pleistocene the lagoonal deposits and Upper Pleistocene the alluvial fans. Zelilidis et. al. (2000) reported that the Pliocene-Pleistocene deposits of the Selinountas river basin were created from seven different sedimentation environments.

These environments are: lagoon deposits, river-lacustrine deposits, braided river deposits, deposits of two different species of alluvial fans and river deposits. The same year Perissoratis et al. identified the age of Selinountas delta as late Pleistocene.

Houghton et al. in 2003 identified the age of the marine sediments of the western Gulf of Corinth (samples from Drepano), applying U/Th Chemical and Isotopic dating method to corals as Middle Pleistocene (MIS 6 (191–130 ka)).

Stamatopoulos et al. in 2004 identified the age of the lagoonal sediments exposed in northwestern Peloponnese (samples from Ano Kastrisi, Arachovitika and Agios Georgios Drepanou) as Upper Pleistocene and Palyvos et. al. (2007) the marine deposits at the western end of the Corinth Rift and the Rion area (samples from Profitis Elias-Ano Zeria, Ano Rodini, Ano Kastritsi, Agios Georgios and Psathopyrgos) as Middle-Late Pleistocene.

In 2010, Palyvos et. al. identified the age of the coastal deposits of the westernmost part of the Corinth Gulf Rift (samples from Selianitika, Aravonitsa, Neos Erineos and Ano Zeria), applying the isotopic (238U, 232Th, 230Th/232Th, 230Th/234, U234U/238U) dating method to corals, as Middle-Late Pleistocene.

In 2014, Gobo et al. identified the age of the gravelly deposits of the large Platanos Gilbert-type delta as Late Pleistocene. In addition, Hemelsdaël et al. (2017) identified the age of the alluvial Lower Group of the western Corinth rift (formations of Mega Spilaio, Lithopetra and Valimi) between about 3.6 Ma to 1.8 Ma, i.e. Pliocene to Lower Pleistocene. Also, Rohais and Moretti (2017) identified the age of the distal marine deposits in Xylokastro and Akrata as Pliocene to Lower Pleistocene (3.0 Ma – 2.55 Ma) and the alluvial deposits in the same area as lower-middle Pleistocene (2.55 Ma – 0.8 Ma).

2.3 Rio-Antirrio sub-basin 2.3.1 LITHOSTRATIGRAPHY OF RIO-ANTIRRIO SUB-BASIN

The Rio-Antirrio graben in northwestern Peloponnese is an asymmetrical graben filled with Pleistocene deposits, which, according to Kontopoulos & Zelilidis (1997), include lacustrine, terrestrial and lagoonal facies. According to Kontopoulos & Zelilidis (1997), a generalized section of the area, could consist of the following lithofacies from the bottom to the top:

• Yellow to gray lacustrine facies: the maximum exposed thickness of this facies is about 100m. This consists of interbedded mudstone, siltstone, sandstone and conglomerates in coarsening-up cycles of 5-20cm thick. In this sequence, nonmarine ostracods (Candona sp., Ilyocypris sp.), nonmarine molluscs (Melanopsis sp., Viviparus sp., Limnocardium sp.) and fossils plant were found. The facies corresponds to deltaic deposits in a lacustrine environment.

• Yellow to brown-red terrestrial facies: these facies consist of three different types of alluvial deposits that belonged to an alluvial fan. The corresponding environment contains the areas of a braided river near the proximal and distal source. The transition from one environment to another is lateral.

1) Alluvial fan deposits. These red-brown deposits include bulky, very poorly graded, non- oriented grains, with a large percentage of conglomerates and a thickness of 120 m. Their size ranges from 1 to 30 cm, and there are outsized clasts up to 50 cm in size. The matrix consists of fine-grained gravel, sand and red-brown silt. Paleosols were identified, consisting of 50 cm thick red-brown silt. Poorly graded conglomerates indicate debris flow deposition (Miall 1978). This indicates an alluvial fan environment in a dry/semi-dry area. 2) Braided river deposits (proximal): these yellow deposits are horizontally stratified, consisting of poor to moderately classified layers of gravels with a thickness of 120 m. Horizontal stratification is characterized by fine-grained layers. The matrix consists of a coarse sand. Sandstone and palaeosol units are also identified in these deposits, with a thickness of 50 cm. The horizontal stratification, the moderately graded conglomerates, and the small variance of paleocurrent directions reveal proximal flow processes of a braided river. 3) Braided river deposits (distal): these deposits have a thickness of 60 m and consist of 3 different facies (Kontopoulos & Zelilidis, 1997): a) Single-storey channel-bodies of conglomerate, b) Multiple channel-bodies of conglomerate/ sandstone, c) Overbank fine deposits.

• Yellow to gray lagoon facies: The maximum observed thickness of this facies corresponds to 20 m. It extends in the Romanos area (5.5 km SE of Patras) and consists of the following lithofacies from the base to the top.

1) Massive gray marl beds with typical lagoonal macro- and microfauna.

2) Interbedded yellow to gray mudstone, siltstone and sandy siltstone beds. This succession shows high values of organic matter and contains brackish to marine ostracods and fossil leaves. 3) Yellowish layers of sand without organic matter. 4) Interbedded yellowish silty sand, sand and strongly cemented sandy gravel beds. Fragments of Ostrea sp. are present. The coarsening upward sequence with lagoonal fauna suggests the appearance of a transgressive sequence of a barrier island complex.

• Red terrestrial facies: these facies belong to the Upper Pleistocene and is 100 m thick. It consists of massive conglomerates with a high percentage of matrix. No fossils were recorded. These facies testify an alluvial fan environment (Kontopoulos & Zelilidis, 1997).

2.3.2 TECTONIC, STRATIGRAPHIC AND PALEOGEOGRAPHIC EVOLUTION OF THE RIO-ANTIRRIO SUB- BASIN The Rio-Antirrio graben is an asymmetrical graben with a NE-SW direction between Peloponnese and Continental Greece. A large part of the Rio-Antirrio graben is submerged in the eastern margin of Patraikos gulf and the straits of Rio. It is limited by the pre-Neogene substrate at its northern margins, near the village of Molykreion with a normal fault and a displacement of 350 m. On the south side there are two major faults: the Saravalli and the Kastritsi faults. The sub-graben of Rio was formed during the upper Pliocene - lower Pleistocene due to NE normal faults. Originally, it was a basin filled with marine/lagoon sediments. In the areas of Platani, Romanos and Ano Kastritsi, lagoonal fine-grained deposits were accumulated during this period (Kontopoulos & Zelilidis, 1997). According to Kontopoulos & Zelilidis (1997), in the lower Pleistocene, alluvial, lacustrine and braided river sediments were deposited unconformably on marine/lagoon layers (Fig. 6).

Fig. 6 Map and block diagram of lacustrine environment in the Upper Pliocene (Kontopoulos and Zelilidis, 1992) In the eastern part of the study area, due to intense tectonic activity, alluvial fans were formed at the southern margins of the basin. To the southwest of the study area, these alluvial fans pass laterally from braided river to lacustrine deposits. This lateral development was controlled by northwestern transfer faults, which divide the eastern section of the basin into three zones (Drepano, Argyra and Ano Kastritsi) (Fig. 7) (Kontopoulos and Zelilidis, 1997). The zone of Argyra was affected by major normal faults that divide it into two sections, the northern and the southern. Due to the intense displacement of the southern marginal fault, a high reef was created in the middle of the basin. This southern part consists of alluvial fan deposits, while at the northern part braided river sediments were deposited. These deposits show southwest growth from proximal to distal in each zone (Fig. 8).

Fig. 7 Geological map of Peloponnesus illustrating the distribution of the Pliocene-Quaternary deposits. (Kontopoulos and Zelilidis, 1997)

Fig. 8 Geological map illustrating the distal braided river and proximal alluvial fan deposits (Kontopoulos and Zelilidis, 1992)

During the Upper Pleistocene, the basin was flooded due to the reactivation of the marginal fault at the southern margin. According to Kontopoulos & Zelilidis (1997), lagoonal deposits from 17

100,000 to 200,000 years were deposited unconformably on lacustrine deposits or braided river deposits and alluvial fan sediments. Subsequently, tectonic activity gradually migrated north causing different elevation to the underlying part of the active fault, as evidenced by three clear levels of lagoonal deposits (600 m a.s.l. in Ano Kastritsi, 500 m a.s.l. in Drepano and 300 m a.s.l. in Romanos). Tectonic activity migrated from the south to the north and vice versa. The southern marginal fault was activated at least twice until the upper Pleistocene (Kontopoulos & Zelilidis, 1997). The fact that lagoon deposits that date back to 100,000 years appear 600 m above the sea level supports the view that the elevation is more than 6 mm/yr (Kontopoulos & Zelilidis, 1997).

3. PALAEONTOLOGY

From the sediment samples we collected mainly ostracods and benthic foraminifera. Charophyte gyrogonites, gastropod opercula and fragments of gastropods and bivalves were also collected.

3.1 Ostracods According to Palacios-Fest (2018) and Rodriguez-Lazaro & Ruiz-Muñoz (2012) ostracods are microscopic crustaceans ranging in size from 0.5 to 2 mm, some may be as large as 8 mm. Unlike other crustaceans, they are protected by a bivalve carapace made of low-magnesium calcite (calcium carbonate). The soft body consists of reduced trunk segmentation with five to eight pairs of limbs (appendages) that they use for crawling, swimming, mating (if amphigonic: female/male, some are parthenogenetic: somatic asexual reproduction), or grabbing food from the surrounding environment (Palacios-Fest, 2018). Ostracods are one of the oldest and most diverse groups of crustaceans, a conservative estimate suggests there are more than 20,000 living species, 8,000 of which have been described to date. Known since the Ordovician (500 million years ago), ostracods may include more than 65,000 living and fossil forms. Only the hard parts (valves) survive in the fossil record (Palacios-Fest, 2018). Nine growth stages (ecdysis) allow the organism to shed its old carapace or shell before forming a new one. Genetic make-up and the environment both influence shell morphology and ornamentation. The shells have a bean-like shape that may vary from kidney-shape, to subrectangular, subtrapezoidal, or triangular (Palacios-Fest, 2018). Secreted by the epidermis, the calcium carbonate shell incorporates more than 25 minor and trace elements into the calcite structure (Bodergat, 1985, Holmes & De Deckker, 2012 and Dettman & Dwyer, 2012). Surface ornamentation may be smooth to reticulated, striated, punctuated, with or without visible pore canals, simple, or cribrated. Genders are clearly dimorphic if the species is amphigonic. Nonmarine ostracods are sensitive to water chemistry, salinity, temperature, and dissolved oxygen, among other parameters. They occur in freshwater, brackish, and brine conditions in lakes, ponds, wetlands, springs, and streams, including irrigation canals and reservoirs (Palacios- Fest, 2002 and Mesquita-Joanes et al., 2012). Altitude and latitude are also important factors controlling the species’ geographic distribution. Based upon their ecological requirements, it is possible to use this group in palaeoecological reconstructions to understand the human– environment interaction (Palacios-Fest, 2018 and Lord et al., 2012).

The hinge is an important feature in terms of taxonomy and classification, as muscle scars and pores. Four basic types of hinge are recognised (Horne et al. 2002): 19

1. The adont hinge is the simplest, without teeth or sockets, often forms part of a contact groove on the larger valve and a corresponding ridge on the smaller valve.

2. The merodont hinge is composed of a tooth and socket at each end of a groove or ridge structure (complementary negative and positive structures in left and right valves).

3. The entomodont hinge differs from the merodont hinge style by having a coarsely crenulated anterior portion of the median groove/ ridge element.

4. The amphidont hinge has a more complex median structure with an anterior tooth and socket.

3.2 Foraminifera Foraminifera are single-celled organisms (protists) that possess a hard test (shell) and which could be preserved in the sedimentary record after death. This test is secreted by the cell and is mainly composed of agglutinated walls (detrital grains glued together with organic cement) or calcium carbonate (predominantly calcite) (Cerraeta, 2018). The test consists of a number of chambers that are arranged in numerous shapes and sizes. Adult foraminifers range in size from less than 0.40 mm (planktonic forms) to up to 10 cm in width (larger benthic foraminifers). They are tolerant to a range of variables such as salinity, temperature, oxygenation, and organic and nutrient flux. Foraminifera are exclusively marine; most are benthic (living on or under the seabed) although a few genera are planktonic (floating in the water column) (Cerraeta, 2018). Foraminifera are among the most abundant and ubiquitous shelled organisms in the marine environments. Their distribution ranges from the intertidal salt-marshes to the deepest ocean trenches and from the equator to the poles. They respond rapidly to environmental changes, and individual species indicate specific environments. For example, a strong relationship exists between the altitudinal distribution of modern benthic foraminiferal species and tidal levels. Transfer functions that quantify this relationship have provided a basis for the reconstruction of Holocene changes in sea level (see sea-level change) at a very high resolution (Cerraeta, 2018). These reconstructions are constrained by taphonomic factors such as reworking and differential dissolution, resulting in mixed assemblages, indicated by poor preservation and unusual assemblage structure. Foraminifera represent several advantages in comparison to macro-fossils (e.g., molluscs). For example, they present a higher density in marine sediments, and consequently much smaller sediment volumes are needed for a reliable assessment (Cerraeta, 2018). They commonly have

shorter life cycles and populations therefore respond quickly to environmental changes. After reproduction or death a large part of the foraminifer assemblage is preserved in the sediment (Cerraeta, 2018).

4. MATERIAL & METHODS When the sections were mapped, a detailed recording of the layers, sedimentary sections, fossil recordings and other observations was made.

Microfaunal analyses were carried out on 267 samples collected every 20-40cm from two natural sections in the area of Magoula. From the first section (section M) (Fig. 9 & 10), which has a total thickness of 31.30 meters, 133 samples were processed and from the second section (section K) (Fig. 9 & 11) with a total thickness of 27.20 meters, 134 samples.

Sediment samples of 100 grammars were wet sieved with tap water through 500 and 63 μm mesh sieves and were dried at 60o C. Microfossils were sorted from the dried residues and subsequently were collected, studied under the stereoscope and photographed by Scanning Electron Microscopy (SEM).

Fig. 9 Section M and section K (Google Earth)

Fig. 10 Section M

Fig. 11 Section K

Foraminifera were identified based on Holbourn et al. (2013). Ostracoda were identified on several papers published on “A stereo-atlas of ostracod shells”, edited by Sylvester Bradley & Siveter from 1973 to 1975, by Bate and al. from 1976 to 1987 and by Athersuch et al. from 1988 to

1999, and on other published literature listed in the following paragraphs). The collected data were analyzed, relative abundance diagrams were prepared for each species using the software C2 (Microsoft Windows program for the analysis and visualisation of ecological and palaeoenvironmental data). Furthermore, taphonomic indices (Right/Left valve ratio, Sex ratio, Adult/Juvenile ratio and Carapace/Disarticulated Valves ratio) were calculated for most of the abundant species of ostracods. Moreover, the Ammonia-Elphidium Index (IAE) were also calculated from the samples with the presence of Ammonia sp. and Elphidium sp.

RV / LV ratio

According to Schellenberg (2007), this index characterizes the deposition of organisms. On one hand, if the ratio varies slightly from the unit, it is considered that the valves have been deposited in-situ (by the way, the similarity of the valves in size and in hydrodynamic characteristics plays an important taphonomic role). On the other hand, if the ratio varies significantly from unit, the lighter valves may have been transported (Breman, 1980, Boomer et al., 2003).

F / M ratio

The use of this index can be easily applied to ostracod assemblages, as many species exhibit prominent sexual dimorphism (Abe, 1990). In ostracods, the ratio between female and male valves often varies greatly from unit and the interpretation of the ratio is therefore confusing (Abe, 1990), as it even depends on the ostracod species. Mostly, different numbers are attributed to environmental differences and occurs rarely when males are more abundant than females or more often when the population consists solely of females due to asexual reproduction (Namiotko & Martins, 2008, Boomer et al., 2003).

A / J ratio

Podocopid ostracods goes through 8 growth stages (called instars). However, all of the eight stages are rarely kept in sediments, as in the early stages of ecdysis the shells are very thin and cannot be preserved, while many die before reaching adulthood. However, the relative proportion of Adult/Young ostracod valves may provide important palaeoenvironmental information (Frenzel et al., 2005). For example, a ratio of 5:1 (5) probably represents an in-situ deposition with significant taphonomic removal of many young stages. A midrange of 1:8 to 1:4 might be attributed to an in-situ thanatocoenosis, but with less removal of the young stages and therefore more representative of the biocoenosis. In addition, a sample with a very low ratio, such as 1:25, 24

may represent the local deposition of young valves, which are easily transported or even an in-situ mass death episode (Schellenberg, 2007). Therefore, when only adult or juvenile late-stage valves are found, this is interpreted as deposition in a high-energy environment. On the contrary, if only juveniles ostracods are found in an assemblage, it is interpreted as being deposited in a low- energy environment, but displaced from where the animal lived. In the case where all or almost all the instars of a particular species are identified, this indicates a low energy environment and an in- situ deposition (Frenzel & Boomer, 2005, Armstrong & Brasier, 2005, Boomer et al., 2003).

C / V ratio

Whole ostracod shells, as compared to individual right or left valves, are found relatively rare in sediments, due to degree of post-mortem reworking and time until burial. Consequently, a lower index value is considered to reflect a relatively disturbed surface of the sediment, where the carapaces were exposed and disarticulated, whereas extremely high values of the index may indicate low energy conditions as well as possible mass death episodes, which can be also associated with increased sedimentation rates. This ratio tends to be lower in younger ostracods than in adults, due to the poorly developed hinge and ecdysis process that sheds the shell (Schellenberg, 2007). In addition, low index values may be due to redistribution (Frenzel & Boomer, 2005, Hussain et al., 2007, Boomer et al., 2003).

Clustering analysis, Correspondence analysis and Diversity indexes (Taxa_s, Simpson, Shannon and Evenness) were calculated for each section using the software Past 3 (Software for scientific data analysis, with functions for data manipulation, plotting, univariate and multivariate statistics, ecological analysis, time series and spatial analysis, morphometries and stratigraphy) (Hammer et al., 2001).

The number of species (Taxa_s) that exist in a community, is the most important index. The Simpson (dominance) index, indicates the dominant species in the under-study population. The Shannon index takes into account the proportions of non-common species in an assemblage, and the Evenness Index is an index that compares heterogeneity in a sample to the maximum possible heterogeneity for the same number of species (Hammer et al., 2001).

The Ammonia-Elphidium Index (IAE=(NA/(NE+NE)) *100), allows to assess the oxygenation levels of coastal regions. Both genera used in this index are resistant to oxygen reduction conditions. The genus Ammonia has a greater resistance than the genus Elphidium to low oxic conditions, and

both are abundant in the coastal zones, which makes possible the use of this index to access the impact caused by organic matter pollution in these regions (Sen Gupta and Platon, 2006).

Also, stratigraphic columns were plotted according to collected section log data. Considering both the stratigraphic and the micropalaeontological analysis results, a detailed palaeoenvironmental reconstruction took place.

5. STRATIGRAPHY OF THE SECTIONS

As mentioned above the studied samples were collected from two different natural sections, Section M and Section K.

5.1 Section M

The synthetic stratigraphic column (Fig. 12) shown below describes in detail the lithology of section M, as well as various observations that were done during sampling. The section M has a total thickness of 31.30 meters and with direction and dip, respectively, 285o/30o, consisting of 19 different macrofacies.

Fig. 12 Section M: 133 samples (black dots) were collected every 20-40cm from 4 small sections (Ma’, Mb’, Mc’ and Md’), which were correlated and a synthetic stratigraphic log was created (on the right).

1) Brown clays with fragments of freshwater gastropods. 2) Yellow muds. 3) Fine-grained yellow sands. 4) Alternations of brown clays, yellow muds and fine-grained yellow sands. 5) Fine-grained massive gravels. 6) Brown clays. 7) Fine-grained sands. 8) Yellow muds with fragments of freshwater gastropods.

Out of the 133 sediment samples, 75 contained enough numbers of tests and valves (>10%, more than 30 valves of the 300 valves) for quantitative analyses, 53 were barren and 5 contained scarce specimens. According to the microfaunal analysis, 4 ostracod taxa (Cyprideis torosa (both un- noded and noded morphotypes), Candona neglecta, Ilyocypris gibba, and Aurila convexa) were recorded in the studied samples. The most abundant were C. torosa (un-noded morphotypes) and C. neglecta. Two taxa of benthic foraminifera (Ammonia tepida and Haynesina depressula), as well as some charophyte gyrogonites (Plate 1, fig: 19), and freshwater gastropod opercula and fragments, referable respectively to Bithynia sp. and Valvata cristata.

5.2 Section K The synthetic stratigraphic column (Fig. 13) shown below describes in detail the lithology of section K, as well as various characteristics observed during sampling. The section K has a total thickness of 27.20 meters and with direction and dip, respectively, 169o/11o, and consists of 13 macrofacies.

Fig. 13 Section K: 134 samples (black dots) were collected every 20-40cm from 5 small sections (Ka’, Kb’, Kc’, Kd’ and Ke’), which were correlated and a synthetic stratigraphic log was created (on the right).

1) Green mud with fragments of brackish gastropods and bivalves from. 2) Brown mud with fragments of brackish bivalves. 3) Green clay with fragments of brackish bivalves. 4) Blue clay with fragments of brackish bivalves. 5) Green clay with fragments of brackish bivalves, plant fossils and an in-situ death event (Fig. 14). 6) Alternations of brown and grey clay with fragments of brackish bivalves and sediment rich in gypsum. 7) Green clay with fragments of brackish bivalves, plant fossils and sediment rich in gypsum. Alternations of brown and grey clay and sediment rich in gypsum. 8) Grey clay. 9) Brown clay with plant fossils. 10) Alternations of brown and red clay with plant fossils.

Fig. 14 In-situ thanatocoenosis

Out of the 134 sediment samples, 111 contained enough numbers of tests and valves (>10%, more than 30 valves of the 300 valves) for quantitative analyses, 7 were barren and 16 contained scarce specimens. According to the microfaunal analysis, 6 ostracod species (C. torosa (un-noded morphotypes and a lot of growth stages except the last one), C. neglecta, Loxoconcha elliptica, Cytheridea neapolitana, Leptocythere rara and Aurila convexa were recorded in the studied samples, as well as 6 benthic foraminifera species (Ammonia beccarii, A. tepida, Haynesina depressula, Elphidium advenum, E. crispum and Quinqueloculina seminula), and some brackish gastropods (Hydrobia acuta), and brackish bivalves sometimes fragmented (Cerastoderma glaucum and Mytilidae (Fig. 15)).

Fig. 15 Brackish bivalves in the sediments: : (A: Cerastoderma glaucum. and B: Mytilidae)

6. TAXONOMY Kingdom: Animalia Linnaeus, 1758

Phylum: Arthropoda Lar, 1904

Subphylum: Crustacea Pennant, 1777

Class: Ostracoda Latreille, 1806

Subclass: Podocopa Sars, 1866

Order: Podocopida Sars, 1866

Superfamily: Cytheroidea Baird, 1850

Family: Hemicytheridae Puri, 1953

Genus: Aurila Pokorny, 1955

Species: Aurila convexa Baird, 1850

Ecology

A. convexa is a coastal to sub-coastal marine species. It can be a bottom sediment dweller as well as epiphytic. In this last case it is present with high densities due to environmental pressure. The species tolerates high salinity fluctuations (Ruiz et al., 1997, 2006).

Stratigraphic range

Tortonian to Recent (Mostafawi et al., 1969, 1990: Faranda & Gliozzi, 2008).

Family: Leptocytheridae Hanai, 1957

Genus: Leptocythere Sars, 1925

Species: Leptocythere rara Mueller, 1894 (Plate 1, fig: 16)

Ecology

A brackish (meso-euhaline) species (Lachenal, 1989).

Stratigraphic range

Occurrence in Pleistocene sediments. (Tsapralis, 1981 and Danatsas, 1989)

Family: Loxoconchidea Sars, 1925

Genus: Loxoconcha Sars, 1866

Species: Loxoconcha elliptica Brady, 1868 (Plate 1, fig: 22-23)

Ecology

It lives in lagoonal, brackish and coastal environment and is resistant to temperatures of 0-30 ° C and salinities between 2-35 ‰. It is widespread in the Mediterranean and is found in middle and low latitudes (Bignot, 1985) It’s mainly present on April and October (Pascual & Carbonel ,1992).

Stratigraphic range

Miocene to Recent. (Bonaduce et al.1975, Aranki 1987, Yassini 1979, Danatsas, 1989)

Family: Cytherideidae Sars, 1925

Genus: Cyprideis Jones, 1857

Species: Cyprideis torosa Jones, 1850 (Plate 1, fig: 1-12)

Ecology

C. torosa lives in lagoons and estuaries. This species is restricted to permanent wetlands, because its eggs can withstand low temperatures but not drought. (Kilenyi and Whittaker, 1974; Heip 1976). It is resistant to salinities up to 60% and depth up to 30 m as well as very low temperatures (up to ice). C. torosa mainly occurs in waters with salinity of 2-3 ‰ to 15-17 ‰ but when salinity (and/or other environmental factors) fluctuates, some differences in shell morphology are observed. C. torosa (un-noded morphotypes) (occurs in environments above 8‰ salinity) & C. torosa (noded morphotypes) (occurs in environments where salinity drops from 2-3 ‰ to 8‰) (Kilenyi & Whittaker, 1974 and Frenzel et. al, 2012).

Stratigraphic range

Early Pleistocene (Calabrian) to Recent (Gliozzi et al., 2005 and 2016, Krzyminska & Namiotko, 2013).

Family: Cytherideidae Sars, 1925

Genus: Cytheridea Bosquet, 1852

Species: Cytheridea neapolitana Kollmann, 1960 (Plate 1, fig: 20-21)

Ecology

A shallow marine dweller, tolerant for euhaline to mesohaline waters (Tsourou et al., 2015)

Stratigraphic range

Tortonian to Recent (Guernet et al., 2003; Miculan, 1992, Tab. 1; Faranda & Gliozzi, 2008; Aiello & Barra, 2010).

Superfamili: Cypridoidea Baird, 1845

Family: Candonidae, Kaufman, 1900

Genus: Candona, Baird, 1845

Species: Candona neglecta Sars, 1888 (Plate 1, fig:13-15)

Ecology

C. neglecta is widespread in springs, brooks and ponds connected to springs, and lakes, where it is found from the shallow littoral zone down to great depths. The species is distributed throughout the Holarctic (Meisch 2000). It can withstand salinities up to 16‰ (Meisch, 2000).

Stratigraphic range

Pleistocene to Recent (Krzyminska & Namiotko,2013).

Family: Ilyocyprididae Kaufmann, 1900

Genus: Ilyocypris Brady & Norman, 1889 34

Species: Ilyocypris gibba Ramdohr, 1808 (Plate 1, fig: 17-18)

Ecology

I. gibba is a cosmopolitan species. Its tolerance to low levels of total dissolved solids determines its existence in fresh to low salinity waters slightly less than 5‰ (Neale, 1988). It lives in shallow waters with a sandy bedrock and sometimes with marshy vegetation. It cannot survive in environments with temperatures below 10.5 ° C and is usually found in waters of 20-32 °C (Devoto, G., 1965, Delorme, 1991, Külköylüoglu, 2004).

Stratigraphic range

Miocene to Recent (Krzyminska & Namiotko, 2013).

Kingdom: Chromista Cavalier-Smith 1981

Phylum: Foraminifera d'Orbigny, 1826

Class: Globothalamea Pawlowski, Holzmann, & Tyszka, 2013

Order: Rotaliida Delage & Hérouard, 1896

Family: Ammoniidae Saidova, 1981 Genus: Ammonia Brünnich, 1771 Species: Ammonia beccarii Linnaeus, 1758 (Plate 1, fig: 25)

Ecology It is a common species that lives in neritic, marine environments with salinity greater than 33‰. It is often prevalent in the inner region of the platform at all latitudes and is resistant to salinity fluctuations (Le Campion, 1968; Rouvillois, 1970; Debenay, 1978; Redois, 1996; Murray, 2006). Stratigraphic range Oligocene to Recent (Loeblich & Tappan, 1988).

Family: Ammoniidae Saidova, 1981 Genus: Ammonia Brünnich, 1771 35

Species: Ammonia tepida Cushman, 1926 Ecology Is usually found in brackish environments with salinity below 33‰ at river mouths. (Le Campion, 1968; Rouvillois, 1970; Debenay, 1978; Redois, 1996). Stratigraphic range Miocene to Recent (Le Campion, 1968, Rouvillois, 1970, Debenay, 1978, Redois, 1996).

Family: Haynesinidae Mikhalevich, 2013 Genus: Haynesina Banner & Culver, 1978 Species: Haynesina depressula Walker & Jacob, 1798 (Plate 1, fig: 24)

Ecology

It is a benthic foraminifera found in the middle of the continental shelf (Carboni, 2010).

Stratigraphic range

Late Pliocene to Recent (Carboni, 2010)

Family: Elphididae Galloway, 1933 Genus: Elphidium Montfort, 1808 Species: Elphidium crispum Linnaeus, 1758 (Plate 1, fig: 26)

Ecology It is a neritic to medium deep-sea foraminifer. It reflects marine conditions and is abundant in areas of high salinity. It is also adapted to brackish and fresh waters. It is found mainly in sandy sediments of sub-tidal channels. It is located in the inner continental shelf (Lionaki, 2012). Stratigraphic range Miocene to Recent (Jones, 1994).

Family: Elphididae Galloway, 1933 Genus: Elphidium Montfort, 1808 Species: Elphidium advenum Cushman, 1922 Ecology

Mainly confined to shallow waters with depths of 30 m or less and with a low ripple. It is a species living in low salinity waters (Jung-Moo Kim, James P. Kennett, 1998) Stratigraphic range Miocene to Recent (Jones, 1994).

Family: Hauerinidae Schwager, 1876 Genus: Quinqueloculina d'Orbigny, 1826 Species: Quinqueloculina seminula Linnaeus, 1758 (Plate 1, fig: 27)

Ecology Is a benthic foraminifera, found on soft bedrock with high salinity (50‰), pH ~ 8.2. It is an indicator of anoxic environments and tolerates low-oxygen conditions (Moodley and Hess, 1992). As an infaunal taxon you can find it up to 10 cm below the surface of the sea bottom. In the Mediterranean it is a dominant species in lagoons and marshes. It is located on the outer shelf (Lionaki, 2012). Stratigraphic range Paleogene to Recent (Brodniewicz, 1972).

Kingdom: Animalia Linnaeus, 1758

Phylum: Mollusca Linnaeus, 1758

Class: Gastropoda Cuvier, 1795

Order: Littorinimorpha Golikov & Starobogatov, 1975

Family: Bithyniidae Gray, 1857 Genus: Bithynia Leach, 1818 Ecology This genus is found in a wide range of aquatic habitats - streams, rivers, canals, large drains, marsh drains and lakes, but is less common in smaller ponds. It shows a strong preference for richly vegetated habitats, often with muddy or silty substrates (Seddon, 2014).

Family: Valvatidae J. E. Gray, 1840 Genus: Valvata O. F. Müller, 1773 Species: Valvata cristata O. F. Müller, 1774 37

Ecology This species is found in freshwater environments (Mackie et al., 1980).

Family: Hydrobiidae Stimpson, 1865 Genus: Hydrobia Hartmann, 1821 Species: Hydrobia acuta Draparnaud, 1805 Ecology Represent an interface dweller between freshwater habitats and marine conditions. It is a typical species of brackish waters (tolerates up to 33‰ salinity) (Meric et al., 2001).

Kingdom: Animalia Linnaeus, 1758

Phylum: Mollusca Linnaeus, 1758

Class: Bivalvia Linnaeus, 1758

Order: Cardiida Ferussac, 1822

Family: Cardiidae Lamarck, 1809 Genus: Cerastoderma Poli, 1795 Species: Cerastoderma glaucum Bruguière, 1789 (Fig. 15: A) Ecology A shallow water species (Kotta et al., 2006), that lives in a wide range of salinities from 11 to 45 ‰ (Rygg, 1970)

Order: Mytilida Férussac, 1822

Family: Mytilidae Rafinesque, 1815 (Fig. 15: B) Ecology Mytilidae are found in coastal areas, are eurythermal and able to withstand freezing conditions for several months (Walters & Seed, 2006)

Plate 1: 1: Cyprideis torosa (un-noded morphotypes) male LV external view 2: Cyprideis torosa (un-noded morphotypes) male LV internal view, 3: Cyprideis torosa (un-noded morphotypes) male RV external view 4: Cyprideis torosa (un-noded morphotypes) male RV internal view, 5: Cyprideis torosa (un-noded morphotypes) female LV external view 6: Cyprideis torosa (un-noded morphotypes) female LV internal view, 7: Cyprideis torosa (un-noded morphotypes) female RV external view 8: Cyprideis torosa (un-noded morphotypes) female RV internal view, 9: Cyprideis torosa (un-noded morphotypes) juvenile LV external view, 10: Cyprideis torosa (un-noded morphotypes) juvenile RV external view, 11: Cyprideis torosa (noded morphotypes) male RV external view, 12: Cyprideis torosa (noded morphotypes) female LV external view, 13: Candona neglecta juvenile internal view 14: Candona neglecta juvenile external view, 15: Candona neglecta RV external view, 16: Leptocythere rara external view, 17: Ilyocypris gidda external view 18: Ilyocypris gidda internal view, 19: Charophyte, 20: Cytheridea neapolitana internal view 21: Cytheridea neapolitana external view, 22: Loxoconcha elliptica external view 23: Loxoconcha elliptica internal view, 24: Haynesina depressula, 25: Ammonia beccarii, 26: Elphidium crispum, 27: Quinqueloculina seminula. Scale bar: 200 μm

7. RESULTS OF MICROPALAEONTOLOGICAL ANALYSES Based on the collected data (see Annex I and II), relative abundance diagrams and statistic data were plotted for each section.

7.1 Section M 7.1.1 RELATIVE ABUNDANCE DIAGRAMS Relative abundance diagrams for the dominant species were plotted and taphonomic indices (Right/Left valve ratio, Sex ratio, Adult/Juvenile ratio and Carapace/Disarticulated Valves ratio) were also calculated for the most abundant species and were plotted (Fig. 16).

Based on the relative abundance diagrams and the taphonomic indices, five main units can be distinguished (Fig. 16):

Unit Α (0-3.4 m) is mainly characterized by the presence of C. torosa and the minor contribution of C. neglecta. The taphonomic indexes of C. neglecta are: A/J ratio < 1:25 and the R/L ratio ≥ 1, whereas for C. torosa (Fig. 16) the A/J ratio is between 1:12 and 1:4 and the R/L ratio is almost 1.

Unit B (3.4-7.6 m) is mainly characterized by the presence of C. torosa and the minor contribution of C. neglecta and I. gibba. About the taphonomic indices of C. neglecta the A/J ratio is < 1:25 and the R/L ratio is > 1, whereas as far as the taphonomic indices of C. torosa (Fig. 16) are concerned, the A/J ratio is between 1:12 and 1:4 and the R/L ratio is between 1 and 2. At 5.30 meters, where I. gibba is present, the A/J ratio of C. torosa is 0.5 and at 5.50 meters the RV/LV ratio of C. neglecta is 0.4.

Unit C (7.6-14.60 m) is mainly characterized by the presence of C. torosa and the minor contribution of C. neglecta. About the taphonomic indices of C. neglecta, the A/J ratio is < 1:25 and the R/L ratio is ≥ 1, whereas as far as the taphonomic indices of C. torosa (Fig. 16) are concerned, the A/J ratio is between 1:12 and 1:4 and the R/L ratio is almost 1.

Unit D (14.61-23.50 m) consists of barren coarse-grained sediments (Fig. 14), while Unit E (23.50- 31.30 m) is represented mainly by C. torosa, C. neglecta and small numbers of I. gibba valves (Fig. 16). About the taphonomic indices of C. neglecta, the A/J ratio is < 1:25, the R/L ratio is almost 1 and the C/D ratio is >0. On the other hand, about the taphonomic indices of C. torosa, the A/J ratio is between 1:10 and 1:2, the RV/LV ratio is almost 1 and the C/V ratio is >0 at 24.30 meters. Also, in this unit at 25.7 meters, where the I. gibba was present, the C/V ratio of C. neglecta is 0.1 and at 29.90 m, where the I. gibba was also present, the A/J ratio of C. torosa is 0.56 (Fig. 16). 40

Fig. 16 Stratigraphic column of section M, taphonomic indices of the two dominant species, relative abundance diagrams of three selected species. Based on the abundance diagrams and the respective taphonomic indices, five main units can be distinguished (Units: A, B, C, D and E)

7.1.2 STATISTICAL ANALYSIS The diagram below illustrates the Clustering analysis performed in Q mode (samples) of the percentage values of the species, using Bray-Curtis similarity index (Fig. 17). Bray-Curtis is the most commonly used index to express relationships in ecology and environmental sciences. It was used because it is the most suitable for ecological data (it examines species that only appear in at least one of the samples). The horizontal axis shows the depths of the samples.

Two separate clusters (1 and 2) are created. All the barren samples of unit D and the rest of the samples of the other units characterized by very few ostracods are grouped in cluster 1, while all the samples that contained sufficient numbers of valves are grouped in cluster 2. At a similarity level of 0.1, this latter cluster is separated into two sub-clusters (3 and 4). Sub-cluster 3 groups the samples of unit E collected between 23.50-24.50 m. The samples with depth 23.50-24.50 m characterized by presence of I. gibba and taphonomic indexes of C. torosa show variations (Fig. 16). Sub-cluster 4 is still a mix of the four fossiliferous units but a rather high level of similarity (0.58) it splits into two further sub-clusters (5 and 6). Sub-cluster 5 groups the samples of units B and the remaining samples of Unit E in which are present mainly C. torosa, C. neglecta and small numbers of I. gibba valves, whereas sub-cluster 6 groups the samples of units A and C which are mainly characterized by the presence of C. torosa and the minor contribution of C. neglecta.

Fig. 17 Cluster analysis plot based on the percentage values of the species. The diagram is separated in 2 main clusters and 3 sub- clusters.

The diagram below shows the Correspondence analysis performed in Q mode (samples) of based in the matrix of the percentage values of the species (Fig. 18). The samples form 3 clouds. The first one (blue color), groups the samples of units A and C that are mainly characterized by the presence of C. torosa and the minor contribution of C. neglecta; the second one (light blue color), groups the samples of units B and E that includes mainly C. torosa, C. neglecta and small numbers of I. gibba valves. The second group has a subgroup (violet color) which groups all the samples of units B and E that are represented mainly by C. neglecta and I. gibba (Fig. 16).

Fig. 18 Diagram of Correspondence analysis based on the percentage values of the species. The diagram is separated in 2 groups, a group with samples of units A and C (blue color), a group with samples of units B and E (light blue color)) and a subgroup, which is part of the group with the samples of units B and E (red color).

Finally, the diagram below illustrates the Diversity indices (Taxa_S, Simpson, Shannon and Evenness) of the species of the section M (Fig. 19). In unit A the index Taxa_S is ranging from 1 to 4, Simpson from 0 to 0,1472 (with a small raise in the upper part of the unit), Shannon from 0 to 0,2788 (with a small raise in the upper part of the unit) and Evenness from 0,3297 to 1 (with some fluctuations at 100 (0,3883), 160 (1) and 220 (0,3297) cm). In unit B the index Taxa_S is ranging from 1 to 4, Simpson from 0 to 0,6606 (with a raise at 530 cm), Shannon from 0 to 1,144 (with a raise at 530 cm) and Evenness from 0,5515 to 1 (with some fluctuations from 550 to 610 cm). In unit C the index Taxa_S is ranging from 1 to 3, Simpson from 0 to 0,0586, Shannon from 0 to 0,1957 and Evenness from 0,3883 to 1 (with some strong fluctuations at 945 (1), 1380 (1) and 1460 (1) cm). Unit D consists of barren sediments, while in unit E the index Taxa_S is ranging from 1 to 4, Simpson from 0,0198 to 0,5877, Shannon from 0,056 to 0,9653 and Evenness from 0,3689 to 0,8752. In unit E strong fluctuations occurred to all indices.

Fig. 19 Diagram of the Diversity indices (Taxa_S, Simpson, Shannon and Evenness) of the percentage values of the species and five main units that can be distinguished (Units: A, B, C, D and E)

7.2 Section K 7.2.1 RELATIVE ABUNDANCE DIAGRAMS Relative abundance diagrams for the dominant species were plotted. The taphonomic index Adult/Juvenile ratio, was also calculated only for C. torosa, which is represented mainly by juveniles. Moreover, the Ammonia-Elphidium Index (IAE) was also calculated for the samples where Ammonia and Elphidium species were present. Based on the relative abundance diagrams six main units can be distinguished (Fig. 20).

Unit Α (0-1.5 m) is mainly characterized by the presence of juveniles of C. torosa and the minor contribution of L. rara, A. beccarii and A. tepida. The taphonomic index for C. torosa (A/J ratio) is < 1:25.

Unit B (1.5-12.70 m) is mainly characterized by the presence of L. elliptica, C. neapolitana, A. beccarii, A. tepida and H. depressula and the minor contribution of juveniles of C. torosa, L. rara, E. advenum, E. crispum and Q. seminula. At 11.1 m, where an authochthnous? thanatocoenosis

event took place, it is represented by the presence of L. elliptica, A. beccarii, A. tepida, H. depressula and the sharp discontinuation of gastropods and bivalves.

Unit C (12.70-18 m) is mainly characterized by the presence of juveniles of C. torosa and the minor contribution of A. beccarii. The taphonomic index for C. torosa (A/J ratio) is 0.

Unit D (18-23 m) is mainly characterized by the presence of juveniles of C. torosa and juveniles of C. neglecta and the minor contribution of A. beccarii and H. depressula. The taphonomic index for C. torosa (A/J ratio) is 0.

Unit E (23-25.3 m) is represented only by juveniles of C. torosa. The taphonomic index for C. torosa (A/J ratio) is 0

Unit F (25.3-27.2 m) consists of barren sediments.

Fig. 20 Stratigraphic column of section K, relative abundance diagrams of selected species. Based on the abundance diagrams six main units can be distinguished (Units: A, B, C, D, E and F). Th is the “In-situ thanatocoenosis event”.

7.2.2 STATISTICAL ANALYSIS The diagram below illustrates the Cluster analysis performed in Q mode (samples) of the percentage values of the species using Bray-Curtis similarity index (Fig. 21).

Two separate clusters are created (1 and 2). All barren samples of unit F as well as of the other units, are grouped in cluster 1, while all the samples that contained sufficient numbers of tests and valves are grouped in cluster 2. at the significant similarity value of 0.1 this latter cluster splits into two sub-clusters (3 and 4). Cluster 3 contains the samples of unit B, represented mainly by foraminifera and marine ostracods, whereas cluster 4 groups the samples of units A, C, D and E represented mainly by juveniles of C. torosa.

Fig. 21 Diagram of Clustering analysis of the percentage values of the species. The diagram is separated in 2 clades and 2 sub- clades.

The diagram below illustrates the Correspondence analysis performed in Q mode (samples) of the percentage values of the species (Fig. 22). The samples form 5 clouds. The first one groups samples where percentage values of A. beccarii are from 68 to 78%, A. tepida are from 5 to 20%, H. depressula are from 1 to 13% and of C. torosa are from 1 to 14% (all samples from unit B from 4.50 to 4.90m and from 8.30 to 9.10m) . The second one groups samples where percentage values of A. beccarii are from 36 to 79%, A. tepida are from 0 to 45%, H. depressula are from 0 to 34% and of C. torosa are from 0 to 32% (all samples from unit B, most of them, from 1.50 to 2.30m and from 6.90 to 7.50m). The third one groups samples where percentage values of A. beccarii are from 0 to 59%, A. tepida are from 0 to 25%, H. depressula are from 0 to 70% and of C. torosa are from 0 to 99% (samples from units A, B, E and D) (Fig. 22). The fourth one groups samples where 46

percentage values of A. beccarii are from 2 to 8%, A. tepida are from 0 to 7%, H. depressula are 0% and of C. torosa are from 77 to 100% (samples from units A and C). Finally, the fifth one groups samples where percentage values of A. beccarii are from 5 to 21%, A. tepida are from 2 to 9%, H. depressula are from 7 to 8%, C. torosa are from 0 to 4% and of L. elliptica are from 47 to 73% (all samples from unit B from 9.70 to 10.30 m).

Fig. 22 Diagram of Correspondence analysis of the percentage values of the species. The diagram is separated in 5 groups, a group with samples, where percentage values of A. beccarii is from 68 to 78%, A. tepida is from 5 to 20%, H. depressula is from 1 to 13% and of C. torosa is from 1 to 14%, (1), a group with samples, where percentage values of A. beccarii is from 36 to 79%, A. tepida is from 0 to 45%, H. depressula is from 0 to 34% and of C. torosa is from 0 to 32%, (2), a group with samples, where percentage values of A. beccarii is from 0 to 59%, A. tepida is from 0 to 25%, H. depressula is from 0 to 70% and of C. torosa is from 0 to 99%, (3), a group with samples, where percentage values of A. beccarii is from 2 to 8%, A. tepida is from 0 to 7%, H. depressula is 0% and of C. torosa is from 77 to 100%, (4) and a group with samples, where percentage values of A. beccarii is from 5 to 21%, A. tepida is from 2 to 9%, H. depressula is from 7 to 8% , C. torosa is from 0 to 4% and of L. elliptica is from 47 to 73% (5)

Moreover, the diagram below depicts the Diversity indices (Taxa_S, Simpson, Shannon and Evenness) of the percentage values of the species of section K (Fig. 23). In unit A, the index Taxa_S is ranging from 1 to 5, Simpson from 0 to 0,4032, Shannon from 0 to 0,8475 and Evenness from 0,4204 to 1. In unit B, the index Taxa_S is ranging from 2 to 8, Simpson from 0,3606 to 0,8054, Shannon from 0,6022 to 1,728 and Evenness from 0,5515 to 1. In unit C, the index Taxa_S is ranging from 1 to 3, Simpson from 0 to 0,0586, Shannon from 0 to 0,1957 and Evenness from 0,3532 to 0,946. In unit D, the index Taxa_S is ranging from 1 to 3, Simpson from 0 to 0,1314, Shannon from 0 to 0,2823 and Evenness from 0,4168 to 1. In unit E, the index Taxa_S is 1, Simpson is 0, Shannon is 0 and Evenness is 1. Unit F consists of barren sediments.

Fig. 23 Diagram of the Diversity indices (Taxa_S, Simpson, Shannon and Evenness) of the percentage values of the species and six main units that can be distinguished (Units: A, B, C, D, E and F).

Finally, the Ammonia-Elphidium Index was also calculated only for the samples of Unit B (Fig. 24). The IAE from 1.50 to 2.50 m is 100, from 2.70 to 4.10 m is ranging from 61,90476 to 98,969072, from 4.30 to 4.70 m is 100, from 4.90 to 5.50 m is ranging from 85,71428 to 97,77777, from 5.70 to 6.30 m is 100, from 6.60 to 9.90 m is ranging from 82,35294 to 100 and from 10.10 to 12.50 m is 100 except the sample at 11.90 m, that is 92,53731.

Fig. 24 Diagram of the Ammonia-Elphidium Index were also calculated only for the samples of Unit B

8. DISCUSSION

Based on the results of the micropalaeontological analyses palaeoenvironmental interpretation can be indicate.

8.1 Section M Generally, a lagoonal environment with several variations in the salinity and the mean depth occurred.

Unit Α (0-3.4 m) is mainly characterized by the presence of C. torosa (mainly characterized by un- noded morphotypes) and the minor contribution of C. neglecta. Based on the taphonomic indices of C. neglecta, Unit A is characterized by the locally focused deposition of more easily transported juvenile valves (A/J ratio < 1:25 & R/L ratio ≥ 1), thus representing hydrodynamic transport, whereas the taphonomic indices of C. torosa (Fig. 25) may represent an in-situ death assemblage, with reduced taphonomic removal of juveniles which therefore can be characterized as a life assemblage (A/J ratio 1:12-1:4 & R/L ratio ≈1). So, unit A, represented in cluster 6, can be characterized as a lagoon environment with small freshwater influxes that, anyway, are not enough to lower the salinity below 16‰ to lead C. neglecta to inhabit it.

Unit B (3.4-7.6 m) is mainly characterized by the presence of C. torosa (mainly characterized by un- noded morphotypes with a small increase of noded morphotypes from 5.30 to 6.10 m) and the minor contribution of C. neglecta and I. gibba (samples in cluster 5). Based on the taphonomic indices of C. neglecta, Unit B is characterized by the locally focused deposition of more easily transported juvenile valves (A/J ratio < 1:25 & R/L ratio > 1), thus representing hydrodynamic transport, whereas the taphonomic indices of C. torosa (Fig. 18) may represent an in-situ death assemblage, with reduced taphonomic removal of juveniles which therefore can be characterized as a life assemblage (A/J ratio 1:12-1:4 & R/L ratio 1-2). At 5.30 m the presence of I. gibba, the A/J ratio (0.5) of C. torosa (un-noded morphotypes) and the RV/LV ratio (0.4) of C. neglecta at 5.50 m indicate an in situ assemblage, recording a short freshwater influx that, possibly, lowered the water salinity sown to 5‰. So, unit B can be characterized as a lagoon environment with freshwater influxes (Fig.25).

Unit C (7.6-14.60 m) is mainly characterized by the presence of C. torosa (mainly characterized by un-noded morphotypes) and the minor contribution of C. neglecta. Based on the taphonomic indices of C. neglecta, Unit C is characterized by the locally focused deposition of more easily 50

transported juvenile valves (A/J ratio < 1:25 & R/L ratio ≥ 1), thus representing hydrodynamic transport, whereas the taphonomic indices of C. torosa (un-noded morphotypes) (Fig. 18) may represent an in-situ death assemblage, with reduced taphonomic removal of juveniles which therefore can be characterized as a life assemblage (A/J ratio 1:12-1:4 & R/L ratio ≈1). So, unit C, whose samples are grouped in cluster 6, can be records again a lagoon environment with small freshwater influxes similarly to Unit A. The freshwater influxes, anyway, are not enough to lower the salinity below 16‰ to lead C. neglecta to inhabit it (Fig.25).

Unit D (14.61-23.50 m), represented by cluster 1, consists of barren coarse-grained sediments, so unit D can be characterized as river mouth deposits from a river outflowing in the lagoon (Fig. 18).

Unit E (23.50-31.30 m) is represented mainly by C. torosa (mainly characterized by un-noded morphotypes with increases of noded morphotypes from 23.50 to 26.90 m), C. neglecta and small numbers of I. gibba valves (Fig. 18) (samples in cluster 5). Based on the taphonomic indices of C. neglecta (A/J ratio < 1:25, R/L ratio ≈1 & C/D ratio >0), unit E may reflect not only low-energy conditions (samples grouped in cluster 5), but also potential mass kill events associated with increased sedimentation rates (smothering via settling of fine-grained sediment from river flood discharge) (sub-cluster 3 groups the samples of unit E with depth 23.50-24.50 m, that indicate a possible flood event). On the other hand, based on the taphonomic indices of C. torosa (A/J ratio 1:10-1:2, R/L ratio ≈1 & C/D ratio >0 at 24.30 m) an in-situ death assemblage (possible flood event) can be considered, where possibly the taphonomic removal of most juveniles occurred (Fig. 18). Also, in this unit at 25.7 m, the presence of I. gibba and the C/V ratio (0.1) of C. neglecta and at 29.90 m, the presence of I. gibba and the A/J ratio (0.56) of C. torosa (un-noded morphotypes) indicate freshwater influxes. So, unit E can be characterized as a lagoon environment with strong freshwater influxes which lowered the water salinity possibly down to 5‰ (Fig.25). It is worth to note that, according to the cluster analysis, Units B and E cluster together, but, according to the taphonomic indexes, the two lagoon environment they represent are, respectively, affected by little and strong freshwater influxes.

Fig. 25 Stratigraphic column of section M, taphonomic indices, relative abundance diagrams of selected species and five main units that can be distinguished (Units: A, B, C, D and E) with their palaeoenvironmental interpretation. The red lines show the freshwater influxes and the blue line at 24.30m show the possible flood event.

According to the Clustering analysis (Fig. 17 and 26), clade 1 gathers the samples of unit D, that indicate river mouth deposits from a river outflowing in the lagoon, sub-clade 3 gathers the samples of unit E with depth 23.50-24.50 m, that indicate a possible flood event (according to the relative abundance diagrams (Fig. 25) in depth of 24.30 m an in-situ death assemblage can be considered), sub-clade 5 gathers the samples of units B and E, that indicate a lagoon environment with strong freshwater influxes and sub-clade 6 gathers the samples of units A and C, that indicate a lagoon environment with small freshwater influxes.

Fig. 26 Diagram of Clustering analysis of the percentage values of the species. The diagram is separated in 2 clades and 4 sub- clades. Clade 1: samples of unit D, that indicate river mouth deposits from a river outflowing in the lagoon, sub-clade 3: samples of unit E with depth 23.50-24.50 m, that indicate a possible flood event, sub-clade 5: samples of units B and E, that indicate a lagoon environment with strong freshwater influxes and sub-clade 6: samples of units A and C, that indicate a lagoon environment with small freshwater influxes.

Considering this environmental interpretation, the axis one should represent the environmental parameter “salinity” decreasing from the left to the right (Fig. 27).

Fig. 27 Diagram of Correspondence analysis of the percentage values of the species. The diagram is separated in 2 groups. A group with samples of units A and C (blue color), that indicate a lagoon environment with small freshwater influxes. A group with samples

of units B and E (light blue color), that indicate a lagoon environment with strong freshwater influxes and a subgroup (red color), which is gathers all the samples of units B and E, that indicate freshwater influxes.

Finally, according to the Diversity indices (Fig. 19), generally, species number is very low, and reveals deteriorated environments (Frenzel and Boomer, 2005). Simpson index values were observed to be low and this means that most of the species were present in low frequencies. The Shannon index values are very low, indicating a low number of rare species and Evenness index fluctuations indicates the moderate uniformity of the samples.

The fact that C. torosa (un-noded morphotypes) is the most abundant species and C. torosa (noded morphotypes) has minor contribution, indicate that the salinity presents strong fluctuations.

So, palaeonvironmental changes at section M occurred due to eustatism. Initially a high mesohaline lagoon system turned gradually into a lagoonal river mouth environment (barren layers) due to the sea level fall and finally when the sea level rose again the environment turned one nore to a lagoonal environment more strongly influenced by the riverine waters that lowered the water salinity to oligohaline and, at least once, affected the lagoon with a possible flood event.

8.2 Section K Generally, a lagoonal environment with several variations in the salinity and the mean depth occurred.

Unit Α (0-1.5 m) is mainly characterized by the presence of C. torosa and the minor contribution of L. rara, A. beccarii and A. tepida, so it can be characterized as a high mesohaline to polyhaline lagoon environment with small marine influxes (Fig. 29). Based on the A/J ratio of C. torosa (A/J ratio< 1:25), Unit A is characterized by the locally focused deposition of more easily transported juvenile valves being deposited in a low-energy environment.

Unit B (1.5-12.70 m) is mainly characterized by the presence of L. elliptica, C. neapolitana, A. beccarii, A. tepida and H. depressula and the minor contribution of C. torosa, L. rara, E. advenum, E. crispum and Q. seminula. Few scattered samples bear also A. convexa. Based on the A/J ratio of C. torosa (A/J ratio< 1:25), Unit A is characterized by the locally focused deposition of more easily transported juvenile valves being deposited in a low-energy environment. At 11.1 m, where a thanatocoenosis event took place, it is represented by the presence of L. elliptica, A. beccarii, A. 54

tepida, H. depressula and the sharp discontinuation of bivalves (C. glaucum and Mytilidae). The barren samples that occur from 11.31 to 11.89 indicate probably an anoxic event. According to Kandeel et al. (2017), population dynamics of C. glaucum is controlled by abiotic factors such as salinity, temperature, immersion time, water velocity and sediment dynamics (Gam et al, 2010; Malham et al, 2012). Salinity may be the main factor affecting its abundance. Rygg (1970) tested the tolerance of C. glaucum in a range from 3 to 60 ‰ and found that this species lived in a wide range of salinities from 11 to 45 ‰, though it suffered high mortality rates. Also, C. torosa is resistant to salinities up to 60‰ (Kilenyi & Whittaker, 1974). Mediterranean Sea is not characterized by high salinity values (according to Science Learning Hub (2017) the higher it can get is 38 ‰), so another abiotic factor may be the main factor affecting the abundance of the species. Often, an anoxic event is caused by an excessive accumulation of organic matter (Nixon (1995), Guyoneaud et al. (1997), Karakassis et al. (2000), Lardicci et al. (2001), De Falco et al. (2004) and Magni et al. (2008)), such as the anoxic event in the Lesina lagoon (Specchiulli et al.

(2009)). Also, the reduction of O2 penetration by the restricted water movement and poor flushing rates and the water column stratification, which inhibits mixing of deep with surface water, could trigger an anoxic event (Maxted et al., 1997).

Based on the Ammonia-Elphidium Index (Fig. 28), in unit B the environment from 1.50 to 2.50 m can be characterized as an environment with low oxygenation level, from 2.70 to 4.10 m, it can be characterized as an environment with fluctuation of the oxygenation level, for the depth from 4.30 to 4.70 m, it can be characterized as an environment with low oxygenation level, from 4.90 to 5.50 m, it can be characterized as an environment with small fluctuation of low oxygenation level, from 5.70 to 6.30 m, it can be characterized as an environment with low oxygenation level, from 6.60 to 9.90 m it can be characterized as an environment with small fluctuation of oxygenation level and from 10.10 to 12.50 m it can be characterized as an environment with low oxygenation level. Finally, according to Levy (1970) A. tepida associated with Elphidium sp. and/or with Haynesina sp. and Q. seminula is a dominant taxon in Mediterranean lagoons that are subjected to anoxic episodes resulting from eutrophication. This dominant taxon occurred at 4.30, 5.10, 6.60, 9.70 and 11.90 m.

Fig. 28 Diagram of the Ammonia-Elphidium Index for Unit B. The environment from 1.50 to 2.50 m is characterized as an environment with low oxygenation level (red), from 2.70 to 4.10 m, is characterized as an environment with fluctuation of the oxygenation level (blue), for the depth from 4.30 to 4.70 m, is characterized as an environment with low oxygenation level (red), from 4.90 to 5.50 m,is characterized as an environment with small fluctuation of low oxygenation level (brown), from 5.70 to 6.30 m, is characterized as an environment with low oxygenation level (red), from 6.60 to 9.90 m is characterized as an environment with a small fluctuation of oxygenation level (blue) and from 10.10 to 12.50 m is characterized as an environment with low oxygenation level (red).

So, unit B can be characterized as an open polyhaline to euhaline lagoon environment with strong marine influxes (evidenced by the presence of A. convexa) and with strong fluctuations in salinity, with low oxygenation levels (possibly fluctuating from 2.70 to 4.10 m). A significant anoxic event possibly occurred at 11.10-11.70 m, whereas at 11.90 m a smaller anoxic event took place, and 4 small hypoxia events took place at 4.30, 6.60, 5.10 and 9.70 m. (Fig. 29).

Unit C (12.70-18 m) is mainly characterized by the presence of C. torosa and the minor contribution of A. beccarii. Sediments rich in gypsum are presenting this unit, so, it can be testify a closed lagoon environment (Fig. 29). Based on the A/J ratio of C. torosa (A/J ratio< 1:25), Unit C is

characterized by the locally focused deposition of more easily transported juvenile valves being deposited in a low-energy environment.

Unit D (18-23 m) is mainly characterized by the presence of C. torosa and C. neglecta and the minor contribution of A. beccarii and H. depressula. So, it can be characterized as a lagoon environment with freshwater influxes (Fig. 29). Based on the A/J ratio of C. torosa (A/J ratio< 1:25), Unit D is characterized by the locally focused deposition of more easily transported juvenile valves being deposited in a low-energy environment.

Unit E (23-25.3 m) is represented only by C. torosa, so, it can be characterized as a deteriorated lagoon environment (Fig. 29) Based on the A/J ratio of C. torosa (A/J ratio< 1:25), Unit E is characterized by the locally focused deposition of more easily transported juvenile valves being deposited in a low-energy environment.

Unit F (25.3-27.2 m) consists of barren sediments probably because of taphonomic factors or anoxic conditions (Fig. 29).

Fig. 29 Stratigraphic column of section Κ, relative abundance diagrams of selected species and six main units that can be distinguished (Units: A, B, C, D, E and F) with their palaeoenvironmental interpretation. Also, the red line shows the in-situ thanatocoenosis event (anoxic event), the red intermittent line the small anoxic event at 11.90 m and the blue lines show 4 small hypoxia events took place at 4.30, 6.60, 5.10 and 9.70 m. Unit A indicate a lagoon environment with small marine influxes, Unit B a lagoon environment with strong marine influxes, Unit C a closed lagoon environment, Unit D a lagoon environment with freshwater influxes, Unit E a closed lagoon environment and Unit F an environment maybe with anoxic conditions.

According to the Clustering analysis (Fig. 30), in the first separation we can notice that one of the clades gathers the samples of units A, C, D and E (which are represented mainly by C. torosa) 57

and the other one contains the samples of unit B (which is represented mainly by foraminifera and marine ostracods). This separation confirms the strong differentiation between the environment of unit B and the environments of the other units.

Fig. 30 Diagram of Clustering analysis of the percentage values of the species. The diagram is separated in 2 clades and 2 sub- clades. Clade 1: samples mainly of unit F, that indicate an anoxic environment , sub-clade 3: samples of unit B, that indicate an open lagoon environment with strong marine influxes and sub-clade 4: samples of units A, C, D and E, that indicate an closed lagoon environment with small freshwater influxes.

Also, according to the Correspondence analysis (Fig. 22) the diagram is separated in 5 groups. The first one, groups samples, characterizing an environment close to the marine end member and the second one, groups samples, is showing an environment less close to the oceanic end member. The third one, groups samples, is indicating an environment less close to the oceanic end member and more close to the continental end member, the fourth one, groups samples, is indicating an environment close to the continental end member and the fifth one, groups samples, that may indicate 4 sedimentation cycles. The first one from 1.50 to 3.50m, the second one from 3.51 to 5.30m, the third one from 5.31 to 7.90 and the last one from 7.91 to 10.30m. (Fig. 29 and 31).

Fig. 31 Diagram of Correspondence analysis of the percentage values of the species. The diagram is separated in 5 groups. The first one, groups samples, that indicate a lagoonal environment close to the oceanic end member, the second one, groups samples, that indicate an environment less close to the oceanic end member. The third one, groups samples, that indicate an environment less close to the oceanic end member and more close to the continental end member, the fourth one, groups samples that indicate an environment close to the continental end member and the fifth one, groups samples, that maybe indicate 4 annual sedimentation cycles. The first one from 1.50 to 3.50m, the second one from 3.51 to 5.30m, the third one from 5.31 to 7.90 and the last one from 7.91 to 10.30m.

According to the Diversity indices (Fig. 23), in units C, D and E, species number is very low (1-3), and reveals deteriorated environments (Frenzel and Boomer, 2005). Simpson index values were observed to be low and this means that most of the species were present in low frequencies. The Shannon index values are very low, indicating a low number of rare species and Evenness index fluctuations indicating a moderate-good amount of uniformity of the samples. In units A, species number is not very low (5) but Simpson index values were observed to be low and this means that most of the species were present with low abundancies. The Shannon index values are very low, indicating a low number of rare species and Evenness index fluctuations indicates the moderate uniformity of the samples. On the other hand, in unit B species number is higher (2-8), Simpson index values were observed to be moderate and this means that most of the species were present with relatively low abundancies. The Shannon index values are high, indicating a big number of rare species and Evenness index fluctuations indicating the moderate amount of uniformity of the samples.

Moreover, in Unit C, the sharp discontinuation of all foraminifera, the main contribution of C. torosa (un-noded morphotypes) and sediments rich in gypsum, indicate that the connection with the sea was blocked from time to time, and freshwater influx stopped, hence, as evaporation took place, salinity was getting increased.

So, palaeoenvironmental changes occurred due to eustatism. Initially a lagoon system with small marine influxes, turned into an open lagoon environment where, due to a sea level rise, suddenly it turned into an open lagoon environment with strong marine influxes, with strong salinity fluctuations in salinity, and with low oxygenation level (with small with fluctuation of the oxygenation level from 2.70 to 4.10 m). A significant anoxic event possibly occurred at 11.10-11.70 m, whereas at 11.90 m a smaller anoxic event took place, and 4 small hypoxia events took place at 4.30, 6.60, 5.10 and 9.70 m. Subsequently, when sea level dropped, the connection with the sea was closed and evaporation took place, as it became a closed lagoon environment with salinity higher than 45‰. The system at the end turned into a lagoon influenced by a river system with freshwater influxes. The sharp increase in salinity and the abrupt transition from an open lagoon to a closed lagoon environment is something that should be studied further, in case it could be related to Milankovitch cycles.

8.3 Age of the sections

Based on the stratigraphic distributions of the previous chapter, the dating of the sediments of the two sections was deduced, but ostracods do not permit a very detailed aging.

In samples of section M, most species have a wide range, except for C. neglecta (Pleistocene to Recent) and C. torosa (Early Pleistocene (Calabrian) to Recent, thus sediments should have been deposited from Early Pleistocene (Calabrian) to Recent (Chart. 1).

For section K, where most species occur, based on C. neglecta (Pleistocene to recent), C. torosa (Early Pleistocene (Calabrian) to Recent, the sediments were dated from Early Pleistocene (Calabrian) to Recent (Chart. 2).

Having C. neglecta and C. torosa a wide stratigraphic range it is not possible to base the age of the studied section on ostracods. Based on the references of Doutsos et al (1988), Frydas (1991), Doutsos and Poulimenos (1992), Stamatopoulos et al. (1994/2004), Frydas et al. (1995),

Kontopoulos & Zelilidis (1997), Palyvos et. al. (2007/2010) and Houghton et al. (2003) the age of the sections should be considered as Middle Pleistocene.

Species Stratigraphic range Candona neglecta Quaternary (Pleistocene) to Recent. (Krzyminska & Namiotko, 2013) Cyprideis torosa Early Pleistocene (Calabrian) to Recent. (Gliozzi et al., 2016, Krzyminska & Namiotko, 2013) Ilyocypris gibba Neogene (Miocene) to Recent. (Krzyminska & Namiotko, 2013) Aurila convexa. Neogene (Pliocene) to Recent (Mostafawi et al., 1969) Haynesina depressula Neogene (Late Pliocene) to Recent (Carboni, 2010) Ammonia tepida Neogene (Miocene) to Recent. (Le Campion, 1968, Rouvillois, 1970, Debenay, 1978, Redois, 1996) Chart 1: Species of section M and their Stratigraphic range

Species Stratigraphic range Candona neglecta Quaternary (Pleistocene) to Recent. (Krzyminska & Namiotko,2013) Cyprideis torosa Early Pleistocene (Calabrian) to Recent. (Gliozzi et al., 2016, Krzyminska & Namiotko, 2013) Cytheridea neapolitana Neogene (Pliocene) to Quaternary (Holocene) (Guernet et al., 2003) Loxoconcha elliptica Neogene (Miocene) to Recent. (Bonaduce et al.1975, Aranki 1987, Yassini 1979, Danatsas, 1989) Leptocythere rara Occurrence in Pleistocene sediments. (Tsapralis, 1981 and Danatsas, 1989) Aurila convexa. Neogene (Pliocene) to Recent (Mostafawi et al., 1969) Haynesina depressula Neogene (Late Pliocene) to Recent (Carboni, 2010) Ammonia tepida Neogene (Miocene) to Recent. (Le Campion, 1968, Rouvillois, 1970, Debenay, 1978, Redois, 1996) Ammonia beccarii Paleogene (Oligocene) to Recent (Loeblich & Tappan, 1988) Elphidium advenum Neogene (Miocene) to Recent. (Jones, 1994) Elphidium crispum Neogene (Miocene) to Recent. (Jones, 1994) Quinqueloculina seminula Paleogene to Recent (Brodniewicz, 1972) Chart 2: Species of section K and their Stratigraphic range

8.4 Correlation between the sections

The study area belongs to the tectonically controlled Rio –Antirio basin, which is part of the Corinth rift system. Although the basin is crossed by a dense array of faults, up to now, their control on the sedimentation is poorly described. This is an attempt of a bigger program that tries to understand how the active fault exerts control on the sedimentation. However, this is not a simple task. The distance between section M and section K is only 138 meters (Fig. 9) but, there is no obvious stratigraphic connection between the palaeoenvironments in the two sections. In section M a lagoon system, turned gradually into a lagoonal river mouth environment (barren layers) due to sea level drop and finally in a new course of sea level rise a lagoonal environment was established. In the former environments the influence of a river system is prevailing as is suggested by strong freshwater influxes. In section K a lagoon system, turned gradually into an open lagoon environment due to sea level rise and finally when sea level dropped, it became again a lagoonal environment influenced by a river system with freshwater influxes. The small distance among the sections and the difference of the palaeoenvironments indicate that the two sections are juxtaposed by a fault (Fig. 32). If this interpretation is correct, then the displacement on the fault is at least the thickness of the two sections.

Fig. 32 The palaeoenvironments and the effect of the fault

This interpretation agrees with Tsoni et. al. (2019) Mapping the faults of the study area indicates the existence of the fault between the two sections (Fig. 33, 34).

Because there is no stratigraphic correlation between sections M and K, and thus the total thickness of the sections resembles the displacement of the fault in the order of 60 m.

If these age determinations are correct, then the fault is active. However, it is impossible with the present data to define correctly the fault displacement. A possible estimation of the offset is 60 m suggesting a slip rate for the fault ranging between 0.1 to 0.4 mm/yr.

Fig. 33 Geological map with the faults of the study area and the two sections (M and K) (Tsoni et. al., submitted)

Fig. 34 Google Earth figure with the faults of the study area and the two sections (M and K)

8.5 Correlation with previous studies Both the sections indicate a Middle Pleistocene lagoonal environment.

Kontopoulos and Zelilidis (1997), determined the sediments of Argyra, Kastritsi and Romanos as: Plio-Pleistocene in age marine/lagoonal deposits, Lower Pleistocene in age proximal braided river deposits, and Middle to Upper Pleistocene in age lagoonal deposits and Upper Pleistocene the alluvial fans. Also, in 2010, Palyvos et. al. indicated the sequence of layers (from brackish environment sediments to shallow marine sediments, from shallow marine sediments to brackish environment sediments again and finally, from brackish environment sediments to lacustrine and fluvial sediments) of Aravonitsa (Location 10) as Middle Pleistocene. Determined the marine deposits of Aravonitsa (Location 10) as Middle Pleistocene (biozone MNN20: 270–440 ka) so the following brackish deposits were determined as Middle Pleistocene or younger. Also C. glaucum is one of the fossils that were found in the part of the brackish environment deposits.

The palaeo-environmental interpretation of sections M and K of the Middle Pleistocene lagoonal deposits of Magoula, could correlate with a part of the Middle to Upper Pleistocene the lagoonal deposits of Kontopoulos and Zelilidis (1997) and the Middle Pleistocene or younger brackish environment deposits of Palyvos et. al. (2010) (Fig. 35).

Fig. 35 The palaeo-environmental interpretation of sections M and K of the Middle Pleistocene lagoonal deposits of Magoula, could correlate with a part of the Middle to Upper Pleistocene the lagoonal deposits of Kontopoulos and Zelilidis (1997) and the Middle Pleistocene or younger brackish environment deposits of Palyvos et. al. (2010)

9. CONCLUSIONS

1. At section M, according to micropalaeontological and taphonomic analysis, palaeonvironmental changes occurred due to relative sea level variations. Initially a lagoon system turned gradually into a lagoonal river mouth environment (barren layers) due to a sea level drop and finally, when sea level rose, it became again a lagoonal environment influenced by a river system with strong freshwater influxes. The relative abundance diagrams and the taphonomic indices in combination with the stratigraphic column characterize a possible flood event at 24.10-24.30 meters. 2. Section K, according to micropalaeontological analyses, can be characterized by palaeonvironmental changes that occurred due to relative sea level changes. Initially, a lagoon system with small marine influxes turned into an open lagoon environment due to a sea level rise; marine influxes were strong as well as fluctuations in salinity and oxygen content. A significant anoxic event possibly occurred at 11.10-11.70 m, whereas at 11.90 m a smaller anoxic event took place, and 4 small hypoxia events took place at 4.30, 6.60, 5.10 and 9.70 m. Later, when the sea level dropped, the connection with the sea was closed and evaporation took place, as it became a closed lagoonal environment with salinity higher than 45‰. At the end, the system turned into a lagoon influenced by a river system with freshwater influxes. 3. Four sedimentation cycles are possibly present in Unit B of section K. The first one from 1.50 to 3.50m, the second one from 3.51 to 5.30m, the third one from 5.31 to 7.90 and the last one from 7.91 to 10.30m. 4. In section K the sharp increase in salinity and the abrupt transition from an open lagoon environment to a closed lagoon environment is something that should be studied further in case it is related to Milankovitch cycles. 5. The age of the sections, based on datings from nearby sections, is considered as Middle Pleistocene. 6. The small distance among the sections and the difference of the palaeoenvironments indicate the presence of an active fault (Fig. 32, Fig. 33). 7. The displacement of the fault is at least 58.5 meters (the total high of the sections). 8. A part of the Middle to Upper Pleistocene lagoon deposits of Kontopoulos and Zelilidis (1997) and the Middle Pleistocene or younger brackish environment deposits of Palyvos et. al. (2010) can be correlated with the Middle Pleistocene lagoon deposits of Magoula.

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Annex I Sample Depth (cm) Candona neglecta Cyprideis torosa Leptocythere rara Ilyocypris gibba Aurila convexa Haynesina depressula Ammonia tepida total 1 20 13 254 0 0 0 0 0 267 2 40 2 301 0 0 1 0 0 304 3 60 0 0 0 0 0 0 0 4 80 9 560 1 0 0 2 1 573 5 100 4 234 2 0 0 0 0 240 6 120 6 252 0 0 0 0 1 259 7 140 10 373 1 0 0 0 0 384 8 160 0 73 0 0 0 0 0 73 9 180 2 320 0 0 0 0 0 322 10 200 8 320 0 0 0 0 0 328 11 220 8 180 1 0 1 0 0 190 12 240 14 254 0 1 0 0 0 269 13 260 7 182 0 0 0 0 0 189 14 280 9 274 0 1 0 0 0 284 15 300 7 84 0 0 0 0 0 91 16 340 1 3 0 0 0 0 0 4 17 370 0 0 0 0 0 0 0 0 18 400 0 2 0 1 0 0 0 3 19 430 0 0 0 0 0 0 0 0 20 460 0 0 0 0 0 0 0 0 21 490 0 0 0 0 0 0 0 0 22 510 0 0 0 0 0 0 0 0 23 530 18 21 0 11 0 0 1 51 24 550 6 118 0 0 0 0 0 124 25 580 0 55 1 0 0 0 0 56 26 610 0 54 0 0 0 0 0 54 27 640 0 0 0 0 0 0 0 0 28 670 0 0 0 0 0 0 0 0 29 700 0 0 0 0 0 0 0 0 30 730 0 0 0 0 0 0 0 0 31 760 0 0 0 0 0 0 0 0 32 780 2 116 0 0 0 0 0 118 33 805 3 230 0 0 0 0 0 233 34 840 1 114 0 0 0 0 0 115 35 860 7 122 0 0 0 0 0 129 36 865 3 208 0 0 0 0 0 211 37 885 1 134 0 0 0 0 0 135 38 900 1 187 0 0 0 0 0 188 39 905 6 297 0 0 1 0 0 304 40 935 9 155 0 0 0 0 0 164 41 945 0 168 2 0 0 0 0 170 42 965 6 330 0 0 0 0 0 336 43 985 4 228 0 0 0 0 0 232 44 1015 7 330 0 0 0 0 0 337 45 1035 10 528 0 0 0 0 0 538 46 1055 9 467 0 0 0 0 0 476 47 1075 2 262 0 0 0 0 0 264 48 1090 2 260 0 0 0 0 0 262 49 1110 5 356 0 0 0 0 0 361 50 1130 13 370 0 0 0 0 0 383 51 1160 5 382 1 0 0 0 1 389 52 1180 3 380 0 0 0 0 0 383 53 1200 13 389 0 0 0 0 0 402 54 1205 2 304 0 0 0 0 0 306 55 1230 3 143 0 0 0 0 0 146 56 1250 5 236 0 0 0 0 0 241 57 1270 2 277 0 0 1 0 0 280 58 1285 0 303 0 0 2 0 0 305 59 1300 7 284 0 0 6 0 0 297 60 1320 3 190 0 0 1 0 0 194 61 1340 4 189 0 0 1 0 0 194 62 1360 3 276 0 0 0 0 0 279 63 1380 0 159 0 0 0 0 0 159 64 1400 7 291 0 0 0 0 1 299 65 1420 5 295 0 0 0 0 0 300 66 1440 2 101 0 0 0 0 0 103 67 1460 0 80 0 0 0 0 0 80 68 1480 0 21 0 0 0 0 0 21 69 1500 0 22 0 0 0 0 0 22 70 1530 0 0 0 0 0 0 0 0 71 1550 0 0 0 0 0 0 0 0 72 1570 0 0 0 0 0 0 0 0 73 1590 0 0 0 0 0 0 0 0 74 1610 0 0 0 0 0 0 0 0 75 1630 0 0 0 0 0 0 0 0 76 1650 0 0 0 0 0 0 0 0 77 1670 0 0 0 0 0 0 0 0 78 1680 0 0 0 0 0 0 0 0 79 1700 0 0 0 0 0 0 0 0 80 1720 0 0 0 0 0 0 0 0 81 1740 0 0 0 0 0 0 0 0 82 1750 0 0 0 0 0 0 0 0 83 1810 0 0 0 0 0 0 0 0 84 1818 0 0 0 0 0 0 0 0 85 1870 0 0 0 0 0 0 0 0 86 1872 0 0 0 0 0 0 0 0 87 2230 0 0 0 0 0 0 0 0 - 2280 0 0 0 0 0 0 0 0 88 2290 0 0 0 0 0 0 0 0 89 2310 0 0 0 0 0 0 0 0 90 2330 7 0 0 0 2 0 0 9 91 2350 157 41 0 16 0 0 0 214 92 2370 80 147 0 6 0 0 0 233 93 2390 151 138 0 18 0 0 0 307 94 2410 222 20 0 43 0 0 0 285 95 2430 75 9 0 17 0 0 0 101 96 2450 165 56 0 21 0 0 0 242 97 2470 1 154 0 0 0 0 0 155 98 2498 0 0 0 0 0 0 0 0 99 2512 0 0 0 0 0 0 0 0 100 2521 0 0 0 0 0 0 0 0 101 2534 0 0 0 0 0 0 0 0 102 2556 0 0 0 0 0 0 0 0 103 2570 10 75 0 6 0 0 3 94 104 2590 31 268 0 5 0 0 0 304 105 2610 26 277 0 3 0 0 3 309 106 2630 17 59 0 5 0 0 2 83 107 2650 55 31 0 5 0 0 0 91 108 2670 27 29 0 1 0 0 0 57 109 2690 24 285 0 2 0 0 0 311 110 2715 0 0 0 0 0 0 0 0 111 2725 0 0 0 0 0 0 0 0 112 2735 0 12 0 0 0 0 0 12 113 2750 0 0 0 0 0 0 0 0 114 2770 0 0 0 0 0 0 0 0 115 2790 5 39 0 0 0 0 0 44 116 2815 41 270 0 0 0 0 0 311 117 2825 0 0 0 0 0 0 0 0 118 2840 0 0 0 0 0 0 0 0 119 2848 0 0 0 0 0 0 0 0 120 2856 0 0 0 0 0 0 0 0 121 2895 0 0 0 0 0 0 0 0 122 2910 0 0 0 0 0 0 0 0 123 2930 0 0 0 0 0 0 0 0 124 2950 0 0 0 0 0 0 0 0 125 2970 0 0 0 0 0 0 0 0 126 2990 155 108 0 37 0 0 0 300 127 3010 44 90 0 2 2 0 0 138 128 3030 47 81 0 7 1 0 0 136 129 3050 51 91 0 4 3 0 0 149 130 3070 9 29 0 3 0 0 0 41 131 3085 0 0 0 0 0 0 0 0 132 3115 0 0 0 0 0 0 0 0 133 3130 0 0 0 0 0 0 0 0 Chart 3 Data with the valves of each species of each sample and the total number of valves of section M

Cyprideis torosa Sample Depth (cm) RV/LV ratio F/Mratio A/Jratio C/Vratio 1 20 0,926829268 10 0,040740741 0 2 40 1,066225166 9 0,048780488 0 3 60 0 0 0 0 4 80 1,180555556 36 0,076923077 0 5 100 0,986666667 3,142857143 0,164179104 0 6 120 1,416666667 6 0,125 0 7 140 1,588235294 4,428571429 0,13030303 0 8 160 0,5 0 0,089552239 0 9 180 1,52173913 4,666666667 0,203007519 0 10 200 0,75 3,333333333 0,095890411 0 11 220 0,5 3 0,058823529 0 12 240 1,3 6,666666667 0,104347826 0 13 260 0,736842105 6,333333333 0,1375 0 14 280 0,857142857 2 0,096 0 15 300 1,75 2,666666667 0,090909091 0 16 340 0 0 0 0 17 370 0 0 0 0 18 400 0 0 0 0 19 430 0 0 0 0 20 460 0 0 0 0 21 490 0 0 0 0 22 510 0 0 0 0 23 530 1,3 4,5 0,5 0 24 550 1 0 0,123809524 0,00862069 25 580 1,411764706 0 0 0 26 610 1,823529412 0 0 0 27 640 0 0 0 0 28 670 0 0 0 0 29 700 0 0 0 0 30 730 0 0 0 0 31 760 0 0 0 0 32 780 1,311111111 1,25 0,08411215 0 33 805 1,384615385 5,2 0,144278607 0 34 840 1,243902439 13 0,14 0 35 860 0,934782609 3,5 0,079646018 0 36 865 0,986486486 3 0,04 0 37 885 0,970588235 5 0,046875 0 38 900 1,073170732 1,666666667 0,038888889 0 39 905 1,08 0 0,03125 0 40 935 1,12195122 9 0,076388889 0 41 945 1 0 0,037037037 0 42 965 1 5 0,071428571 0 43 985 1,111111111 2 0,085714286 0 44 1015 0,666666667 2,333333333 0,057692308 0 45 1035 0,875 1,727272727 0,056 0 46 1055 0,75 2,857142857 0,063781321 0 47 1075 3 3,5 0,02745098 0 48 1090 0,666666667 3 0,019607843 0 49 1110 0,733333333 4,2 0,069069069 0 50 1130 0,866666667 3,8 0,072463768 0 51 1160 1,375 3,25 0,088319088 0 52 1180 1,666666667 0 0,010638298 0 53 1200 0,909090909 2,5 0,031830239 0 54 1205 0,75 3,666666667 0,037542662 0 55 1230 1 0 0,014184397 0 56 1250 2,571428571 0 0,026086957 0 57 1270 1,055555556 0,333333333 0,045283019 0 58 1285 0,8 0,5 0,01 0 59 1300 5,5 1 0,03649635 0 60 1320 1,4 0,5 0,027027027 0 61 1340 1,384615385 1,333333333 0,027173913 0 62 1360 1,166666667 0,857142857 0,022222222 0 63 1380 2 1,333333333 0,039215686 0 64 1400 2 2 0,021052632 0 65 1420 0,666666667 2,75 0,035087719 0 66 1440 1 2 0,01 0 67 1460 0,5 0 0 0 68 1480 0 0 0 0 69 1500 0 0 0 0 70 1530 0 0 0 0 71 1550 0 0 0 0 72 1570 0 0 0 0 73 1590 0 0 0 0 74 1610 0 0 0 0 75 1630 0 0 0 0 76 1650 0 0 0 0 77 1670 0 0 0 0 78 1680 0 0 0 0 79 1700 0 0 0 0 80 1720 0 0 0 0 81 1740 0 0 0 0 82 1750 0 0 0 0 83 1810 0 0 0 0 84 1818 0 0 0 0 85 1870 0 0 0 0 86 1872 0 0 0 0 87 2230 0 0 0 0 - 2280 0 0 0 0 88 2290 0 0 0 0 89 2310 0 0 0 0 90 2330 0 0 0 0 91 2350 1,5 2 0,078947368 0 92 2370 1,8 0,555555556 0,113636364 0 93 2390 3,666666667 0,75 0,112903226 0 94 2410 0,75 0,5 0,333333333 0 95 2430 1,25 0 0,125 0,4 96 2450 1,157894737 7 0,166666667 0 97 2470 1,666666667 7 0,054794521 0 98 2498 0 0 0 0 99 2512 0 0 0 0 100 2521 0 0 0 0 101 2534 0 0 0 0 102 2556 0 0 0 0 103 2570 1,095238095 0 0,071428571 0 104 2590 0,818181818 1 0,072 0 105 2610 1,444444444 1,833333333 0,08627451 0 106 2630 0,75 6 0,113207547 0 107 2650 1,666666667 0 0 0 108 2670 0,125 1,666666667 0,45 0 109 2690 0,95 6,75 0,182572614 0 110 2715 0 0 0 0 111 2725 0 0 0 0 112 2735 0 0 0 0 113 2750 0 0 0 0 114 2770 0 0 0 0 115 2790 1 0 0,114285714 0 116 2815 0,857142857 11,33333333 0,2 0 117 2825 0 0 0 0 118 2840 0 0 0 0 119 2848 0 0 0 0 120 2856 0 0 0 0 121 2895 0 0 0 0 122 2910 0 0 0 0 123 2930 0 0 0 0 124 2950 0 0 0 0 125 2970 0 0 0 0 126 2990 0,578947368 4,5 0,565217391 0,029411765 127 3010 0,75 2,5 0,084337349 0 128 3030 0,333333333 1,666666667 0,109589041 0 129 3050 1,4 3,75 0,3 0 130 3070 1,545454545 0 0,035714286 0 131 3085 0 0 0 0 132 3115 0 0 0 0 133 3130 0 0 0 0 Chart 4 Data with the taphonomic indices (Right/Left valve ratio, Sex ratio, Adult/Juvenile ratio and Carapace/Disarticulated Valves ratio) of Cyprideis torosa of each sample of section M

Candona neglecta Sample Depth (cm) RV/LV ratio C/Vratio A/Jratio 1 20 0,833333333 0 0 2 40 0 0 0 3 60 0 0 0 4 80 4 0 0 5 100 1 0 0 6 120 2 0 0 7 140 0,5 0 0 8 160 0 0 0 9 180 0 0 0 10 200 0,6 0 0 11 220 1 0 0 12 240 0,75 0 0,076923077 13 260 1,666666667 0 0 14 280 3 0 0 15 300 0,166666667 0 0 16 340 0 0 0 17 370 0 0 0 18 400 0 0 0 19 430 0 0 0 20 460 0 0 0 21 490 0 0 0 22 510 0 0 0 23 530 0,4 0 0,058823529 24 550 4 0 0 25 580 0 0 0 26 610 0 0 0 27 640 0 0 0 28 670 0 0 0 29 700 0 0 0 30 730 0 0 0 31 760 0 0 0 32 780 1 0 0 33 805 2 0 0 34 840 0 0 0 35 860 0 0 0 36 865 0 0 0 37 885 0 0 0 38 900 0 0 0 39 905 1 0 0 40 935 0,428571429 0 0 41 945 0 0 0 42 965 2 0 0 43 985 3 0 0 44 1015 1,5 0 0 45 1035 1,25 0 0 46 1055 0,8 0 0 47 1075 0 0 0 48 1090 0 0 0 49 1110 0 0 0 50 1130 3 0 0,083333333 51 1160 0 0 0 52 1180 0 0 0 53 1200 2,333333333 0 0 54 1205 1 0 0 55 1230 0,5 0 0 56 1250 4 0 0 57 1270 1 0 0 58 1285 0 0 0 59 1300 0,75 0 0 60 1320 2 0 0 61 1340 1,5 0 0 62 1360 0 0 0 63 1380 0 0 0 64 1400 1,666666667 0 0 65 1420 1 0 0 66 1440 1 0 0 67 1460 0 0 0 68 1480 0 0 0 69 1500 0 0 0 70 1530 0 0 0 71 1550 0 0 0 72 1570 0 0 0 73 1590 0 0 0 74 1610 0 0 0 75 1630 0 0 0 76 1650 0 0 0 77 1670 0 0 0 78 1680 0 0 0 79 1700 0 0 0 80 1720 0 0 0 81 1740 0 0 0 82 1750 0 0 0 83 1810 0 0 0 84 1818 0 0 0 85 1870 0 0 0 86 1872 0 0 0 87 2230 0 0 0 - 2280 0 0 0 88 2290 0 0 0 89 2310 0 0 0 90 2330 0 0 0 91 2350 1,20754717 0,026143791 0,032894737 92 2370 1,285714286 0,064935065 0 93 2390 1,307692308 0 0 94 2410 0,727272727 0 0 95 2430 0,666666667 0 0 96 2450 1,053846154 0,006097561 0,012269939 97 2470 0 0 0 98 2498 0 0 0 99 2512 0 0 0 100 2521 0 0 0 101 2534 0 0 0 102 2556 0 0 0 103 2570 1,666666667 0,111111111 0 104 2590 2 0 0 105 2610 1,444444444 0 0 106 2630 1,25 0 0 107 2650 0,925925926 0 0 108 2670 1,222222222 0 0 109 2690 1,5 0 0 110 2715 0 0 0 111 2725 0 0 0 112 2735 0 0 0 113 2750 0 0 0 114 2770 0 0 0 115 2790 1 0 0 116 2815 1,4 0 0 117 2825 0 0 0 118 2840 0 0 0 119 2848 0 0 0 120 2856 0 0 0 121 2895 0 0 0 122 2910 0 0 0 123 2930 0 0 0 124 2950 0 0 0 125 2970 0 0 0 126 2990 1,013333333 0,026490066 0,040268456 127 3010 1,2 0 0,047619048 128 3030 1,1875 0 0,02173913 129 3050 1,15 0 0,02 130 3070 0,5 0,125 0 131 3085 0 0 0 132 3115 0 0 0 133 3130 0 0 0 Chart 5 Data with the taphonomic indices (Right/Left valve ratio, Sex ratio, Adult/Juvenile ratio and Carapace/Disarticulated Valves ratio) of Candona neglecta of each sample of section M

Depth (cm) Taxa_S Simpson_1-D Shannon_H Evenness_e^H/S Fisher_alpha 20 2 0,095 0,1985 0,6098 0,3542 40 2 0,0198 0,056 0,5288 0,3542 80 2 0,0392 0,09804 0,5515 0,3542 100 3 0,05803 0,1526 0,3883 0,5809 120 2 0,03959 0,09882 0,5519 0,355 140 2 0,0582 0,1347 0,5721 0,3542 160 1 0 0 1 0,1544 180 2 0,0198 0,056 0,5288 0,3542 200 2 0,0392 0,09804 0,5515 0,3542 220 4 0,1135 0,2769 0,3297 0,8321 240 2 0,09591 0,2 0,6107 0,355 260 2 0,0768 0,1679 0,5914 0,3542 280 2 0,05877 0,1358 0,5727 0,355 300 2 0,1472 0,2788 0,6608 0,3542 530 4 0,6606 1,144 0,7851 0,8342 550 2 0,095 0,1985 0,6098 0,3542 580 2 0,0392 0,09804 0,5515 0,3542 610 1 0 0 1 0,1544 780 2 0,0392 0,09804 0,5515 0,3542 805 2 0,0198 0,056 0,5288 0,3542 840 2 0,0198 0,056 0,5288 0,3542 860 2 0,095 0,1985 0,6098 0,3542 865 2 0,0198 0,056 0,5288 0,3542 885 2 0,0198 0,056 0,5288 0,3542 900 2 0,0198 0,056 0,5288 0,3542 905 2 0,0392 0,09804 0,5515 0,3542 935 2 0,095 0,1985 0,6098 0,3542 945 1 0 0 1 0,1544 965 2 0,0392 0,09804 0,5515 0,3542 985 2 0,0392 0,09804 0,5515 0,3542 1015 2 0,0392 0,09804 0,5515 0,3542 1035 2 0,0392 0,09804 0,5515 0,3542 1055 2 0,0392 0,09804 0,5515 0,3542 1075 2 0,0198 0,056 0,5288 0,3542 1090 2 0,0198 0,056 0,5288 0,3542 1110 2 0,0198 0,056 0,5288 0,3542 1130 2 0,0582 0,1347 0,5721 0,3542 1160 2 0,02 0,05647 0,529 0,355 1180 2 0,0198 0,056 0,5288 0,3542 1200 2 0,0582 0,1347 0,5721 0,3542 1205 2 0,0198 0,056 0,5288 0,3542 1230 2 0,0392 0,09804 0,5515 0,3542 1250 2 0,0392 0,09804 0,5515 0,3542 1270 2 0,0198 0,056 0,5288 0,3542 1285 2 0,0198 0,056 0,5288 0,3542 1300 3 0,0776 0,1957 0,4054 0,5823 1320 3 0,05803 0,1526 0,3883 0,5809 1340 3 0,0586 0,1538 0,3888 0,5823 1360 2 0,0198 0,056 0,5288 0,3542 1380 1 0 0 1 0,1544 1400 2 0,03959 0,09882 0,5519 0,355 1420 2 0,0392 0,09804 0,5515 0,3542 1440 2 0,0392 0,09804 0,5515 0,3542 1460 1 0 0 1 0,1544 2330 2 0,3432 0,5269 0,8468 0,3542 2350 3 0,4144 0,7288 0,6908 0,5837 2370 3 0,4866 0,7631 0,715 0,5823 2390 3 0,5538 0,8777 0,8018 0,5823 2410 3 0,3642 0,6645 0,6478 0,5823 2430 3 0,4154 0,7408 0,6992 0,5823 2450 3 0,4766 0,817 0,7546 0,5823 2470 2 0,0198 0,056 0,5288 0,3542 2570 4 0,3434 0,6953 0,5011 0,8342 2590 3 0,2152 0,421 0,5078 0,5823 2610 4 0,1834 0,389 0,3689 0,8342 2630 4 0,4408 0,8103 0,5621 0,8364 2650 3 0,5122 0,8213 0,7578 0,5837 2670 3 0,5186 0,7765 0,7246 0,5823 2690 3 0,1639 0,3316 0,4644 0,5809 2790 2 0,1958 0,3465 0,7071 0,3542 2815 2 0,2262 0,3864 0,7358 0,3542 2990 3 0,5877 0,9653 0,8752 0,5837 3010 4 0,4642 0,7341 0,5209 0,8364 3030 4 0,5245 0,8711 0,5974 0,8321 3050 4 0,511 0,8518 0,5859 0,8342 3070 3 0,4426 0,7624 0,7145 0,5823 Chart 6 D Data with the Diversity indices (Taxa_s, Simpson, Shannon and Evenness) of each sample of section M

Annex II

Sample Depth (cm) Cyprideis torosa Candona neglecta Loxoconcha elliptica Cytheridea neapolitana Leptocythere rara Aurila convexa Ammonia beccarii Ammonia tepida Haynesina depressula Elphidium advenum Elphidium crispum Quinqueloculina seminula total 1 10 80 0 0 0 0 0 0 0 0 0 0 0 80 2 30 230 0 8 0 19 0 20 20 0 0 0 0 297 3 50 128 0 0 0 0 0 0 0 0 0 0 0 128 4 70 103 0 0 0 26 0 0 0 0 0 0 0 129 5 90 85 0 0 0 7 0 0 1 0 0 0 0 93 6 110 182 0 0 0 6 0 4 0 0 0 0 0 192 7 130 302 0 0 0 2 0 27 0 0 0 0 0 331 8 150 116 0 0 0 2 0 300 0 0 0 0 0 418 9 170 100 0 0 0 0 0 250 0 0 0 0 0 350 10 190 120 0 0 0 0 0 250 10 0 0 0 0 380 11 210 100 0 0 0 0 0 250 4 0 0 0 0 354 12 230 5 0 44 0 0 0 98 75 0 0 0 0 222 13 250 0 0 65 0 0 0 100 43 0 0 0 0 208 14 270 0 0 163 11 0 0 58 72 6 6 6 0 322 15 290 1 0 66 12 0 0 30 39 110 2 2 0 262 16 310 0 0 41 93 0 0 15 31 120 2 2 0 304 17 330 0 0 3 20 0 0 15 45 200 2 2 0 287 18 350 80 0 7 22 0 0 11 2 200 4 4 0 330 19 370 40 0 2 0 0 1 137 55 58 1 1 0 295 20 390 0 0 125 6 0 0 50 31 55 3 3 0 273 21 410 0 0 141 0 0 0 37 50 37 4 4 0 273 22 430 11 0 140 95 0 0 14 7 25 0 0 6 298 23 450 3 0 5 48 0 0 150 2 95 0 0 0 303 24 470 25 0 16 13 0 0 200 10 25 0 0 0 289 25 490 3 0 7 3 0 0 200 20 60 2 3 0 298 26 510 0 0 13 15 0 0 82 20 150 15 2 0 297 27 530 63 0 11 24 0 0 80 20 150 10 0 0 358 28 550 10 0 27 1 0 0 100 15 130 5 0 0 288 29 570 50 0 0 0 0 0 200 50 0 0 0 0 300 30 590 129 0 0 0 0 0 165 30 0 0 0 0 324 31 610 13 0 0 0 0 0 8 0 0 0 0 0 21 32 630 50 0 0 0 0 0 245 15 2 0 0 0 312 33 660 2 0 149 135 0 0 130 50 120 10 3 23 622 34 690 82 0 1 2 0 0 150 80 20 0 0 2 337 35 710 42 0 0 0 0 0 120 50 15 2 0 0 229 36 730 48 0 32 0 0 0 150 30 5 0 0 0 265 37 750 4 0 89 0 2 0 100 25 45 5 0 0 270 38 770 0 0 18 0 0 0 7 0 0 0 0 0 25 39 790 0 0 63 0 0 0 30 5 10 1 0 0 109 40 810 13 0 0 0 0 0 150 15 25 0 0 0 203 41 830 11 0 2 0 0 0 160 30 30 3 0 0 236 42 850 23 0 0 0 0 0 200 50 70 2 1 0 346 43 870 20 0 0 0 0 0 200 45 40 2 1 0 308 44 890 21 0 2 0 0 1 200 15 15 2 0 0 256 45 910 38 0 3 0 0 0 200 15 15 2 0 273 46 930 60 0 1 0 0 0 200 45 40 2 1 349 47 950 36 0 1 0 0 0 200 50 70 2 1 0 360 48 970 1 0 230 0 0 0 40 30 25 15 0 0 341 49 990 4 0 72 0 0 0 21 0 0 1 0 0 98 50 1010 9 0 38 0 0 0 3 6 1 0 0 0 57 51 1030 1 0 124 11 2 0 20 15 15 0 0 0 188 52 1050 25 0 27 0 0 0 200 50 70 0 0 0 372 53 1070 20 0 0 0 0 0 200 50 70 0 0 0 340 54 1090 4 0 1 0 0 0 200 50 70 0 0 0 325 55 1110 0 0 34 0 0 0 90 25 45 0 0 0 194 56 1130 0 0 6 0 0 0 35 15 5 0 0 0 61 57 1150 0 0 2 0 0 0 5 0 0 0 0 0 7 58 1170 0 0 3 0 0 0 10 0 0 0 0 0 13 59 1190 0 0 0 0 0 0 50 12 15 5 0 0 82 60 1210 6 0 0 0 0 0 40 10 0 0 0 0 56 61 1230 61 0 0 0 0 0 20 6 0 0 0 0 87 62 1250 22 0 0 0 0 0 100 15 4 0 0 0 141 63 1270 47 0 0 0 0 0 0 0 0 0 0 0 47 64 1290 80 0 0 0 0 0 0 0 0 0 0 0 80 65 1310 100 0 0 0 0 0 0 0 0 0 0 0 100 66 1330 17 0 0 0 0 0 0 0 0 0 0 0 17 67 1350 62 0 0 0 0 0 0 0 0 0 0 0 62 68 1370 70 0 0 0 0 0 0 0 0 0 0 0 70 69 1390 63 0 0 0 0 0 0 0 0 0 0 0 63 70 1410 105 0 0 0 0 0 0 0 0 0 0 0 105 71 1430 93 0 0 0 0 0 0 0 0 0 0 0 93 72 1450 121 0 0 0 0 0 0 0 0 0 0 0 121 73 1470 280 0 0 0 0 0 0 0 0 0 0 0 280 74 1490 137 0 0 0 0 0 0 0 0 0 0 0 137 75 1510 166 0 0 0 0 0 0 0 0 0 0 0 166 76 1530 200 0 0 0 0 0 0 0 0 0 0 0 200 77 1550 81 0 0 0 0 0 0 0 0 0 0 0 81 78 1570 158 0 0 0 0 0 0 0 0 0 0 0 158 79 1590 120 0 0 0 0 0 0 0 0 0 0 0 120 80 1610 135 0 0 0 0 0 0 0 0 0 0 0 135 81 1630 55 0 0 0 0 0 0 0 0 0 0 0 55 82 1650 65 0 0 0 0 0 0 0 0 0 0 0 65 83 1670 28 0 0 0 0 0 0 0 0 0 0 0 28 84 1690 150 0 0 0 0 0 0 0 0 0 0 0 150 85 1710 93 0 0 0 0 0 1 0 0 0 0 0 94 86 1730 100 0 0 0 0 0 0 0 0 0 0 0 100 87 1750 100 0 0 0 0 0 0 0 0 0 0 0 100 - 1770 0 0 0 88 1790 70 0 0 0 0 0 0 0 0 0 0 0 70 89 1810 80 4 0 0 0 0 0 0 0 0 0 0 84 90 1830 20 0 0 0 0 0 0 0 0 0 0 0 20 91 1850 87 0 0 0 0 0 0 0 0 0 0 0 87 92 1870 35 0 0 0 0 0 1 0 0 0 0 0 36 93 1890 70 0 0 0 0 0 0 0 0 0 0 0 70 94 1910 100 0 0 0 0 0 0 0 0 0 0 0 100 95 1930 80 3 0 0 0 0 0 0 1 0 0 0 84 96 1950 100 7 0 0 0 1 0 0 0 0 0 0 108 97 1970 90 5 0 0 0 0 0 0 0 0 0 0 95 98 1990 77 2 0 0 0 0 0 0 0 0 0 0 79 99 2010 100 0 0 0 0 0 0 0 0 0 0 0 100 100 2030 65 1 0 0 0 0 0 0 0 0 0 0 66 101 2050 55 0 0 0 0 0 0 0 0 0 0 0 55 102 2070 19 0 0 0 0 0 0 0 0 0 0 0 19 103 2090 24 0 0 0 0 0 0 0 0 0 0 0 24 104 2110 34 0 0 0 0 0 0 0 0 0 0 0 34 105 2130 26 1 0 0 0 0 0 0 0 0 0 0 27 106 2150 50 0 0 0 0 0 0 0 0 0 0 0 50 107 2170 70 2 0 0 0 0 0 0 0 0 0 0 72 108 2190 130 6 0 0 0 0 0 0 0 0 0 0 136 109 2210 120 2 0 0 0 0 0 0 0 0 0 0 122 110 2230 180 2 0 0 0 0 0 0 0 0 0 0 182 111 2250 200 0 0 0 0 0 0 0 0 0 0 0 200 112 2270 180 3 0 0 0 0 0 0 0 0 0 0 183 113 2290 100 2 0 0 0 0 0 0 0 0 0 0 102 114 2310 50 0 0 0 0 0 0 0 0 0 0 0 50 115 2330 40 0 0 0 0 0 0 0 0 0 0 0 40 116 2350 50 0 0 0 0 0 0 0 0 0 0 0 50 117 2370 38 0 0 0 0 0 0 0 0 0 0 0 38 118 2390 0 0 0 0 0 0 0 0 0 0 0 0 0 119 2410 30 0 0 0 0 0 0 0 0 0 0 0 30 120 2430 35 0 0 0 0 0 0 0 0 0 0 0 35 121 2450 50 0 0 0 0 0 0 0 0 0 0 0 50 122 2470 50 0 0 0 0 0 0 0 0 0 0 0 50 123 2490 0 0 0 0 0 0 0 0 0 0 0 0 0 124 2510 60 0 0 0 0 0 0 0 0 0 0 0 60 125 2530 0 0 0 0 0 0 0 0 0 0 0 0 0 126 2550 17 0 0 0 0 0 0 0 0 0 0 0 17 127 2570 15 0 0 0 0 0 0 0 0 0 0 0 15 128 2590 15 0 0 0 0 0 0 0 0 0 0 0 15 129 2610 0 0 0 0 0 0 0 0 0 0 0 0 0 130 2630 0 0 0 0 0 0 0 0 0 0 0 0 0 131 2650 0 0 0 0 0 0 0 0 0 0 0 0 0 132 2670 15 0 0 0 0 0 0 0 0 0 0 0 15 133 2690 25 0 0 0 0 0 0 0 0 0 0 0 25 134 2710 0 0 0 0 0 0 0 0 0 0 0 0 0 Chart 7 Data with the valves of each species of each sample and the total number of valves of section K

Depth (cm) Taxa_S Simpson_1-D Shannon_H Evenness_e^H/S 10 1 0 0 1 30 5 0,3928 0,8475 0,4668 50 1 0 0 1 70 2 0,32 0,5004 0,8247 90 3 0,1654 0,3339 0,4655 110 3 0,0962 0,2322 0,4204 130 3 0,1654 0,3339 0,4655 150 2 0,4032 0,593 0,9047 170 2 0,4118 0,6022 0,913 190 3 0,4717 0,7466 0,7033 210 3 0,4174 0,6457 0,6357 230 4 0,6504 1,128 0,7725 250 3 0,6294 1,043 0,946 270 7 0,657 1,325 0,5375 290 7 0,7238 1,48 0,6277 310 7 0,7222 1,468 0,6199 330 7 0,487 1,017 0,3949 350 8 0,5638 1,152 0,3955 370 5 0,6926 1,316 0,7456 390 7 0,6973 1,405 0,5822 410 6 0,6578 1,291 0,6063 430 7 0,6654 1,357 0,5547 450 6 0,635 1,172 0,5378 470 6 0,5016 1,092 0,4968 490 8 0,5054 1,039 0,3532 510 7 0,6568 1,357 0,5548 530 7 0,7378 1,566 0,6838 550 6 0,6563 1,28 0,5992 570 3 0,5033 0,8721 0,7973 590 3 0,5718 0,9266 0,842 630 4 0,3606 0,6785 0,4927 660 7 0,8054 1,728 0,8042 690 6 0,6848 1,302 0,6129 710 5 0,6438 1,214 0,6734 730 5 0,6158 1,205 0,667 750 6 0,7109 1,38 0,6624 790 5 0,5829 1,084 0,5914 810 4 0,4179 0,8306 0,5736 830 6 0,5109 1,034 0,4689 850 5 0,599 1,145 0,6287 870 5 0,5344 1,045 0,5685 890 6 0,3778 0,8256 0,3805 910 6 0,431 0,8957 0,4082 930 5 0,6093 1,178 0,6493 950 5 0,6206 1,192 0,6586 970 5 0,5124 1,055 0,5744 990 4 0,4096 0,7296 0,5186 1010 5 0,5201 1,032 0,5614 1030 7 0,5448 1,18 0,4651 1050 5 0,6456 1,286 0,7235 1070 4 0,5899 1,092 0,7447 1090 4 0,5446 0,9601 0,653 1110 4 0,6862 1,269 0,8894 1130 4 0,5962 1,099 0,7505 1190 4 0,5694 1,064 0,7242 1210 3 0,4514 0,7946 0,7379 1230 3 0,4522 0,7738 0,7227 1250 4 0,468 0,8856 0,6061 1270 1 0 0 1 1290 1 0 0 1 1310 1 0 0 1 1350 1 0 0 1 1370 1 0 0 1 1390 1 0 0 1 1410 1 0 0 1 1430 1 0 0 1 1450 1 0 0 1 1470 1 0 0 1 1490 1 0 0 1 1510 1 0 0 1 1530 1 0 0 1 1550 1 0 0 1 1570 1 0 0 1 1590 1 0 0 1 1610 1 0 0 1 1630 1 0 0 1 1650 1 0 0 1 1690 1 0 0 1 1710 2 0,0198 0,056 0,5288 1730 1 0 0 1 1750 1 0 0 1 1790 1 0 0 1 1810 2 0,095 0,1985 0,6098 1850 1 0 0 1 1870 2 0,0582 0,1347 0,5721 1890 1 0 0 1 1910 1 0 0 1 1930 3 0,0958 0,2235 0,4168 1950 3 0,1314 0,2823 0,4421 1970 2 0,095 0,1985 0,6098 1990 2 0,0582 0,1347 0,5721 2010 1 0 0 1 2030 2 0,0392 0,09804 0,5515 2050 1 0 0 1 2150 1 0 0 1 2170 2 0,0582 0,1347 0,5721 2190 2 0,0768 0,1679 0,5914 2210 2 0,0392 0,09804 0,5515 2230 2 0,0198 0,056 0,5288 2250 1 0 0 1 2270 2 0,0392 0,09804 0,5515 2290 2 0,0392 0,09804 0,5515 2310 1 0 0 1 2330 1 0 0 1 2350 1 0 0 1 2370 1 0 0 1 2410 1 0 0 1 2430 1 0 0 1 2450 1 0 0 1 2470 1 0 0 1 2510 1 0 0 1 Chart 8 Data with the Diversity indices (Taxa_s, Simpson, Shannon and Evenness) of each sample of section K