Paleoenvironmental evolution based on benthic foraminifera biofacies of the Paraíba do Sul Deltaic Complex, eastern Brazil

Accepted Manuscript Paleoenvironmental evolution based on benthic foraminifera biofacies of the Paraíba do Sul Deltaic Complex, eastern Brazil Sarah Pereira Gasparini, Claudia Gutterres Vilela PII:

S0895-9811(17)30125-6

DOI:

10.1016/j.jsames.2017.09.026

Reference:

SAMES 1791

To appear in:

Journal of South American Earth Sciences

Received Date: 3 April 2017 Revised Date:

21 September 2017

Accepted Date: 21 September 2017

Please cite this article as: Gasparini, S.P., Vilela, C.G., Paleoenvironmental evolution based on benthic foraminifera biofacies of the Paraíba do Sul Deltaic Complex, eastern Brazil, Journal of South American Earth Sciences (2017), doi: 10.1016/j.jsames.2017.09.026. This is a PDF file of an unedited manuscript that has been accepted for publication. As a service to our customers we are providing this early version of the manuscript. The manuscript will undergo copyediting, typesetting, and review of the resulting proof before it is published in its final form. Please note that during the production process errors may be discovered which could affect the content, and all legal disclaimers that apply to the journal pertain.

ACCEPTED MANUSCRIPT Paleoenvironmental evolution based on benthic foraminifera biofacies of the Paraíba do Sul Deltaic Complex, eastern Brazil Sarah Pereira Gasparinia,*; Claudia Gutterres Vilelaa a

Universidade Federal do Rio de Janeiro, Instituto de Geociências/Departamento de Geologia, MicroCentro - Laboratório de Análise Micropaleontológica. Av. Athos das Silveira Ramos, 274, Cidade Universitária, Ilha do Fundão, 21.941-916, Rio de Janeiro, Brasil.

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*Corresponding author. E-mail addresses: [email protected] (S.P. Gasparini), [email protected] (C.G. Vilela).

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Abstract

The paleoecology and distribution of benthic foraminiferal assemblages were analyzed

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in the core 2-MU-1-RJ well, drilled in the Paraíba do Sul Deltaic Complex, Rio de Janeiro (Brazil). An abundant assemblage was found in the upper portion of the well core, inferred to be pleistocenic deposits. The coastal dynamic was recognized from five biofacies based on clusters, the Planktonic/Benthic (P/B) ratios and indicator species

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distribution in the core. Several biofacies were identified along the core depending on the species dominance. From the bottom to the top of the core, the biofacies succession represents the environmental changes in the coastal area associated to sea-level

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oscillations. The biofacies ABP dominated by Ammonia parkinsoniana and Bolivina spp. and Pararotalia cananeiaensis represents an inner shelf environment; biofacies QP

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dominated by shelf miliolids species; biofacies PGH, dominated by P. cananeiaensis, Gavelinopsis praegeri, and Hanzawaia nitidula, represents the estuary complex with middle or outer shelf influence; biofacies QL represents hypersaline waters dominated by lagoonal miliolids; and biofacies HP characterized by Haynesina germanica and P. cananeiaensis is associated with paralic environments. Marine ingressions are recorded and those biofacies show the pleistocenic coastal hydrodinamic in the deltaic complex. The foraminiferal biofacies contribute with detailed information to sedimentary facies

ACCEPTED MANUSCRIPT previously characterized in the study area by the reconstruction of paleoenvironment succession. Keywords: benthic foraminifera, coastal hydrodynamic, biofacies, paleoecology,

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indicator species.

1 Introduction

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The Paraíba do Sul Deltaic Complex is an expressive depositional feature in the Brazilian coast. For this reason, many authors studied its sedimentological

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characteristics, coastal morphology, and evolution of the delta, but most of these old studies were only with superficial samples and none of them considers paleontological tools to make the paleoenvironmental models (e.g. Bacoccoli, 1971; Dominguez et al., 1983; Martin et al., 1993, 1984).

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Benthic foraminifera are an excellent microfossil to paleoenvironmental reconstructions because they are wide spatial-temporal spread and good environmental indicators used

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in the determination of variables, such as oxygen, organic matter, salinity, among others (Boltovskoy et al., 1991; Jorissen et al., 2007; Martins and Gomes, 2004; Murray, 2006,

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2001; Silva and Duleba, 2013). The potential preservation of their tests in the geological record and a significant density of them in a small volume of sediment make these microfossils a useful tool for paleoenvironmental reconstructions (Boltovskoy and Wright, 1976; BouDagher-Fadel, 2008; Scott et al., 2004; Sen Gupta, 2003). Recently, Laut et al. (2016, 2011) studied foraminifera in superficial samples of the Paraíba do Sul delta associating them to sedimentological, microbiological and carbon analysis. This work goes further in the study of the paleoenvironmental evolution of the Paraíba do Sul Deltaic Complex. It aims to identify benthic foraminifera biofacies through

ACCEPTED MANUSCRIPT subsurface samples to reconstruct the paleoenvironmental history, correlate and compare the acquired data with sedimentary facies data to contribute to the comprehension of the study area.

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2 Study area

The Paraíba do Sul Deltaic Complex is located on the northern coast of the Rio de Janeiro state, Brazil (Figure 1), with an area of 3000 km2 of coastal plain (Martin et al.,

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1984). It is situated on the onshore portion of Campos Basin. This basin had its origin

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with the breakup of Gondwana supercontinent and its sedimentary infill can be separated in three depositional supersequences, according to Winter et al. (2007): continental rift (Neocomian to Eoaptian), transitional post-rift with evaporates and shallow marine sequence (Aptian to Early Albian) and marine drift (Albian to Recent).

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The deltaic complex is classified as wave-dominated (Bacoccolli, 1971), and its evolution was controlled by the interplay between fluvial and marine processes, the relative changes in the sea level and neotectonics during the Quaternary (Silva, 1987).

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The following geological unit and Quaternary deposits compose the deltaic plain (Figure 1): Barreiras Formation (Plateau), alluvial plain, fluvial-lagoon plains, coastal

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plains and others minor deposits, as mangrove and peat (CPRM, 2001; Dillenburg and Hesp, 2009; Martin et al., 1997, 1984). The coastal tablelands, known as Barreiras Formation (Pliocene), correspond to sandy clay deposits of continental sedimentation in semi-arid conditions, with a lower sea level position than the present. Channel deposits, crevasse splays, floodplains and levee deposits at the area of the low downhill characterize the Quaternary alluvial plain. Quaternary fluvial-lagoon deposits represent a wide superficial sedimentation of muddy sand, with biodetritic sand and organic mud rich in shells. In the study area, Feia Lagoon stands out. The coastal plains are

ACCEPTED MANUSCRIPT represented by beach ridge systems and they are characterized by the gently undulating landscape. There are two systems in the area and each one comprises a phase of development of the deltaic complex. A pleistocenic one, located in the south of the deltaic complex, is related to an older orientation of Paraíba do Sul River. And the

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holocenic and active one is developed along the current orientation of the river, located in the north of the area. These deposits are represented by quartzose medium sand and they are sedimentary features of a wave-dominated delta. From satellite images, several

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system and paleo-channels directed São Tomé Cape.

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sets, based on unconformities that indicate phases of erosion, in those beach ridge

Figure 1 – Geomorphological map of the Paraíba do Sul Deltaic Complex, showing the location of the 2-MU-1-RJ well (modified from Rodrigues et al., 2015).

ACCEPTED MANUSCRIPT Martin et al. (1993) proposed the evolution of the coastal plain of the Brazil, between Macaé (RJ) and Maceió (AL). After that, Martin et al. (1997) detailed the holocenic evolution of the Paraíba do Sul River based on the geological mapping. Those two models together suggest eight stages of evolution. The first stage represents the

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sedimentation of Barreiras Formation, probably under the influence of a semi-arid climate with sporadic rains in the Pliocene, when the sea level was lower than the current one. The sedimentation of this group occupied the coastal plains. In the second

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stage, the climate became more humid, interrupting the sedimentation of the Barreiras Formation. The sea level rose and eroded the outer portion of this formation, forming

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the cliffs, in the Pleistocene. At this stage, the preservation of these cliffs is found in the states of northeast Brazil. The third stage corresponds to a regressive phase and the climate became again semi-arid, forming new continental deposits, composed of alluvial coalescent fans at the base of the cliffs. The fourth stage represents the total or partial

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erosion of the deposits of the previous stage due to the maximum of the penultimate transgression (123,000 years BP). Also, the river valley was flooded, giving place to estuaries and lagoons. The fifth stage comprises the construction of Pleistocene terraces

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formed by prograding beach ridges due to regression of the sea. In the sixth stage, the Pleistocene coastal plains were submerged by the last sea transgression (5,100 years

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BP). Then there was the development of barriers and the installation of lagoons of considerable size, isolated from the open sea by those barriers. Radiocarbon dating shows that those barriers have existed before the peak of the latter transgression. The seventh stage comprises the infilling of paleo-lagoons by deltaic deposition through distributary channels of Paraíba do Sul River arranged according to the bird-foot pattern. There was a distributary channel which reached the ocean in the current position. Over time, some of the lagoons in the area became freshwater lakes, and then

ACCEPTED MANUSCRIPT peat swamps were developed with complete infilling of them. The eighth stage represents the regressive phase, with the formation of Holocene marine terraces from the original barriers. Some lagoons have evolved into lakes or ponds. There were many erosion and construction phases due to the hydrodynamic conditions and the sea-level

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changes. 3 Materials and methods

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The 2-MU-1-RJ well core was drilled in the coastal plain of the Paraíba do Sul River, in Mussurepe district, Rio de Janeiro (Brazil), at 21º55’17.01” S and 41º08’24.02” W

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(WGS 84)(Figure 1). The well comprises 200 m of sediments and sedimentary rocks, poorly recovered (43%) due to the friable nature of the material. The well was drilled using a rotary drilling, model MACH 700, in 2004, as part of a project by LAGESED Laboratory, UFRJ.

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A total of 58 sediment samples were selected for foraminiferal analysis based on facies interpretation of the core, according to Plantz (2014). They were collected from the top of the core 2-MU-1-RJ well (1.85 – 64.35 m) at intervals of 60 or 120 cm in the marine

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influenced facies. Sampling occurred in aliquots of 2 centimeters per sample with about total 20 g before the treatment methods. From each sample, it was separated a quote of

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10 g of sediments, washed through a 500 and 63-µm-mesh sieves and dried. When necessary the samples were splitted to provide specimen counts of ~300, according to Boltovskoy and Wright (1976), and analyzed using a Zeiss STEMI 2000-C stereomicroscope. For further analysis, the planktonic foraminifera was also counted and biotic components were identified, such as ascidia spicules, echinoderm spines, and scaphopods. Benthic foraminifera was classified using taxonomic references such as those of Boltovskoy et al. (1980), Cushman (1939), Ellis and Messina (1940 et seq.), Loeblich Jr. and Tappan (1987), WoRMS (2017) and other specific taxonomic works.

ACCEPTED MANUSCRIPT Then, the photomicrographs were taken on the Zeiss Discovery V12 stereomicroscope coupled to the AxioCam camera and the AxioPlus system, at the MicroCentro Laboratory, UFRJ. The absolute and relative abundances, species dominance (relative abundance > 10%

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per sample, according to Boltovskoy and Totah, 1985), richness (S’) and planktonic/benthic ratio were calculated for each sample. The Shannon diversity index (H’) (Shannon, 1948) estimates the specific diversity of each sample by evaluating the

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number of species and the individual distribution between them (Sen Gupta and

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Kilbourne, 1974). The equitability (J’) is the ratio between diversity Shannon-index and maximum richness. It determines whether species have a homogeneous distribution in the samples (Clarke and Warwick, 1994; Pielou, 1969). The Shannon diversity and equitability were used for samples with more than 100 individuals (Fatela and Taborda, 2002). They were calculated using Paleontological Statistics program (PAST), Version

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2.17c (Hammer et al., 2013). The relative abundance was used to generate cluster analysis (Q-mode), with PC-ORD, Version 6 (McCune and Mefford, 2011).

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4 Results

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4.1 Sedimentary facies and age dating of the well core The sediments of the samples were siliciclastic, hybrid (siliciclastic with carbonate) and carbonate deposits (Figure 2). In the siliciclastic sediments, it can be observed intense pedogenetic processes as clay illuviation, plants bioturbation, feldspar dissolution and oxide/hydroxide precipitation (Plantz, 2014; Rodrigues et al., 2015). Plantz (2014) identified 16 sedimentary facies based on the lithological profile. These facies were clustered in five successions representing different sedimentation stages. Three samples were standardized by radiocarbon dating: 13.20 m (shells), 37.70 m (shells) and 59.00

ACCEPTED MANUSCRIPT m (organic matter), but all of them showed ages older than 40,000 years BP (Plantz,

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2014).

Figure 2 – Schematic descriptions of the deposits in the 2-MU-1-RJ well core. The portion studied is in the marine and in the nonmarine in the top of the well, from 64.35 m to 1.85 m (modified from Rodrigues et al., 2015). 4.2 Species richness, Shannon diversity and Equitability In most of the studied section, the richness presented values greater than 30 species; the diversity, values above 2; and equitability, above 0.5. Eleven samples do not present the minimum number (100) of specimens for the confident calculation of the indexes. The

ACCEPTED MANUSCRIPT three indexes have a maximum value in the sample 58.8 m and a minimum value in 9 m richness

and

diversity,

and

in

14.9

m

for

equitability

(Figure

3).

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for

Figure 3 – Richness (S), Shannon diversity (H’) and Equitability (J’) in core 2-MU-1-RJ

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well.

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4.3 Composition and abundance of the foraminifera A total of 297 species were identified, representing 79 genera (Table A). The calcareous hyaline species were the prevalent group (262 species), followed by the porcelanous (30 species) and agglutinated forms (five species). In the analyzed samples, seven samples were barren for benthic foraminifera, five in the base of the studied portion, respectively at 64.35 m, 63.55 m, 63.15 m, 62.55 m and 61.95 m. The first occurrence of benthic foraminifera was at the depth of 61.35 m, with

ACCEPTED MANUSCRIPT the presence of five tests. At the top of the core, two barren samples occur at 9.35 m and 1.85 m. At 9 m sample interval occurred a total of 45 tests. There are four intervals with high absolute abundance of tests in the core. The first occurs between 52.5 and 47.25 m, with a maximum of 60,023 specimens at the depth of

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48.6 m. The second interval occurs between 41 and 32.6 m of depth, with a maximum of 90,368 specimens at 32.6 m. In the third interval, two isolated peak occurs at 25.4 m with 40,576 specimens and at 21.8 m with 20,736 specimens, respectively. The fourth

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interval occurs between 16.05 m and 13.7 m, with 38.784 specimens at 16.05 and

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38.144 at 13.8 m.

The following species are dominant (> 10%): Ammonia parkinsoniana, Bolivina spp., Cassidulina

reniforme,

Hanzawaia

nitidula,

Cibicidoides

pseudoungeriana,

Haynesina

germanica,

Gavelinopsis

Pararotalia

praegeri,

cananeiaensis,

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Quinqueloculina lamarckiana, Quinqueloculina vulgaris, Quinqueloculina spp. and Sahulia conica. The species P. cananeiaensis was dominant in 27 samples and G. praegeri, in 22 samples (Plate I and II; Appendix A; Table B).

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Although some species do not present statistically significance, they were included in the discussion as indicator species, such as: Angulogerina spp., Buliminella

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elegantissima, Cancris sagra, Elphidium spp., Eponides repandus, Fissurina spp., Fursenkoina pontoni, Globocassidulina subglobosa, Haynesina depressula, Hopkinsina pacifica, Islandiella spp., Lagena spp., Miliolinella subrotunda, Neoconorbina spp., Pyrgo spp., Rosalina williamsoni, Rosalina spp., Trifarina bradyi, Triloculina spp. and Uvigerina spp. (Plate I and II; Appendix A; Table B).

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Plate I – Benthic foraminifera species found in the 2-MU-1-RJ well core. 1-2: Quinqueloculina lamarckiana, general view, sample 37,4 m; 3: Bolivina ordinaria, lateral view, sample 41 m; 4: Bolivina pseudoplicata, lateral view, sample 57,6m; 5: Bolivina spathulata, lateral view, sample 23 m; 6: Bolivina variabilis, lateral view, sample 33,7 m; 7: Bolivina striatula, lateral view, sample 28,9 m; 8: Globocassidulina crassa, general view, sample 39,8 m; 9: Globocassidulina minuta, general view, sample 58,2 m; 10-11: Cassidulina reniforme, general view, sample 39,8 m; 12: Buliminella elegantissima, lateral view, sample 21,8 m; 13 Trifarina angulosa, lateral view, sample 41 m; 14: Angulogerina cojimarensis, lateral view, sample 41 m; 15-16: Cancris sagra, 15: spiral view, 16: apertural view, sample 58,8 m; 17-18: Rosalina williamsoni, 17: spiral view, 18: apertural view, sample 35 m; 19-20: Gavelinopsis praegeri, 19: spiral view, 20: apertural view, sample 29,5 m; 21-22: Neoconorbina parkerae, 21: spiral view, 22: apertural view, sample 18,2 m. Scale: 50 µm.

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Plate II – Benthic foraminifera species found in the 2-MU-1-RJ well core. 1-2: Rosalina floridana, 1: spiral view, 2: apertural view, sample 23 m; 3-4: Rosalina globularis, 3: spiral view, 4: apertural view, sample 35 m; 5-6: Cibicidoides pseudoungeriana, 5: spiral view, 6: apertural view, sample 37,4 m; 7-8: Mullinoides differens, 7: spiral view, 8: apertural view, sample 23 m; 9: Haynesina germanica, lateral view, sample 52,5 m; 10: Haynesina depressula, lateral view, sample 37,4 m; 11: Haynesina depressula var. matgordanum, lateral view, sample 24,2 m; 12: Cribroelphidium incertum, lateral view, sample 35 m; 13-14: Hanzawaia nitidula, 13: spiral view, 14: apertural view, sample 41 m; 15-16: Pararotalia cananeiaensis, 15: spiral view, 16: umbilical view, sample 57,6 m; 17-18: Ammonia parkinsoniana, 17: spiral view, 18: umbilical view, sample 54,6 m. Scale: 50 µm.

ACCEPTED MANUSCRIPT Taphonomically, some foraminiferal tests were in general abraded and broken (Figure 4 A). The majority of the tests presented yellowish color at 59.2 m, 58.8 m and 58.2 m intervals.

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4.4 Planktonic/Benthic ratio (P/B ratio) The P/B ratio is low at the bottom of the studied section, with some peaks of small amplitude, less than 10%. It increases at the core of 41 m, reaching its maximum at 28.9

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m (25%), and decreasing at 20.6 m with a peak at 12.5 m (Figure 4 B).

Figure 4 – Total picked tests and taphonomy (A) and Planktonic/Benthic ratio (B) in core 2-MU-1-RJ well.

ACCEPTED MANUSCRIPT 4.5 Cluster Analyses Five groups of samples were generated by cluster analysis, Q mode, using a similarity

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level of ~ 62% (Figure 5):

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Figure 5 – Dendrogram resulting from the cluster analysis of the samples with dominant species.

- Group A: Sample intervals 9 m; 13.7 m; 17.2 m; 46.2 m; 46.8 m; 47.25 m; 48 m; 48.6 m; 49.2 m; 50 m; 51 m; 51.6 m; 52.25 m; 52.5 m; 54.6 m; 55.2 m; 55.8 m and 57 m.

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The dominant species are Pararotalia cananeiaensis, Gavelinopsis praegeri, and Ammonia parkinsoniana. Those hyaline species are typical of near-coastal and/or inner

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shelf environment (Debenay et al., 2001b; Martins and Gomes, 2004; Murray, 2006) - Group B: Sample intervals 14.9 m and 16.05 m, with two hyaline species: P. cananeiaensis and Haynesina germanica, of the shelf or coastal environment, tolerant to high salinity, present in sediments with great variability of mud and TOC (Debenay et al., 2001b, 2006; Murray, 2006).

ACCEPTED MANUSCRIPT - Group C: Sample intervals 18.2 m; 19.4 m and 54 m, with dominance of Quinqueloculina spp. Porcelaneous genera are proxies of hypersaline environments in coastal areas (Debenay et al., 2001a; Martins and Gomes, 2004; Murray, 2006). - Group D: Sample intervals 21.8 m; 23 m; 24.2 m; 25.4 m; 27.7 m; 28.9 m; 29.5 m;

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30.15 m; 32.6 m; 33.7 m; 35 m; 36.2 m; 37.4 m; 38.6 m; 39.8 m and 41 m, assemblage of shelf hyaline tests and one agglutinated test: Cassidulina reniforme, Cibicidoides pseudoungeriana, Gavelinopsis praegeri, Globocassidulina crassa, Hanzawaia

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nitidula, Mullinoides differens, Rosalina floridana, R. globularis, R. williamsoni and

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Sahulia conica (Martins and Gomes, 2004; Murray, 2006).

- Group E: Sample intervals 57.6 m; 58.2 m; 58.8 m; 59.2 m and 60 m, the dominant species Bolivina spp. followed by A. parkinsoniana and P. cananeiaensis. These hyaline specimens represent coastal/shelf environments, suggesting a low oxygen level

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(Boltovskoy et al., 1991; Debenay et al., 2001b; Jorissen et al., 2007; Martins and Gomes 2004; Murray, 2006, 2001).

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5 Discussion

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5.1 Sedimentary facies’ paleoenvironment and age dating of the core The paleoenvironment succession identified by Plantz (2014) was tidal flat, marine, lagoonal and fluvial environment, along the study section, from the bottom to top, according to sedimentary facies. The age of the dated material by radiocarbon is not reliable, so the sedimentary column is inferred as Pleistocene down to approximately 63.15 m based on coccolithophorids (Motta, 2016). It is associated with the transgression of ~120,000 years BP, and to Paleogene/Neogene till 200 m because of

ACCEPTED MANUSCRIPT the lithologic similarity to Emborê/Barreiras Formation (Rodrigues et al., 2015). In this work, all studied samples are placed in the Pleistocene.

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5.2 Preservation of fossil benthic foraminifera The tests deposited from 61.4 to 46.2 m and from 41 to 9 m depth intervals were probably reworked due to some of them are abraded and broken (Martin et al., 1995).

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Almost all tests presented yellowish color in the samples 59.20 m; 58.80 m and 58.20 m, and some of them are abraded and broken suggesting reworking of the tests in the

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past. According to Leão and Machado (1989), the yellowish tests indicate a period of slow sedimentation rate accompanied by exposure of the tests in the oxidizing zone. From 54 to 46.2 m, the assemblage has abraded tests and, they possible get into a

5.3 Biofacies

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diagenetic process.

species.

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Five biofacies were defined using the clusters, dominance species (>10%) and indicator

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5.3.1 Biofacies ABP (Ammonia parkinsoniana, Bolivina spp. and Pararotalia cananeiaensis biofacies) This biofacies represents the beginning of the marine influence and establishment of an inner shelf. It is present at the intervals from 60.0 m to 55.2 m with high richness, diversity and equitability. A. parkinsoniana and Elphidium spp. are opportunistic and infaunal species, typical of a dysaerobic environment with sandy and muddy sediments. The assemblage Ammonia-Elphidium is used to indicate brackish waters in the paralic

ACCEPTED MANUSCRIPT environment (Bastos et al., 2010; Hart and Kaesler, 1986). Based on the presence of this association, Silva et al. (2014) inferred a lagoonal environment on SE São Paulo coast, with polyhaline/mesohaline stratified waters, proximal marine contribution and low oxygen sediments. Laut et al. (2011) found the assemblage Amomnia tepida-Elphidium

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gunteri at the lower delta in the area of the current Paraíba do Sul River mouth. According to Murray (2006), the Elphidium can be found on the inner shelf and in brackish to hypersaline waters, as in marshes and mangroves. In Brazil, Ammonia-

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Elphidium were recorded mainly in coastal environments such as bays, estuaries, and lagoons (Brönnimann et al., 1981; Laut et al., 2011; Machado and Araújo, 2014; Vilela

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et al., 2014). The abundance of A. parkinsoniana is 37% at 60 m and Elphidium spp. was 2%.

Bolivina spp. (B. compacta, B. ordinaria, B. pseudoplicata, B. spathulata, B. striatula, B. variabilis) are marine shelf and presents abundance of 14%, reaching 30% at 58.8 m.

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This marine genus is associated with the Minimum Oxygen Zone and represents habitats with a high supply of organic matter and oxygen deficiency in shallow depths. Its morphotype is adapted to suboxide environments (Boltovskoy et al., 1991; Jorissen

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1993).

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et al., 2007; Martins and Gomes 2004; Murray, 2006; Sen Gupta and Machain-Castillo,

Pararotalia cananeiaensis appears at 59.2 m and it is dominant until 55.2 m, with abundance above of 12%. It is a marine species, present in the shelf at shallow depths, although it also indicates marine influence in coastal environments (Debenay et al., 2001b; Duleba et al., 2003). The occurrence of associated marine species at the biofacies’ deeper intervals, such as Angulogerina spp., Cancris sagrum, Cassidulina spp., Cibicidoides pseudoungeriana, Fissurina spp., Globocassidulina subglobosa, Islandiella spp., Lagena spp., Rosalina

ACCEPTED MANUSCRIPT williamsoni, Rosalina spp. and Uvigerina spp. and the paralic Haynesina germanica suggested high marine influence in the the open coast. From 59.2 m to 57.6 m, several species of Bolivina and other infaunal species such as Buliminella elegantissima, Fursenkoina pontoni, and Hopkinsina pacifica can represent

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high values of organic matter with low values of oxygen. An increase in the abundance of P. cananeiaensis at the top intervals (57 m to 55.2 m) in this biofacies confirmed the

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5.3.2 Biofacies QP (shelf miliolids biofacies)

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marine influence in coastal areas or inner shelf.

This biofacies is dominated by several species of Quinqueloculina such as Q. angulata, Q. bosciana, Q. candeiana, Q. delicatula, Q. frigida, Q. laevigata, Q. lamarckiana, Q. paralela, Q. poeyana, Q. seminula, Q. schlumbergeri and Q. vulgaris. It is present from

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54.6 m to 54 m and from 24.2 m to 19.4 m and the abundance of Quinqueloculina spp. is above 10%, reaching 33% at 54 m. This biofacies is characterized by high values of richness, diversity, and equitability, and can enable a shelf environment with normal to

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high levels of salinity (Murray, 2006; Vieira et al., 2014). Associated species in this biofacies are Bolivina spp., Cassidulina spp., Miliolinella subrotunda, Pararotalia

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cananeiaensis, Pyrgo spp., Rosalina spp. and Triloculina spp.

5.3.3 Biofacies PGH (Pararotalia cananeiaensis, Gavelinopsis praegeri, and Hanzawaia nitidula biofacies) This biofacies is present from 52.5 m to 46.2 m, 41m to 25.4 m, and 13.7 m to 9 m. It can represent a complex environment, like an estuary with high marine influence, with characteristic middle/outer shelf species. The Pararotalia cananeiaensis dominated

ACCEPTED MANUSCRIPT with abundance above 13%, reaching 45% at 46.2 m, Gavelinopsis praegeri above 10%, reaching 21% at 27.7 m, and Hanzawaia nitidula above 11%. The occurrence of marine species such as G. praegeri can infer neritic to bathyal environment (Martins and Gomes, 2004) or the presence of an estuary (Debenay et al.,

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2006). Low diversity and equitability can indicate a stressful environment that is common in estuaries, from 52.5 m to 46.2 m. From 41 m to 25.4 m there are high richness, diversity, and equitability, indicating middle to outer shelf environment. The

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absolute abundance reaches 90.368 tests in this interval. The presence of dominant

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marine species such as Cassidulina spp. (29.5 m, 28.9 m and 27.7), Cibicidoides pseudoungeriana (39.8 m), Neoconorbina spp. (37.4 m), Rosalina spp. (52.5 m, 51.6 m, 51 m, 50 m, 41 m and 35 m) and other associated species corroborate the assignment of this

biofacies

to

a

shelf

environment

(Angulogerina

spp.,

Bolivina

spp.,

Trifarina spp.).

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Globocassidulina spp., Islandiella spp., Quinqueloculina spp., Sahulia conica and

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5.3.4 Biofacies QL (lagoonal miliolids biofacies) This biofacies is characterized by several species of Quinqueloculina and Triloculina

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and occur from 19.4 to 17.2 m. It differs from QP by low richness and diversity and low abundance of marine species. The abundance of Quinqueloculina (above 19%, reaching 40% at 18.2 m) and Triloculina (10%) indicates hypersaline and restricted or confined lagoon (Debenay et al., 2001a; Murray, 2006; Scott et al., 2004). The associated species are Miliolinella subrotunda, Pararotalia cananeiaensis, Poroeponides lateralis, Cribroelphidium spp., Elphidium spp. and Ammonia spp.

5.3.5 Biofacies HP (Haynesina germanica and P. cananeiaensis biofacies)

ACCEPTED MANUSCRIPT This biofacies is associated with paralic environment, such estuaries and lagoons by the abundance of Haynesina germanica (above 28%, reaching 38% at 14.9 m) and P. cananeiaensis (above 35%) (Alday et al., 2013; Debenay et al., 1998; Martins and Gomes 2004; Murray, 2006; Semensatto-Jr. et al., 2009). It occurs from 16.05 to 14.9

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m. There are high richness and low diversity and equitability. The associated species are Ammonia spp., Bolivina spp., Buliminella elegantissima, Fissurina spp., Gavelinopsis

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praegeri, Quinqueloculina spp. and Rosalina spp.

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5.4 Paleoenvironmental history

From bottom to top of the core, the presence of the foraminiferal biofacies pointed out the sea-level oscillation with sea ingressions and a succession of marine environments. The establishment of the coastal area occurred with the rose of the sea level and the establishment of the inner shelf (ABP, QP). After that, the sea level fell and the area

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changed to an estuary and rose again establishing middle/outer shelf (PGH). The sea level fell and the environment became inner shelf (QP), turning into the hypersaline

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lagoon (QL), and then into the normal lagoon (HP) until the end of the marine influence. At the top of the core occurred the biofacies PGH between barren samples,

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inferring a marine ingression in a period of sea-level oscillation. Barren intervals with sandy sediments can represent fluvial deposits (Plantz, 2014) (Figure 6). The data were integrated with biotic components. It was possible to confirm a greater marine influence when marine organisms like ascidia, echinoderm, nannofossils and/or scaphopods occurred in marine sample intervals. The results of the benthic foraminiferal biofacies in this well core must be integrated to results from other cores which are still in study, for a better understanding of the paleoenvironmental evolution of the Paraíba do Sul River deltaic complex.

ACCEPTED MANUSCRIPT Five barren samples for foraminifera occur in the base of the well core, from 64.35 to 61.95 m, although one of the samples (63.15 m) presents nannofossils (Motta, 2016). The absence of foraminifera in river mouths can be explained by the high turbidity, high sedimentation rate, resuspension and reworking, due to frequent erosion and deposition

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processes, making the substrate unstable for the development of benthic foraminifera, as assumed by Vilela (1995) at the mouth of the Amazon river. Nevertheless, the high clay indexes (80%) in the current study suggested a tidal flat environment (Plantz, 2014).

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Probably, the fluvial influence was greater than marine, preventing the establishment of

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benthic foraminifera or did not occur the preservation of foraminifera.

Five tests demonstrate the increase of marine influence at 61.35 m: Ammonia parkinsoniana (three), Lagena sp. (one) and Quinqueloculina sp. (one test). It is not possible to interpret the paleoenvironment with five tests, however echinoderm spines

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also occur in this sample, suggesting that the environment changes to coastal one. At 60 m, biofacies ABP represents the beginning of the marine influence (AmmoniaElphidium association) evolving to shelf environment (Bolivina spp.) with low oxygen

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and high content of organic matter. The abundance of Bolivina spp. and the presence of species such as Ammonia parkinsoniana, Buliminella elegantissima, Fursenkoina

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pontoni and Hopkinsina pacifica corroborate the interpretation. Van Der Zwaan and Jorissen (1991) observed the occurrence of zones parallel to the coast, rich in organic matter with anoxic or disoxic conditions at the water-sediment interface, in three river discharge areas. The above mentioned authors and Duleba et al. (2003) interpret marine transgression conditions.

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ACCEPTED MANUSCRIPT

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Figure 6 – Schematic interpretation of the pleistocenic deposits in 2-MU-1-RJ well core according to foraminiferal biofacies. ABP - Ammonia parkinsoniana, Bolivina spp. and Pararotalia cananeiaensis biofacies; QP - shelf miliolids biofacies; PGH - P. cananeiaensis, Gavelinopsis praegeri, and Hanzawaia nitidula biofacies; QL - lagoonal miliolids biofacies; HP - Haynesina germanica and P. cananeiaensis biofacies (modified from Rodrigues et al., 2015).

At 57 m, the environment becomes coastal marine, with the presence of characteristic species like Ammonia parkinsoniana, Pararotalia cananeiaensis, and Rosalina spp. At 55.8 m, the presence of Angulogerina spp., Cassidulina spp., increases of Bolivina spp. and reduction of Ammonia spp. indicate the return of the shelf environment. At 55.2 m, the abundance of Bolivina spp. (13.5%) points to increase of organic matter in the environment.

ACCEPTED MANUSCRIPT The shelf environment is still present with an increase of miliolids, biofacies QP, from 54.6 to 54 m. Vieira et al. (2014) characterized the biofacies Pseudononion atlanticummiliolids between 25 and 50 m, in the shelf in front of São Tomé Cape, with superficial salinity at 34.8 and bottom salinity at 35.8 ‰. The presence of calcareous species such

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as Angulogerina spp., Bolivina spp., Gavelinopsis praegeri, Eponides repandus, Mullinoides differens, and porcelaneous as Pyrgo spp., reduction of P. cananeiaensis and absence of H. germanica, indicate normal salinity, despite the increase of miliolids.

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planktonic foraminifera and echinoderms.

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It is possible to infer a normal marine environment at 54 m, due to the presence of

The shelf environment becomes shallow indicated by the presence of H. germanica, from 52.5 to 46.2 m, biofacies PGH. In these samples occur planktonic foraminifera, echinoderms, and ascidia. Broken and reworked tests can infer hydrodynamic

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environment under stress.

The environment becomes a middle to outter shelf from 41 to 25.4 m, biofacies PGH. The abundance of Angulogerina spp. and presence of Trifarina bradyi and, Uvigerina

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spp. indicates a deeper marine environment. The P/B ratio indicates that the greatest depth was reached at the sample interval 28.9 m. Planktonic foraminifera and

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echinoderms occur in all samples; nannofossils (Motta, 2016) and ascidia occur in the majority (Table B).

The biofacies QP, from 24.2 to 21.8 m, indicates once more inner shelf environment. Planktonic foraminifera and ascidia occur in all samples. The environment becomes a hypersaline lagoon at the interval 19.4 till 17.2 m, biofacies QL. Ascidia, echinoderms, nannofossils (Motta, 2016) and planktonic foraminifera occur in these samples, indicating marine influence. However, those marine organisms do not occur in the sample with more than 50% of miliolids (18.2 m). The environment evolved to the

ACCEPTED MANUSCRIPT lagoon with normal salinity, biofacies HP, from 16.05 to 14.9 m. The presence of marine species indicated marine influence, corroborated by the presence of ascidia, echinoids, nannofossils (Motta, 2016) and planktonic foraminifera. At 13.7 and 9 m, the biofacies PGH pointed to marine ingressions. At 9 m, it could be a record of a washover

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between fluvial sediments. The marine influence decreases at 12.5 m and occurs the sedimentary infilling of the lagoon. The absence of benthic foraminifera at 9.35 and 1.85 m indicates that the environment becomes continental.

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The models proposed by Martin et al. (1997, 1993) described stages with estuaries and

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lagoons formed by a pleistocenic transgression in 123,000 years BP. The paleoenvironment succession presented here can be placed from that pleistocenic transgression until a holocenic transgression in 5,100 years BP, according to those evolution models. The age dating of the core is not precise and it doesn’t permit to link

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the characterized biofacies to the events proposed by those authors. When we compare the paleoenvironment succession interpreted through sedimentary facies and through biofacies (Table 1), it is clear how foraminifera add information to

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the studied core, as they are controlled by other factors but the sedimentation. Foraminifera biofacies contributed to refining the paleoenvironment interpretations and

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qualitative information.

ACCEPTED MANUSCRIPT Table 1 – Paleoenvironment succession interpreted by sedimentary facies (Plantz, 2014) and biofacies (present work) in the 2-MU-1-RJ core.

Paleoenvironments (Plantz, 2014) Fluvial

Paleoenvironments (Present work) Barren Overwash

Marine

Lagoon Hypersaline Lagoon

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Lagoon

Inner or Outer Shelf Barren Estuary

Inner Shelf

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Tidal Flat

Barren

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Depths (m) 0 - 9.0 9.0 - 13.7 13.7 - 14.9 14.9 - 17.2 17.2 - 21.8 21.8 - 30.0 30.0 - 42.0 42.0 - 46.0 46.0 - 52.3 52.3 - 55.2 55.2 - 61.4 61.4 - 68.0

6 Conclusions

In the Brazilian east-southeast coastal areas there are described stages with estuaries and lagoons formed by the sea transgressions during the Pleistocene. The succession of the

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foraminiferal biofacies along the studied well core at the Paraíba do Sul River Deltaic Complex contributes to the knowledge of that paleoenvironmental evolution. The

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complex and abundant assemblage of benthic foraminifera of the 2-MU-1-RJ well core shows the pleistocenic dynamics of the deltaic complex, with indicator species of both

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coastal and shelf environments. The sedimentary facies were refined by five benthic foraminifera biofacies alternating from the core bottom to the top, inferring several marine paleoenvironment successions. According to the P/B ratio, the deepest depth (higher P/B ratio) occurs at the core depth of 28.9 m. Biofacies characterized middle/outer shelf at this interval. The classification and distribution of the benthic foraminiferal species in this study determined five biofacies that show the evolution of the Paraíba do Sul Deltaic Complex in the Mussurepe region. At the lower part of the studied portion the paleoenvironmental evolution change from coastal to the inner shelf

ACCEPTED MANUSCRIPT and it is associated with low oxygen in the sediments, occurring a change from deeper to shallower environments, and tests reworking. In the middle portion, the environment evolved to the middle or outer shelf, and then to a hypersaline and normal lagoon. A succession of fluvial deposits with a marine ingression occurs in the top of the well

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core, at the interval of 9 m. It could be a record of washover plain. Comparing the paleoenvironments interpreted through sedimentary facies and biofacies, it becomes clear the importance of paleontological studies for better comprehension of the studied

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area and how the foraminifera can be a good tool to understand the environment

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evolution in an area.

Acknowledgements

We thank Dr. Leonardo Borghi, MSc. Thiago Carelli and MSc. Josiane Plantz

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(LAGESED, Universidade Federal do Rio de Janeiro) for the samples and to let us contribute to Projeto Delta (UFRJ/UFF/Chevron – Fundação Coppetec IGEO-15.857). This work was supported by CNPq (Conselho Nacional de Desenvolvimento Científico e Tecnológico), FAPERJ (Fundação de Amparo à Pesquisa do Estado do Rio de

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Janeiro) and Universidade Federal do Rio de Janeiro. We thank Dr. Virgínia Martins and the two anonymous reviewers for their suggestions and collaboration in the

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improvement of this work.

Supplementary Data Table A Table B

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Machado, A.J., Araújo, H.A.B., 2014. Characterization of the Caravelas River Estuary ( Bahia ) from a Temporal Distributional Analysis of the Foraminifera Microfauna Caracterização do Estuário do Rio Caravelas ( Bahia ) a partir de Análises de Distr. Anuário do Instituto de Geociências - UFRJ 37, 23–38. doi:http://dx.doi.org/10.11137/2014_2_23_38 Martin, L., Suguio, K., Flexor, J.-M., Dominguez, J.M.L., Azevedo, A.E.G. de, 1984. Evolução da planície costeira do Rio Paraíba do Sul (RJ) durante o Quaternário: Influência das flutuações do nível do mar. Anais do XXXIII Congresso Brasileiro de Geologia. Martin, L., Suguio, K., Flexor, J.M., 1993. As Flutuações de Nível do Mar Durante o Quaternário Superior e a Evolução Geológica de ‘Deltas’ Brasileiros. Boletim IGUSP. PublicaçÃ\poundso Especial 1–186. doi:10.11606/issn.23178078.v0i15p01-186 Martin, R.E., Harris, M.S., Liddell, W.D., 1995. Taphonomy and time-averaging of foraminiferal assemblages in Holocene tidal flat sediments, Bahia la Choya, Sonora, Mexico (northern Gulf of California). Marine Micropaleontology 26, 187–

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ACCEPTED MANUSCRIPT Vilela, C.G., Figueira, B.O., Macedo, M.C., Baptista Neto, J.A., 2014. Late Holocene evolution and increasing pollution in Guanabara Bay, Rio de Janeiro, SE Brazil. Marine Pollution Bulletin 79, 175–187. doi:10.1016/j.marpolbul.2013.12.020 Winter, W.R., Jahnert, R.J., França, A.B., 2007. Carta Estratigráfica Bacia de Campos. Boletim de Geociências da Petrobras. APPENDIX A

A. tepida Cushman, 1926 Ammonia sp.1 Angulogerina cojimarensis Palmer, 1941

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Angulogerina sp.1 Bolivina compacta Sidebottom, 1905

B. ordinaria Phleger and Parker, 1952

B. pseudoplicata Heron-Allen and Earland, 1930 B. spathulata Williamson, 1858 B. striatula Cushman, 1922

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B. variabilis Williamson, 1858

Buliminella elegantissima d’Orbigny, 1839 Cancris sagra d’Orbigny, 1839

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Cassidulina braziliensis Cushman, 1922 C. laevigata d’Orbigny, 1826

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C. reniforme Nørvang, 1945 C. teretis Tappan, 1951

Cibicidoides pseudoungeriana Cushman, 1922 Cribroelphidium incertum Williamson, 1858 C. poeyanum d’Orbigny, 1839 Elphidium discoidale d’Orbigny, 1839 E. gunteri Cole, 1931 Eponides repandus Fichtel and Moll, 1798 Fissurina cucurbitasema Loeblich and Tappan, 1953 F. laevigata Reuss, 1850

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Ammonia parkinsoniana d’Orbigny, 1839

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Alphabetic List of Main Species

ACCEPTED MANUSCRIPT F. lucida Williamson, 1848 F. marginata Montagu, 1803 Fursenkoina pontoni Cushman, 1932 Gavelinopsis praegeri Heron-Allen and Earland, 1913

G. subglobosa Brady, 1881 Hanzawaia nitidula Bandy, 1953 Haynesina depressula Walker and Jacob, 1798 H. depressula var. matagordanum Kornfeld, 1931 H. germanica Ehrenberg, 1840

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Hopkinsina pacifica Cushman, 1933 Islandiella helenae Feyling-Hanssen and Buzas, 1976 I. norcrossi Cushman, 1933 Lagena substriata Williamson, 1848 L. sulcata Walker and Jacob, 1798

Lenticulina sp.1

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Lenticulina cultrata Montfort, 1808

Miliolinella subrotunda Montagu, 1803 M. suborbicularis d’Orbigny, 1839

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Neoconorbina albida McCulloch, 1977 N. crustata Cushman, 1933

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N. parkerea Natland, 1950 N. terquemi Rzehak, 1888

Oolina lineata Williamson, 1848 O. stelligera Brady, 1881 Pararotalia cananeiaensis Debenay et al., 2001 Pileolina patelliformis Brady, 1884 Pseudotriloculina laevigata d’Orbigny, 1839 Pyrgo murrhina Schwager, 1866 P. nasuta Cushman, 1935 P. ringens Lamarck, 1804

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G. minuta Cushman, 1933

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Globocassidulina crassa d’Orbigny, 1839

ACCEPTED MANUSCRIPT P. subsphaerica d’Orbigny, 1839 Quinqueloculina angulata Williamson, 1853 Q. bosciana d’Orbigny, 1839 Q. candeiana d’Orbigny, 1939 Q. delicatula Vella,1957

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Q. frigida Parker, 1952 Q. laevigata d’Orbigny, 1839 Q. lamarckiana d’Orbigny, 1839 Q. parallela Zheng, 1979

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Q. poeyana d’Orbigny, 1839 Q. schlumbergeri, Wiesner, 1923

Q. vulgaris d’Orbigny, 1826 Reussoolina laevis Montagu, 1803 Rosalina floridana Cushman, 1922 R. globularis d’Orbigny, 1826

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Q. seminula Linné, 1767

R. williamsoni Chapman and Parr, 1932

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Sahulia conica d’Orbigny, 1839

Trifarina angulosa Williamson, 1858 T. bradyi Cushman, 1923

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Triloculina baldai Bermúdez and Seiglie, 1963 T. oblonga Montagu, 1803

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T. trigonula Lamarck, 1804

Uvigerina canariensis d’Orbigny, 1839 U. peregrina Cushman, 1923

Appendix B. Supplementary data

ACCEPTED MANUSCRIPT Paleoenvironments (Present work)

Paleoenvironments (Plantz, 2014)

Barren

Fluvial

Overwash Lagoon Hypersaline Lagoon

Lagoon

Inner or Outer Shelf

Marine

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Barren Estuary

Tidal Flat

Inner Shelf Barren

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Depths (m) 0 - 9.0 9.0 - 13.7 13.7 - 14.9 14.9 - 17.2 17.2 - 21.8 21.8 - 30.0 30.0 - 42.0 42.0 - 46.0 46.0 - 52.3 52.3 - 55.2 55.2 - 61.4 61.4 - 68.0

ACCEPTED MANUSCRIPT

7

8

5

9

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SC

6

4

3

2

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1

11

16

13

12

17

14

18

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EP

15

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10

19

20

21

22

2

5

6

9

10

13

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1

3

4

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ACCEPTED MANUSCRIPT

8

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ACCEPTED MANUSCRIPT Highlights Five biofacies based on benthic foraminifera were recognized. Organic matter and disoxic conditions were identified by indicator species. The planktic/benthic ratio indicates the deepest depth at the interval of 28.9 m. Lithofacies were refined by foraminiferal biofacies.

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